Contributions to the Ordovician 

Paleontology of Kentuck1R?{g@~D\YJJ:g 

and Nearby States Nov 9 1979 IDJ 

FISHERIES RESEARCH 

The Ordovician Paleontology of Kentucky and Nearby States-Introduction LAB LIBRARY 

The Brachiopod Genus Platystrophia 

Middle and Late Ordovician Plectambonitacean, Rhynchonellacean, Syntrophiacean, 

Trimerellacean, and Atrypacean Brachiopods 

Additional Trilobites From the Ordovician of Kentucky 

Edrioasteroids (Echinodermata) 

Asteroidea (Echinodermata) 

Conodonts and Conodont Biostratigraphy of Post-Tyrone Ordovician Rocks 

of the Cincinnati Region 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-A-G 

Prepared in cooperation with the 

Commonwealth of Kentucky, 

University of Kentucky, 

Kentucky Geological Survey 
Contributions. to the Ordovician 

PaleontOlogy of Kentucky 

and Nearby States 

. Edited by.John Pojet~, Jr. 

A. The Ordovician Paleontology of Kentucky and Nearby StatesIntroduction, by John Pojeta, Jr. 

B. The Brachiop~d Genus Platystrophia, by Leonard P. Alberstadt 

C. Middle and ~~te Ordovician Plectambonitacean, Rhynchonellacean, Syntrophiacean, 

TrimereUacean, and Atrypacean Brachiopods, by Herbert J. Howe 

D. Additional T;ilobites From the Ordovician of Kentucky, by Reuben James Ross, Jr. 

E. Edrioasteroids (Echinodermata), by Bruce M. Bell 

F. Asteroidea (Echinodermata), by J. W. Branstrator 

G. · Conodonts and Conodont Biostratigraphy of Post-Tyrone Ordovician Rocks 

of the Cincinnati Region, by Walter C. Sweet 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-A-G 

Prepared in cooperation with the 

Commonwealth of K~n'tucky, 

University of Kentucky,. 

Kentucky Geological SUrvey 

UNITED STATES GOVERN.MENT PRINTING. OFFICE, WASHINGTON 19 79 
UNITED STATES DEPARTMENT OF THE INTERIOR 

CECIL D. ANDRUS, Secretary 

GEOLOGICAL SURVEY 

H. William Menard, Director 

Library of Congress Cataloging in Publication Data 

Main entry under title: 

The Ordovician paleontology of Kentucky and nearby States. 

(Geological Survey professional paper; 1066-A-G) 

Includes bibliographies and indexes. 

CONTENTS: [1] Pojeta, J., Jr. Introduction.-[2] Alberstadt, L. P. The b;rachiopod genus Platystrophia.-[3] Howe, H. J. Middle and late Ordovician plectambonitacean, rhynchonellacean, synthrophiacean, trimerellacean, and atrypacean brachiopods. [etc.] 

1. Invertebrates, Fossil. 2. Paleontology-Ordovician. 3. Paleontology-Kentucky. 4. Paleontology-

,Southern States. I. Pojeta, John. II. Kentucky. University. III. Kentucky. Geological Survey. IV. 

Series: United States. Geological Survey. Professional paper; 1066-A-G. 

QE770.07 562'.09769 77~608346 

For sale by the Superintendent of Documents, U.S. G~vernment Printing Office 

Washington, D.C. 20402 

Stock Number 024~001~03171-0 
I 

'' I I 

( 

CONTENTS 

Page 

A. The Ordovician paleontology of Kentucky 

and nearby States-Introduction, by 

John Pojeta, J r ---------------:----------------------- Al 

B. The brachiopod genus Platystrophia, by 

Leonard P. AlberstadL-------------------------- Bl 

C. Middle and Late Ordovician plectambonitacean, rhynchonellacean, syntrophiacean, 

trimerellacean, and atrypacean brachiopods, by Herbert J. Howe ---------------------- Cl 

D. Additional trilobites trom the Ordovician of 

Kentucky, by Reuben James Ross, Jr ----- Dl 

E. Edrioasteroids (Echinodermata), by Bruce M. 

Bell ------------------------------------------------------ E 1 

F. Asteroidea (Echinodermata), by J. W. Branstrator ---------------------.:--------------------------- Fl 

G. Conodonts and conodont biostratigraphy of 

post-Tyrone Ordovician rocks of the 

Cincinnati region, by Walter C. Sweet---- Gl 
The Ordovician Paleontology of 

Kentucky and Nearby StatesIntroduction 

By .JOHN PO .JET A, .JR. 

CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF 

KENTUCKY AND NEARBY STATES 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-A 

Prepared in cooperation with the 

Commonwealth of Kentucky, 

University of Kentucky, 

Kentucky Geological Survey 

A su1nmaTy of the lithostratigraphy 

ancl biost?·atigrajJhy of the area) 

a clescrijJtion of 1naterials ancl 

1nethocls) ancl a list of collecting 

localities foT the six syste1natic 

jJaleontology jJajJe?·s in this series 

UNITED STATES GOVERNi\1ENT PRINTING OFFICE, WASHINGTON 1979 
j 
CONTENTS 

Abstract -----------------------------------------------------------------

Introduction -------------------------------------------------------------

Acknovvledgments -----------------~--------------------------------------

Lithostratigraphy -------------------------------------------------------- Ashlock Formation _____________________ --- _ -- __ --------- ___ --- _ --- __ _ 

Tate ]dember ----------------------------------------------------

Gilbert ]dember -------------------------------------------------- Stingy Creek ]dember _________ ---- ___ - __ - ------------------------

Terrill ]dember ________________________ - ------ ___ - ---------------

Reba ]dember ----------------------------------------------------

Bull Fork Formation -------------------------------------------------

Sunset ]dember ---------------------------------------------------

Callovvay Creek Limestone --------------------------------------------

Camp Nelson Limestone ----------------------------------------------

Clays Ferry Formation -----------------------------------------------

Point Pleasant Tongue -------------------------------------------- Dillsboro Formation ______________ --- __________ -----------------------

Drakes Formation ---------------------------------------------------- Rovvland ]d,ernber _____________________ ---------------------------- Preachersville ]dember _____________________ --- __________________ _ 

Otter Creek Coral Bed ----------------------------------------

Bardstovvn ]dember ----------------------------------------------- Saluda Dolomite ]dember (or Saluda Formation in Indiana) --------

Hitz Limestone Bed ------------------------------------------ Fairvievv Formation ______________________ ------- __ -------- __________ _ 

North Bend Tongue ---------------------------------------------- Garrard Siltstone ___________ ------ ______________ ------ _ ----- ________ _ 

Grant Lake Limestone ------------------------------------------------ Bellevue Tongue (or "Bellevue Limestone") ------------------------

High Bridge Group ---------------------------------------------------

Kope Formation ------------------------------------------------------

Grand Avenue ]dember -------------------------------------------- Wesselman Tongue __________________________ ----- ______ ------ ___ _ 

Leipers Limestone ------------- ______________ ---------- ___ --------- __ _ 

Lexington Limestone --------------------------------------------------

Curdsville Limestone ]dember --------------------------------------

Logana ]dember -------------------------------------------------- Grier Limestone Member ------------------------------------------

]dacedonia Bed -----------------------------------------------

Cane Run Bed ----------------------------------------------- Perryville Limestone ]dember --------------------------------------

Faulconer Bed -----------------------------------------------

Salvisa Bed --------------------------------------------------

Cornishville Bed ----------------------------------------------

Brannon Member _ ------------------------..,.-----------------------

Sulphur Well ]dember -----------------------~-------------------­

Stamping Ground Member -------------------~-------------------- Greendale Lentil _____________________________ ------ _______ ----- __ 

Devils Hollovv ]dember ___________________________________________ _ 

Millersburg ]dember _______ ------------ ___ ------------------------

Strodes Creek ]dember -------------------------------------------- Tanglevvood Limestone ]dember ___________________________ ------ __ _ Nicholas Bed _______________________________________________ _ 

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III 
IV CONTENTS 

Lithostratigraphy-(Continued) 

Lexington Limestone-(Continued) 

Page 

Miamitown Shale ---------------------------------------------- A13 

Oregon Formation ---------------------------------------------------- 13 

Tyrone Limestone ---------------------------------------------------- 13 

Whitewater Formation ----------------------------------------- 13 

Middle Ordovician-Upper Ordovician boundary ------------------------------ 13 

Other biostratigraphic boundaries ------------------------------------------ 15 

Materials and methods ---------------------------------------------------- 15 

Locality register ______________________________ -------------------------- _ 19 

References cited ---------------------------------------------------------- 46 

ILLUSTRATIONS 

Page 

FIGURE 1. Index map showing location of tristate area studied and outcrop of 

Ordovician rocks ------------------------------------------- A2 

2. Stratigraphic columns for various geographical areas in the area of 

study ----------------------------------------------------- 4 

3. Index to 7.5-minute quadrangles from which collections were made in 

the area of study ----------------------------------------- 16 

SYSTElVI OF lVIEASUREl\tiENT UNITS 

The investigations underlying this series of reports were made over a period of 

years, and distances and stratigraphic measurements appear fairly uniformly in 

English units. Measurements of fossil specimens, on the other hand, follow the longstanding convention of appearing in metric units. Because of the dates of the investigations and the amount of resulting data, the English measurements have been retained. Conversions to metric units may be made by using the following conversion 

table: 

To convert 

English unit: To metric unit: Multiply by: 

Mile (mi) --------------- Kilometer (km) ----------------- 1.61 

Foot (ft) ----------------Meter (m) ---------------------- .305 
CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY 

AND NEARBY STATES-INTRODUCTION 

By JoHN PoJETAJ JR. 

ABSTRACT 

The introduction contains the g1eneral information common 

to the systematic paleontology sections that are included in 

the six accompanying reports (Chapters B-G) . This general information consists of brief desc·riptions of the formations from which the fossils were collected, the environments 

of deposition of the formations, current thoughts on the 

placement of the Middle Ordovician-Upper Ordovician boundary in the area of study, a summary of the current stadial 

classification of the outcropping Ordovician rocks in the area 

of study, the methods used for extracting silicified fossils 

from limestone, and a locality register. 

INTRODUCTION 

This chapteT and chapters B to G of Professional 

Paper 1066 are part of a series of papers primarily 

dealing with the Ordovician megafossils of Kentucky. Previous reports in this series have dealt with 

some of the trilobites (Ross, 1967) and brachiopods 

(Neuman, 1967) ; the parts of the fauna described 

in these reports are: the brachiopod genus Platystrophia (Alberstadt, chapter B) ; plectambonitacean, rhynchonellacean, syntrophiacean, and trimerellacean brachiopods (Howe, chapter C) ; trilobites 

(R. J. Ross, Jr., chapter D) ; edrioasteroids (Bell, 

chapter E); and asteroids (Branstrator, chapter F); 

the conodont biostratigraphy of the area is summarized by Sweet (chapter G) . 

Most of the material described consists of silicified 

specimens from central and north-central Kentucky 

(Blue Grass region). Some of the specimens are 

from the Cumberland River area of south-central 

Kentucky near the Tennessee border, and some are 

from nearby States, particularly Ohio and Indiana 

(fig. 1). The tristate area of Kentucky, Ohio, and 

Indiana is a classical one in the study of late Middle 

and Late Ordovician faunas of North America, and 

it is the type area for the Am.erican Upper Ordovician stages (Edenian, Maysvillian, and Richmondian). Once the megafaunas are redescribed in modern terms, this information can be used for a biostratigraphic synthesis of the area; this synthesis 

can then be compared with the biostratigraphic conclusions derived from the study of conodonts of the 

area, which are summarized in Bergstrom and Sweet 

(1966), Sweet and Bergstrom (1971) and Sweet 

herein. 

This report contains the stratigraphic and locality 

information for each of the collections cited in the 

paleontological chapters. This information is gathered together in a lo·cality register at the end of the 

introduction. 

The U.S. Geological Survey, in cooperation with 

the Kentucky Geological Survey, began the geologic 

mapping of Kentucky in 1961. The scale used in this 

mapping program is 1:24,000 and the State is being 

mapped quadrangle by quadrangle; this project is 

now nearly completed. The mapping program resulted in the accumulation of large numbers of fossils, particularly from the Ordovician outcrop area, 

and faunal lists were published on many of the maps. 

In addition, Cressman (1973) published several lines 

of sections that included faunal lists. In part these 

faunal lists are documented herein, and the identifications provided supersede all previous identifications. The same collection numbers. are used her.ein, 

on the quadrangle maps, and in Cressman (1973). 

The collections made by the mapping parties were 

augmented and expanded by various paleontologists 

of the U.S. Geological Survey, with especial concentration on silicifi·ed fossils in the Lexington Limestone. Silicification of the fauna above and below the 

Lexington Limestone is neither ·so well developed 

nor so widespread; where silicification of fossils was 

found in these intervals, collections were made. The 

Al 
A2 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

rI 

\ 

) 

I ·' 

/ "' ,; 

,; " 

/ ""-. / --------------r-----

__ / 

INDIANA 

KENTUCKY 

OHIO 

I 

, 

\ 

/ 

I 

/ 

\ 

\ 

( 

( 

'\' 

I L' 

"-/ 

./ 

; 

/ 

------------~-------/// 

I I I I I I I I I ~ 50 100 150 200 250 KILOMETERS 

I I I I I I I 0 50 100 150 MILES 

.... -.--, / I 

I 

I 

( 

) 

/ 

/ 

\ 

I 

) 

FIGURE 1.-Index map showing location of the tristate area studied and the surface exposure of the Ordovician rocks 

sampled (patterned). Modified from King and Beikman (1974). 

new well-preserved material described herein is accurately located geographically and stratigraphically; it has presented an unparalleled opportunity to 

restudy the paleontology and bio·stratigraphy of a 

classical area. 

Although it is now standard procedure for U.S. 

Geological Survey reports to use metric units of 

measure, much of the work reported here was done 

at a time when English units of measure were used. 

Thus, most of the stratigraphic measurements are 
INTRODUCTION A3 

given in feet, and the size of collections of silicified 

fossils is given in pounds. Because some of the field 

and laboratory work dates back to 1961, it was felt 

that it simply would not be sufficiently profitable to 

convert this mass of data to metric units. Further, 

many of the collections cited in the locality register 

are also listed on Cressman's (1973) stratigraphic 

sections and on published quadrangle maps, and as 

these publications used English units of measure, 

it facilitates comparison to use these here also. 

Where pos·sible, as in the measurements of specimens, m.etric units of measure have been used. 

ACKNOWLEDGMENTS 

Most of the material described was collected by 

members of the U.S. Geological Survey; specimens 

not collected by members of that organization are 

individually acknowledged in the appropriate places 

in the text. Members of the U.S. Geological Survey 

who contributed significantly to the collecting of the 

Ordavician fossils in the area of study are: D. F. B. 

Black, E. R. Cressman, N. P. Cuppels, R. C. Green, 

A. B. Gibbons, 0. L. Karklins, R. C. Kepferle, S. J. 

Luft, R. B. Neuman, W. F. Outerbridge, J. H. Peck, 

W. L. Peterson, John Pojeta, Jr., J. S. Pomeroy, R. J. 

Ross, Jr., G. C. Simmons, W. C. Swadley, G. W. Weir, 

the late D. E. Wolcott, and E. L. Yochelson. W. C. 

MacQuown, Jr., of the University of Kentucky, also 

collected sp.ecimens. David Oldham, Andrea Ludwig, 

Malikah Roberts, and L. W. Ward did much of the 

laboratory processing of silicified specimens. 

LITHOSTRATIGRAPHY 

The past decade has been one of intense interest in 

and much work on the lithostratigraphic classification of the Middle and Upper Ordovician rocks of the 

tristate area of Kentucky, Ohio, and Indiana. Much 

of the work in central and north-central Kentucky 

has resulted from the U.S. Geological Survey-Kentucky Geological Survey cooperative mapping program, and significant changes have been made in the 

lithostratigraphic classification of the Ordovician 

rocks of Kentucky above the Tyvone Limestone. All 

the rock units are now based upon well-documented 

and measured type sections. They have been mapped 

over all the outcrop area, and the facies relationships 

have been worked out. This new lithostratigraphic 

information is published in a number of works including: Weiss and Sweet (1964); Black and MacQuown (1965); Black, Cressman, and MacQuown 

(1965); Weir and Greene (1965); Weir, Greene, and 

Simmons (1965) ; Peck (1966) ; Simmons and Oliver 

(1967); MacQuown (1967); Weir and Peck (1968); 

Hatfield (1968) ; Ford (1968) ; Anstey and Fowler 

(1969) ; Peterson (1970) ; Cressman and Karklins 

(1970); Hrabar, Cressman, and Potter (1971); Wolcott, Cressman, and Connor (1972); Black and Cuppels (1973); Cressman (1973); Swadley, Luft, and 

Gibbons, 1975; Cressman and Noger, 1976; and Ethington and Sweet, 1977. In addition to these publications, much stratigraphic information is summarized 

on the various geologic quadrangle maps of the Blue 

Grass region of Kentucky; the names of the maps 

are listed for each locality in the locality register. 

Weiss and Norman (1960a) summarized the development of the stratigraphic classification of the 

Ordovician rocks exposed in the Cincinnati, Ohio, 

region to 1960. Since that publication, Weiss and 

Sweet (1964) ; Ford (1967, 1972, 1974) ; Hatfield 

(1968) ; Osborne (1968, 1974) ; and Anstey and 

Fowler (1969) have given further consideration to 

the classification of the Ordovician rocks of southwestern Ohio. Recent consideration o.f the stratigraphic classification of the Ordovician rocks of 

southeastern Indiana can be found in Fox (1962) ; 

Brown and Lineback (1966) ; Brown and Anstey 

(1968) ; Hatfield (1968) ; Anstey and Fowler 

(1969) ; Gray (1972) ; and Hay (1977). 

Herein, the lithostratigraphic information for the 

area of study is summarized in brief descriptions for 

each of the rock units, and in a series of ·stratigraphic columns for the various geographic areas 

where the formations crop out (fig. 2). The brief 

descriptions of the rock units are arranged alphabetically, and they are provided in order to allow 

readers to have some idea of the lithologic differences 

between units without having to. refer elsewhere. 

Members of a formation are arranged in ascending 

order under the formation name. For the most part 

thes.e descriptions are taken from or paraphrased 

from the works cited above; the work or works from 

which each rock description is taken are cited at the 

end of the description. Many of the units pinch out, 

and the thicknesses given are for their principal 

areas of outcrop. A number of authors have attempted to determine the environment of deposition 

of the formation they were describing; where such 

information is available, it is indicated below after 

the lithologic description of the formation. In figure 

2, each column is taken from the author indicated, 

and in most cases each stratigraphic column is a 

composite of the.area indicated. 
A4 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

I I 

INDIANA 

I 

I 

,-.._.,. 

; 

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IJ 

Whitewater 

Formation 

Saluda Formation 

Dillsboro 

Formation 

Kope 

Formation 

Point Pleasant 

Tongue11 

Bull Fork 

Formation 

~ Bellevue Limestoner 

Miamitown Shale -

---{airview 

·~. c Formation 

Kope 

Gra·-=:nd'"'A""v=en"'"ue"M""'e=m"'"bedr 

Formation 

/ Bellevue Tongue3 , 

1

--..., Fairview ' 

, Formation l \ Kope 

OHIO 

--- /-~- ~ -~.....__ ... -......_ : \.._ ., ' Formation \ ._/ - I l eo'"'"-"' 4eFalmouth 'S~,_f"'-,, /./ \ 

-

Tongue t F~~~~~~n Maysville \../ ' - \ Preachersville ........____ 

Drakes Formation 

Calloway Creek 

Limestone 

Clays Ferry 

Formation 

•Maud 

9 

1 Of Clay Ferry Formation 2

As used by Ford (1967) 30f Grant Lake Limestone 

Garrard Siltstone 

Clays Ferry 

Formation 

Upper part 

of Lexington 

Limestone 

f-/Brannon Member of'-

Lexington Limestone 

Kope 

Formation 

Point Pleasant 

Tongue 1 

Grier Limestone 

Member of 

Lexington 

Limestone 

o7°L~=~n~~~ .lexington 

Member Drakes Formation 

Bull Fork 

Formation 

Grant Lake 

Limestone 

Fairview 

Formation 

Kope 

Formation 

Limestone 7 ~~~--~ •Winchester Tyrone Limestone 6 Oregon Formation 

Camp Nelson 

Limestone 

Drakes Formation 

Ashlock Formation 

Calloway Creek 

Limestone 

Garrard Siltstone 

Clays Ferry 

Formation 

•Lancaster 

8 

Drakes Formation 

Ashlock Formation 

Calloway Creek 

Limestone 

Garrard Siltstone 

Clays Ferry 

Formation 

Upper part of 

Lexington 

Limestone 

.~rannon ~~.?~mber of Lexington Limestone 

Lower part 

of Lexington 

Limestone 

~~ 

KENTUCKY 

3JOI- _,. )-

! ___ ... 

... • , ..... ,...,...... 

,.._,,' VIRGINIA ---------------------------------- ~--------------- 11 E N N E S S E E I ---- I 

10 20 30 40 50 KILOMETERS 

r-~~~,~~--~~~,--~I~IJ 

0 10 20 30 MILES 

FIGURE 2.--Stratigraphic columns, mostly composites, for by the addition of the Point Pleasant Tongue of the 

various geographic locations in the area of study. 1, at Clays Ferry Formation as suggested by Cressman (1973, 

Cincinnati, Ohio, modified from Ford (1967, fig. 2)" by p. 46). 4, at Falmouth, Ky., from Luft (1972). 5, at 

the use of the name Bull Fork Formation for beds above Maysville, from Peck (1966) fig. 2). 6, at Winchester, 

Ford's "Bellevue Limestone," which Ford left unnamed. from Black (1974). 7, composite section for the greater 

2, at Covington, Ky., across the Ohio River from Cin- Lexington-Frankfort area. 8, Lancaster, from Weir 

cinnati, Ohio, from Luft (1971). 3, southeastern In- (1971); 9, at Maud, from Peterson (1972). 

diana, modified from Brown and Lineback (1966, fig. 1) 
INTRODUCTION A5 

ASHLOCK FORMATION 

This unit is 125-145_ feet (ft) thick. The lower 

part is chiefly limy and dolomitic mudstone; the 

middle part is chiefly limestone and argillaceous 

limestone; and the upper part is greenish-gray unfossiliferous limy and dolomitic Mudstone overlain 

by gray thin-bedded fossiliferous s1lty granular limestone (Weir, Greene, and Simmons, 1965). The Ashlock Formation is divided into fiv,e members as follows (ascending) : 

TATE MEMBER 

This member is 30-80 ft thick and is the basal unit 

of the Ashlock Formation. The Tate Member is chief-. 

ly greeni·sh gray, laminated to thin-bedded, sparsely 

glauconitic, limy to dolomitic mudstone commonly 

grading at the top to argillaceous limestone; it contains few m.egafossils (Weir, Greene, and Simmons, 

1965). 

According to Weir and Peck (1968, p .168), their 

dolomitic mudstone lithofacies, to which the Tate 

Member belongs, was formed as very .shallow quietwater deposits, probably laid down on extens.ive flats. 

About 5 to 15 ft above the base of the Tate Mem.-

ber is a persistent unit, from 4 to 8 ft thick, of thin 

beds of olive-gray fine- to coarse-grained silty limestone containing silicified large brachiopods and bryozoans. This is the Back Bed of the Tate Member 

(Weir, Greene, and Simmons, 1965). It forms p·art 

of the nodular-bedded fossiliferous limestone and 

mudstone lithofacies of Weir and Peck (1968), and 

thus was formed in a higher energy environment 

than the rest of the Tate Member. 

GILBERT MEMBER 

This member i·s 10-20 ft thick. It overlies the basal 

Tate Member of the Ashlock Formation and underlies the Stingy Creek Member. The Gilbert is composed of bluish to olive-gray, aphanitic to mediumgrained limestone in crinkly beds a few inches thick. 

Gray limy siltstone oc-curs as partings and seams less 

than 1 in. thick. Contains abundant well-preserved 

megafossils (Weir, Greene, and Simmons, 1965). 

According to Weir and Peck (1968, p. 168), the 

micflograined limestone lithofacies. on the east side of 

the Cincinnati arch, of which the Gilbert Member is 

a part, was laid down in very shallow quiet-water, 

probably tide level lagoons, relatively free of terrigenous material. 

STINGY CREEK MEMBER 

The Stingy Creek Member ranges from 5 to 15ft 

in thickness; it overlies the Gilbert Member and underlies the Terrill Member. It is a sequence of silty 

limestone and limy siltstone. The limestone is chiefly 

mediurn light gray, fine to medium grained, and 

silty. It is obscurely thin bedded, partly in lenticles 

about an inch thick and a few inches long; fos·sils are 

abundant. The limy ·siltstone is chiefly light bluish 

gray and is gradational with the limestone with 

which it is interbedded (Weir, Greene, and Simmons, 1965) . 

The Stingy Creek Member belongs to the sam.e 

lithofacies as the Reba Member (Weir and Peck, 

1968) and suggests the same enviroonment of 

deposition. 

TERRILL MEMBER 

·This unit is 5-15 ft thick; it overlies. the Stingy 

Creek Member and underlies the Reba Member. The 

Terrill is mainly co·mposed of greenish-gray laminated limy or dolomitic mudstone. Many bedding 

surfaces are covered by ripple marks or mud cracks. 

The basal few feet of the member is a limy silty 

mudstone lacking distinct bedding. The· member contains few megafossils (Weir, Greene, and Simmons, 

1965). 

According to Weir and Peck (1968, p. 168), their 

dolomitic mudstone lithofacies., to which the Terrill 

Member belongs, was formed as very shallow quietwater deposits, proobably laid down on extensive flats. 

REBA MEMBER 

This m.ember is the toop unit of the Ashlock Formation, ranging from 10 to 25 ft in thickness. It is composed of micrograined limestone at the base, overlain by m;ore or les·s s.ilty, medium-grained limestone 

that at the top commonly grades into argillaceous 

limestone. Lim,estone in the lower 2-6 ft of the Reba 

Member is commonly in ledge-forming beds as much 

as a foot thick, is aphanitic and micrograined to very 

fine grained, and generally lacks megafossils. Most of 

the limestone in the member is fine to medium 

grained, has silty patche·s and partings in uneven 

beds a few inches thick, and contains abundant fossils (Weir, Greene, and Simmons, 1965). According 

to Weir and Peck (1968, p. 168), their nodularbedded fossiliferous limestone and mudstone lithofacies, to which the Reba Member belongs, was deposited in a higher energy environment than that 

indicated by the Gilbert Member rocks, possibly 

wave agitated shoals on the sloping shelf. 

BULL FORK FORMATION 

The Bull Fork Formation is about 200 ft thick in 

its type area along the Ohio River near Maysville, 
A6 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Ky., and it thins toward the south. The unit is composed of alternating shale and limestone, the shale 

content gradually increasing from about 20 p~ercent 

near the base to about 80 percent near the top of the 

formation. The shale i:S medium gray, grading to 

grayish green in the upper part; it is calcareous, 

plastic when wet, thin bedded, fissile to poorly fissile, 

and obscurely laminated. Shale occurs as thin partings and seams, and as sets from 1 in. to 4 ft thick 

between limestone beds. Fifty to 70 percent of the 

limestone in the unit is mainly gray with olive-gray 

to greenish-gray mottling. The limestone has a fairto well-sorted very fine to medium-grained matrix 

enclosing medi urn to very coarse fossil fragments 

that are oriented subparallel to the bedding. Bedding 

is even to irregular, and beds range in thickness 

from 1 to 8 in. Large ripple marks occur locally. The 

formation is very fossiliferous (Peck, 1966). 

According to Weir and Peck (1968, p. 168) their 

planar-bedded foss.iliferous limestone and mudstone 

lithofacies., to which the Bull Fork Formation belongs, is probably indicative of intermittently wave 

disturbed sediments deposited in more protected, 

perhaps deeper water, than the nodular-bedded limestone and mudstone lithofacies. 

SUNSET MEMBER 

The Sunset Member is as much as 30ft thick; it is 

composed of limestone and mudstone. The limestone 

is micrograined, in part silty and in part fine 

grained; bedding is variable. Near the base, limestone beds are irregular and nodular and from 1 to 3 

in. thick; beds are even, and as much as 3.5 ft thick 

near the middle of the unit; towards the top of the 

unit beds are knobby surfaced and 1-3 in. thick. 

Fossils in limestone beds are varied but sparse compared to overlying and underlying formations. Mudstone is calcitic, greenish and bluish gray, occurs in 

sets a few inches thick, and is generally unfossiliferous (Weir, 1975). 

CALLOWAY CREEK LIMESTONE 

This formation is composed chiefly of limestone 

with interbedded shale and minor siltstone and 

ranges in thickness from 80 to 130 ft. Limestone 

makes up 70-80 percent of the formation. It is mostly gray, fine to medi urn grained, and in .even beds 

0.1-0.3 ft thick. Greenish-gray, limy shale makes up 

15-25 percent of the formation and is interbedded 

with the limestone as partings or seams and, near 

the base, as thin sets as thick as 0.5 ft. Limy siltstone 

makes up about 5 percent of the Calloway Creek and 

occurs in even beds less than 0.5 ft thick, which are 

intercalated with shale and limestone in the lower 

third of the formation. The siltstone is gray to greenish gray and weathers yellowish brown. The formation is very fossiliferous (Weir, Greene, and Simmons, 1965) . 

According to Weir and Peck (1968) the Calloway 

Creek Limestone was deposited under approximately 

the same conditions as the Bull Fork Formation. 

CAMP NELSON LIMESTONE 

The maximum exposure of this unit is 320 ft; it 

i·s the basal formation of the Ordovician exposures in 

central Kentucky. The formation is composed of calcilutite interlaced with dolomite. The interlaced dolomite bodies resemble burrows (Wolcott, Cressman, 

and Connor, 1972; ·cressman, 1973). See High 

Bridge Group. 

CLAYS FERRY FORMATION 

This formation ranges from 120 to 220 ft in thickness. It is characterized by the interbedding of shale 

and limestone in equal amounts. The Clays Ferry 

contains more shale than the Lexington Limestone, 

Garrard Siltstone, and the Calloway Creek Limestone but less shale than the Kope Formation (E. R. 

Cressman, written commun., 1975). 

Cressman (1973, p. 45) commented on the depositional environment of the Clays Ferry Formation : 

***The less fossiliferous parts of the Clays Ferry Formation 

***closely resemble the interbedded calcisiltite and shale of 

the Logana and Brannon Members of the Lexington Limestone and were deposited in a similar environment; that is, 

in quiet water probably at least 25 m deep. The more fossiliferous parts of the Clays Ferry were probably deposited in 

at slightly shallower depths where the oxygenation and light 

would have, at least periodically, permitted the growth of 

the benthos. Yet, the currents were seldom strong enough to 

remove silt- and clay-sized particles or to comminute even 

thin and delicate shells. 

POINT PLEASANT TONGUE 

This unit is as much as 100 ft thick, and it overlies 

the Lexington Limestone and underlies the Kope 

Formation. Cressman (1973, p. 46) made the following comments about the Point Pleasant: 

***At Cincinnati and eastward along the Ohio River, the 

Lexington Limestone and the Kope Formation are separated 

by about 100 feet of limestone and shale, interbedded in 

various proportions but averaging about half-and-half.*** 

The Point Pleasant Formation resembles the Clays Ferry 

Formation in the regular interbedding of limestone and 

shale, and much of the lower part of the Point Pleasant 

cannot be distinguished lithologically from the Clays Ferry 

to the south.*** 
INTRODUCTION A7 

Weiss and others (1965) described the lithology o.f 

the Point Pleasant Tongue in detail. 

The lithologic similarity of the Point Pleasant to 

the Clays Ferry Formation suggests the same depositional envivonment for the former as for the 

latter. 

According to Cressman (1973, p. 46) : "The rocks 

in Gallatin County called Lexington Limestone by 

Brown and Anstey (1968) and Anstey and Fowler 

(1969) should also be termed Point Pleasant." 

Although previously generally recognized as a 

rock unit of formation rank, the Point Pleasant is 

now treated as a tongue of the Clays Ferry Formation by the U.S. Geological Survey and the Kentucky 

Geological Survey (W C Swadley, S. J. Luft, and 

Anthony Gibbons, written commun., 1974; Swadley, 

1975; Swadley, Luft, and Gibbons, 1975). 

DILLSBORO FORMATION 1 

This formation is as much as 325 ft thick. It is 

composed of a sequence of highly fossiliferous argillaceous limestones and calcareous shales that lie between the shale of the lower part of the Kope Formation and the dolomitic limestone of the overlying 

Saluda Formation. Although the greater part of the 

Dillsboro Formation is shale, it contains about 30 

percent limestone, significantly more than is typical 

of the underlying Kope Formation. The lower part of 

the Dillsboro Formation consists of moderately thick 

beds of rubbly weathering argillaceous limestone 

containing abundant shale partings; the upper part 

of the formation c~onsists of thinly interbedded argillaceous limestone and calcareous shale (Brown and 

Lineback, 1966). 

Much of the Dillsboro Formation is similar to the 

Bull Fork Formation and it may have been deposited 

in a similar environment. 

DRAKES FORMATION 

The Drakes Formation ranges from 120 to 150 ft 

in thickness. It is composed of grayish-green dolomitic or limy sparsely glauconitic silty mudstone to 

argillaceous, fine-grained dolomite or dolomitic limestone (Weir, Greene, and Simmons, 1965). On the 

south and east sides of the Jessamine dome the formation is divisible into (ascending) the Rowland 

and Preachersville Members; on the west side of 

the dome the formation is divisible into (ascending) 

the Rowland, Bardstown, and Saluda Dolomite 

Members. 

1 Dillsboro Formation of Brown and Lineback (1 966) herein adopted for 

U.S. Geological Survey usage. 

ROWLAND MEMBER 

This member is from 40 to 60 ft thick and is the 

basal member of the formation. It is chiefly composed of grayish-green dolomitic or limy, sparsely 

glauconitic silty muds.tone. The mudstone is obscurely bedded and W·eather.s to platy fragments a fraction 

of an inch thick and a few inches. across. Many bedding surfaces are covered by ripple marks or mud 

cracks. Fossils are very sparse. 

According to Weir and Peck (1968), their dolomitic mudstone lithofacies, to which the Rowland 

Member belong·s, is interpreted as very shallow 

quiet-water deposits, probably laid down on extensive flats. 

PREACHER:SVILLE MEMBER 

The Preachersville Mem·ber ranges from 55 to 95 

ft in thickness and forms the upper member of the 

Drakes Formation on the east side of the Jessamine 

dome. It is similar to the Rowland Member but contains 10 to 20 percent argillaeeous, fine-grained dolomite of dolomitic limestone in resistant beds, a few 

inches to a few feet thick; commonly the thicker beds 

are near the base of the member (Weir, Greene, and 

Simmons, 1965). 

OTTER CREEK CORAL BED 

Southeast of Lexington, Ky., the base of the 

Preachersville Member is marked by the Otter Creek 

Coral Bed. This unit is a medium-light-gray limestone that weathers light olive gray to medium gray. 

Most of the limestone is medium grained and the unit 

is rich in colonial corals and other fossils. The coral 

bed has a sporadic distribution and ranges in thickness from 0 to 8ft (Simmons. and Oliver, 1967). 

Peterson (1970) noted that the coral layers in the 

Bardstown Member are probably correlatives of the 

Otter Creek Coral Bed. 

BARDSTOWN MEMBER 

Thickness of this member range·s from 12 to 40ft. 

It overlies the Rowland Member and underlies the 

Saluda Dolomite Member on the west side of the 

Jessamine dome. About 90 percent of the Bardstown 

Member consists of fine- to medium-grained, gray to 

greenish-gray muddy limestone that contains scattered to abundant fossils and fossil fragments. Beds 

are discontinuous and lenticular and commonly 1 to 8 

in. thick. About 10 percent of the me·mber is gray bioclastic and coquinoidal limestone composed of whole 

fossils and fossil fragments in a fine-grained to very 

coarse matrix cemented in part by sparry calcite. 

Colonial coral heads are concentrated in two to four 

layers in the middle two-thirds of the Bardstown 
A8 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Member where they may form as much as 50 percent 

of the rock mass (Peter·son, 1970). 

SALUDA DOLOMITE MEMBER (OR SALUDA 

FORMATION IN INDIANA) 

This unit is as much as 25 ft thick and forms the 

top of the Ordovician sequence on the western side of 

the Jessamine dome in Kentucky. It is distinguished 

from the underlying Bardstown Member because the 

fossiliferous limestone of the latter abruptly grades 

into the dolomite of the Saluda at the contact. Generally, the contact must be located by the application 

of dilute hydrochloric acid (Peterson, 1970). 

Both in Kentucky and Indiana the Saluda is characterized by the presence of dolomite (Brown and 

Lineback, 1966), although no·rth of the Ohio River in 

Indiana the Saluda is regarded as a separate formation where it is as much as 60 ft thick. 

The most thorough study of the Saluda is that of 

Hatfield (1968), who ca.me to the following conclusion about its environment of deposition (p. 24) : 

***The coralline zone which essentially surrounds the Saluda 

Formation, records circumscription by a low, broad coral 

bank of the shallow, quiet-water lagoon in which the formation was deposited. The encompassing bank of colonial corals 

isolated the Saluda lagoon from the surrounding open sea, 

allowing evaporation to produce penesalinity in lagoonal 

waters. Inflow of normal marine water through or over the 

coralline barrier replenished water lost by evaporation, but 

such inflow did not prevent frequent exposure of lagoonal 

sediments and attendant desiccation.*** 

HITZ LIMESTONE BED 

Limestone and dolomite are dark gray to olive 

gray, very fine to medium grained, ·silty, laminated in 

part with hackly to blocky fra.cture. Limestone and 

dolomite occur in at least four distinct alternating 

layers 0.2-0.4 ft thick with limestone at bas·e. Interbedded shale is grayish black to dusky brown, carbonaceous, calcareous, strongly fissile. Shale commronly occurs in two beds, one about 0.5 ft thick near 

the base and one 0.2 ft thick near the top (Kepferle, 

1976). 

FAIRVIEW FORMATION 

This formation ranges from 70 to 110 ft in thickness. It consists of closely interbedded limes,tone and 

shale and minor limy siltstone in which no stratum 

is persistently thicker than 1.5 ft. The uninterrupted 

close spacing of the limestone strata in the bulk of 

the formation is a significant lithic property. Limestone makes up 50-60 percent of the formation, is 

mainly gray and chiefly of two types .. Medium.- to 

coarse-grained fossil fragmental limes.tone is do·minant in the lower pa.rt. Fine-grained even-textured 

silty limestone containing few fossils. is dominant in 

the upper p·art. Shale makes up 35-40 percent of the 

forma;tion, is chiefly medium gray, calcareous, and 

silty, and occur·s as partings and thin beds separating limestone beds. Limy siltstone makes up 5-15 

percent of the formation (Peck, 1966; Ford, 1967). 

Osborne (1973) is the most recent author to consider the environment of deposition of the Fairview 

Formation; he noted (p. 145) : 

the Fairview Formation may have been deposited in slightly 

deeper water (lower mechanical energy) than the Kope Formation. There is no available physical or faunal evidence to 

suggest that the Fairview Formation was deposited under 

restricted conditions, therefore the assumed inverse relationship between mechanical energy at the depositional site and 

water depth may be justified.*** 

In the classification of Weir and Peck (1968), the 

Fairview Formation belongs to the planar-bedded 

fossilifer.ous limestone and mudstone lithofacies 

which they noted (p. 168) is probably indicative of 

intermittently wave disturbed sediments deposited in 

more protected, perhaps deeper water. 

Ford ( 1968, p. 1784) commented that: "The Fairview biogenic limestone in southwest Ohio was deposited on shallow shoal banks that were intensively 

populated by * * * marine invert.ebrates." A similar 

environment existed in the central Bluegrass area 

during the time of deposition of the Clays Ferry biogenic limestone·. 

NORTH BEND TONGUE~ 

Ford (1967) defined this unit of the Fairview Formation. He noted (p. 929) : "Both north and west of 

the City of Cincinnati-Delhi Township area, a part 

of the Fairview Formation grades progressively into 

the Wesselman Tongue of the Kope Formation. As a 

consequence, a lower Fairview tongue is separated 

from the main body of the formation. This unit is 

* * * the North Bend Tongue· of the Fairview Formation." At the type section the unit is 12 ft thick. 

GARRARD SILTSTONE 

This unit ranges from 10 to 100 ft in thickness. It 

is chiefly limy siltstone with minor mudstone and 

limestone. The siltstone is gray and very limy when 

fresh. Most beds are 6-24 in. thick; thicker beds are 

commonly contorted. The interbedded mudstone and 

limestone are mostly in lenses a few inches thick and 

a few feet to a few tens of feet long (Weir, Greene, 

and Simmons, 1965) . 

Ford (1968, p. 1784) noted: "Assuming a co·mmon 

origin for the clastic sediment in the Kope and Gar2 North Bend Tongue of Fairview Formation of Ford (1967) herein 

adopted for U.S. Geological Survey usage. 
INTRODUCTION A9 

rard Formations, the northward decrease in particle 

s·ize fro·m silt in the Garrard Siltstone to clay in the 

Kope F;ormation suggests tectonic control of ·sedimentation from :a southerly source area." 

GRANT LAKE LIMESTONE 

This formation is 110 feet thick at its type locality. 

It is chiefly irregularly bedded argillaceous limestone 

and minor interbedded shale. Limestone, which 

makes up 70-90 percent of the formation, is mainly 

medium to light gray and has light-olive-gray mottling. The dominant type of limestone consists of a 

micrograined to medium-grained poorly s1orted argillaceous limestone matrix surrounding jumbled large 

fossil fragments and whole fossils. The beds are 

thin, very irregular, and rubbly weathering. Thin- to 

thick-bedded fine- to coarse-grained well-sorted clastic limestone in even beds oc·ours locally. Gray calcareous shale occurs as irregular partings and thin beds 

separating limestone layers. The Grant Lake is very 

fossiliferous throughout (Peck, 1966). 

In the classification of Weir and Peck (1968), the 

Grant Lake Limes.tone belongs to the nodular-bedded 

fossiliferous limes1tone and mudstone lithofacies 

which they regarded (p. 168) as representing a higher energy environment, possibly wave-agitated 

shoals on the sloping shelf. 

BELLEVUE TONGUE (OR "BELLEVUE LIMESTONE" 

AS USED BY FORD, 1967) 

The thickness of this unit is uncertain because the 

top is often eroded or poorly exposed: it can be 25 ft 

thick. It is a sequence of medium- to thin-bedded 

limestone and shale in which thin-bedded, massive, 

coquinite limestone predominates (Ford, 1967). 

Ford (1967, p. 934) noted th~t the Bellevue thickened to the Slouth and southeast of Cincinnati, Ohio, 

and that it m:ay represent a northweste·rly tongue of 

the Grant Lake Limestone. Luft (1971) mapped the 

unit as the Bellevue Tongue of the Grant Lake 

Limestone. 

HIGH BRIDGE GROUP 

Wolcott, Cressman, and Conn:or (1972) defined the 

High Bridge Group as including (ascending) the 

"Wells Creek Dolomite" (of drillers), Camp Nelson 

Limestone, Oregon Formation, and Tyrone Limestone; that is, all strata between the Knox Group and 

the Lexington Limestone. The "Wells Creek Dolomite" is not expos·ed at the surface, but as much as 

500 ft of the remaining formations are expo·sed in 

the larger river valleys near the center of the J essamine dome. The High Bridge Group oontains the 

oldest rocks exposed in the area of study ( Cress·man 

and Noger, 1976; Whaley, 1973). 

Cressman (1973, p. 9, 10) commented on the environment of deposition of the High Bridge Group: 

"The fine grain size of the carbonates of the· High 

Bridge Group, the abundanc·e of mud cracks in the 

Tyrone Limestone and the Oregon Formation, and 

the presence of algal mats and intraformational breccias, partic•ularly in the Tyrone, indicate· that these 

rocks were deposited as lime mud on tidal flats and 

in shallow lagoons." Cressman and Noger (1976) 

have also studied the environments o.f deposition of 

the High Bridge Group. 

KOPE FORMATION 

In surface exposures the Kope Formation is as 

much as 250 ft thick. The Kope differs from the partly equivalent and somewhat s·imilar Clays Ferry Formation principally in containing more shale; the 

Kope is up to 90 percent shale and generally more 

than 7 5 percent shale, wher.eas the Clays Ferry Formation is 30-60 percent shale. Furthermore shale 

beds 3 ft or more thick are common in the Kope Formation but rare in the Clays Ferry. The interbedded 

limestones of the two formations. are similar (Cressm:an, 1973; Anstey and Fowler, 1969). 

Cressman (1973, p. 46) summarized thoughts on 

Kope deposition: "* * * Conditions were somewhat 

similar to those in which the Clays Ferry Formation was deposited. The dominance of ·shale may have 

resulted fro·m deposition in deeper water or it may 

reflect proximity to the terrigenous source and distance from the carbonate shelf. The absolute depth 

was not great * * * a maximum of 25 m .. " 

Anstey and Fowler (1969) stressed that the Kope 

(called "Eden Shale" by the·m) was probably deposited in deeper quieter water than laterally equivalent carbonate rocks. Ford (1968) suggested tectonic 

control of sedimentation of the Kope from a southerly source area. 

The Kope is divided into (ascending) : 

GRAND AVENUE MEMBER:: 

Ford (1967, p. 925) proposed this name 

':'** for a unit having distinct bulk lithologic characteristics 

within the upper part of the Kope Formation *** In approximately 11 feet of strata each terrigenous unit is no 

more than 2 feet thick and limestone beds are thicker and 

more closely spaced than is typical of the Kope Formation 

*** Compared with the remainder of the Kope Formation, 

the Grand A venue Member shows a lower clastic content and 

higher bedding index.*** 

3 Wesselman Tongue and Grand Avenue Member of Kope Formation of 

Ford 1~67) herein adopted for U.S. Geological Survey usage. 
A10 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Luft (1971) was able to map this unit and noted 

tha.t it ranged from 10 to 13ft in thickness. 

WESSELMAN TONGUE:: 

Ford (1967, p. 928) proposed this name"* * * for 

a unit of Kope lithologic character which has lateral 

equivalents of Fairview lithologic character * * * 

The lower 30-40 feet of the typ·e Fairview Formation * * * grades progressively northwestward into 

rocks of Kope lithologic type [and eventually] 

merges into and cannot be ·separated from the main 

body of the Kope Formation." The Wesselman 

Tongue ranges from 10 to 30 ft in thickness. 

LEIPERS LIMESTONE 

The Leipers Limestone (not shown in fig. 2) is 

120-180 ft thick; it is gray, bluish-gray, and yellowish-gray limestone tha.t weathers gray. The limestone 

is fine to coarse grained, clayey, and irregularly bedded. The formation contains many fossils, especially 

brachiopods (including abundant Platystrophia) and 

bryozoans, which give the rock a nodular appearance. 

In places the formation grades into very calcareous 

shale (Van Horn and Griffitts, 1969). 

LEXINGTON LIMESTONE 

In surface ·exposures., the Lexington Limestone 

ranges fro·m 200 to 300 ft in thickness. It is a heter>ogeneous sequence of mostly bioclastic and fossiliferous limestone and minor shale, underlain by calcilutite of the Tyrone Limes.tone and overlain by interbedded limestone and shale of the Clays Ferry Formation (Cressman, 1973) . The Lexington Limestone 

has 12 na.med members and s·everal named beds 

(listed below in ascending order). The complex 

facies relationships of the members were illustrated 

by Black and MacQuown (1965) and Cressman 

(1973). 

CURDSVILLE LIMESTONE MEMBER 

The Curdsville Limestone Member ranges from 

less than 20 to 40ft thick. It is the basal member of 

the Lexington Limestone and consists of bioclastic 

calcarenite and calcirudite, which is sandy and chert 

bearing in part. Subordinate calcisiltite and irregularly bedded to nodular fossiliferous limestone occur 

(Cressman, 1973). 

Cressman (1973, p. 14) observed that: 

The Cursdville Limestone Member, like the rest of the Lexington Limestone, was deposited in normal marine water as 

shown by the fauna *** The bioclastic calcarenite and calcirudite, crossbedded in part, which makes up much of the 

lower 20 feet of the member was formed in a high-energy 

environment, probably in water above surf base ***; however, the interval also contains beds of calcisiltite, unabraded 

fossils and articulated pelecypods, all indicative of a lowenergy environment. The close interbedding of calcarenite, 

calcirudite, and calcisiltite resulted from frequent changes 

or local variations in energy; the most likely explanation 

of the frequent changes is that the coarser fragments accumulated in small bars whereas finer material was deposited 

in topographic lows. Migration of the bars would have resulted in interbedding of coarser and finer grained sediments. 

The fossiliferous limestone of the upper part of the Curdsville was deposited in slightly deeper water. The currents 

were sufficient to supply oxygen and food but were not 

strong enough to break and. abrade many of the shells*** 

The vertical sequence of rock types in the Curdsville, highenergy shallow-water deposits in the lower part grading to 

deeper water deposits at the top, record a marine transgression * * * 

LOGANA MEMBER 

The Logana Member ranges from 0 to 50 ft in 

thickness; it overlies the Curd ville Limestone Member and underlies or intertongues with the Grier 

Limestone Member. Over much of its outcrop· are·a 

the Logana cons·ists of three major divisions. The 

lower division is interbedded calcisiltite and shale, 

the middle division is mostly a brachiopod coquina, 

and the upper division is calcisiltite and shale similar 

to the lower division (Cressman, 1973). 

Cressman (1973, p. 17) commented as follows on 

the .environment of deposit,ion of the Logana 

Member: 

*** The Logana Member was deposited during the culmination of the initial transgression of Lexington time, and it 

accumulated in deeper water than the calcarenite and fossiliferous limestone of the Curdsville Limestone Member below 

or the fossiliferous limestone of the Grier Limestone Member above. The interbedded calcisiltite and shale accumulated 

below wave base, as shown by the fine grain size and the 

absence of current structure*** 

The oxygen content of the bottom water was low as evidenced by the paucity of fossils, the absence of animal burrows, and the relatively dark color of both the shale and 

the limestone; and the sea floor was probably below the compensation depth *** In the present ocean this depth v;1ries 

greatly, but it ranges from 25 to 45 m in clear coastal 

waters. At least periodically, though, the oxygen content was 

sufficient to permit the· growth of pelecypods found in some 

beds*** 

GRIER LI•MESTONE MEMBER 

This member ranges from 100 to 180 feet in thickness. It overlies the Logana or Curdsville Limestone 

Members and underlies the Perryville Limestone, 

Brannon, or Tanglewood Limestone Members. The 

Grier Limestone Member contains a variety of rock 

types, but the general aspect is of thin and irregularly to nodular-bedded, poorly ·sorted, abundantly 

fio-ssiliferous limestone (Cressman, 1973). 

In discussing the environment of deposition of this 

member Cressman (1973, p. 19) noted: 
INTRODUCTION All 

***The abundance, kind, and state of preservation of the 

fossils and the poor sorting of the limestone indicate that 

most of the Grier Limestone Member was deposited in 

shallow, aerated, only moderately agitated water *** The 

lenticular and nodular beds very closely resemble structure in 

recent sediments that are attributed to churning by burrowing organisms *"'* most of the churning must have been 

by soft-body organisms. 

Currents were sufficient to supply oxygen and food to the 

large fauna of suspension feeders, distribute crinoid_ columnals, and winnow some of the carbonate mud, but they were 

too weak to thoroughly comminute and sort the skeletal 

debris or to remove all of the lime mud *** Much of the 

Grier probably accumulated in depths of less than 15 m 

of water. *"'* 

MACEDON lA BED 

This unit has limited extent, where it is developed 

it is about 115-120 ft above the base of the Grier 

Limestone Member and is as much as 15 ft thick. The 

Macedonia Bed consists of argillaceous calcisiltite in 

even to broadly lensing smooth-surfaced beds 0.2-0.4 

ft thick, interbedded with 10-40 percent shale. It is 

similar to the Logana and Brannon Members and 

was deposited under similar conditions (Cressman, 

1973}. 

CANE RUN BED 

This unit also has limited extent: where it is present it is as much as 5 ft thick and is at the top of the 

Grier Limestone Member. The Cane Run Bed consists of argillaceous calcilutite and calcisiltite with 

abundant chert nodules; contorted bedding is common (Cressman, 1973). 

PERRYVILLE LIMESTONE MEMBER 

This member is as much as 60ft thick. Cress.man 

(1973, p. 23) described the unit as follows: 

***The Perryville Limestone Member of the Lexington Limestone as used herein, includes those beds between the calcarenite of the Tanglewood below and the interbedded calcisiltite 

and shale of the Brannon Member above. The nodular fossiliferous limestone at the top is the Cornishville Bed, the interbedded light-gray and brownish-gray calcilutite is the Salvisa Bed, and the fossiliferous brownish-gray calcilutite is 

the Faulconer Bed. I believe those assignments to be consistent with the original definitions. *** 

Cressman (1973, p. 28) di,scussed the environment 

of deposition of the Perryville as follows: 

*** The depositional environment of the Cornishville Bed 

was similar to that of the Grier Limestone Member. 

Both the Faulconer and Salvisa Beds were deposited in 

shallow quiet water. Shallow water is suggested by the 

fauna in the Faulconer and by the light color of much of 

the Salvisa. The abundant micrite and lack of sorting are 

evidence of lack of turbulence. The fauna of the Faulconer 

Bed would have required marine water of approximately 

normal salinity, but the restricted fauna-ostracodes and 

gastropods-of most of the Salvisa Bed suggest more saline 

water. 

The Perryville Limestone Member is separated from the 

temporally equivalent upper half of the Grier Limestone 

Member to the north by calcarenite. Thus, the shallow quiet 

water· in which the Perryville was deposited was separated 

from the more agitated water to the north by a zone of 

calcarenite bars *** 

J.<~AULCONER BED 

This bed is as much as 40 ft thick and is the basal 

unit of the Perryville Limestone Member. The Faulconer Bed consists of brownish-gray fossiliferous 

calcilutite in rough-surfaced beds commonly about 

0.5 foot thick. Mollusks are the most conspicuous fossils ('Cressman, 1973). 

SALVISA BED 

This unit is as much as 15ft thick and is the middle bed of the Perryville Limestone Member. It consists of interbedded light-gray to light-olive-gray 

calcilutite interbedded with brownish-gray calcilutite. The brownish-gray calcilutite is similar to much 

of -that in the Faulconer, ,and the·Salvisa ~·:is characterized by the light-gray type. Beds are smooth surfaced (Cressman, 1973) . 

CORNISHVILLE BED 

This is the top unit of the Perryville; it is as much 

as 10ft thick and overlies the Salvisa Bed. It is mostly nodular bedded calcisiltite and fine-grained calcarenite containing abundant brachiopods and a few 

bryozoans (Cressman, 1973). 

BRANNON MEMBER 

This member is as much as 30 ft thick; it is underlain by the Perryville Limestone Member and is overlain or interbedded with the Tanglewood Limestone 

Member or the Sulphur Well Member. The Brannon 

Member consists of interbedded argillaceous calcisiltite and shale in nearly equal amounts. The calcisiltite is medium to light gray and i,s generally in 

smooth-surfaced tabular beds 0.2-0.3 ft thick. The 

shale is calcareous and is dark to medium gray in 

fresh exposures. Fossils are sparse in their occurrence. The uppermost beds of the Brannon Member 

are commonly contorted (Cressman, 1973). 

Cressman (1973, p. 37) wrote of the depositional 

environment and noted that it was similar to that of 

the Logana Member. He suggested "that the depth of 

the water was mostly below wave base and below the 

compensation depth which is assumed to have been 

about 25m. Periods of greater turbulence winnowed 

fine bioclastic debris from shallower areas, and the 
A12 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

winnowed material was deposited in the deeper 

water to form the calcilutites." 

SULPHUR WELL MEMBER 

This member is as much as 35ft thick and is ·bryozioan limestone in irregular to lenticular beds that 

are separated by thin shale beds and partings. The 

limestone is mOtstly poorly sorted bryozoan calcirudite containing much silt- and clay-sized calcite and 

dolomite matrix. The shale contains closely packed 

bryozoan fragments (Cressman, 1973). The Sulphur 

Well Member is underlain by the Brannon, Perryville Limestone, Grier Limestone, or Tanglewood 

Lim.estone Members and is overlain by the Clays 

Ferry Formation. 

Cressman (1973, p. 37) di,scussed the environm.ent 

of deposition of the Sulphur Well Member: "The 

Sulphur Well Member was deposited under conditions similar to those described for the Grier Limestone Member. It accumulated below surf ba,se, 

mostly at depths ·of less than 15 m, in moderately 

turbulent normal marine water. It is uncertain what 

environmental fac,tors caused the great abundance of 

bryozoans." 

STAMPING GROUND MEMBER 

This unit is as much as 15 ft thick. Lithologically 

it is similar tn the Millersburg Member and the 

Greendale Lentil, being composed of fossiliferous 

nodular limestone and shale. The Stamping Ground 

Member is stratigraphically lower than the Millersburg Member and is both underlain and overlain by 

calcarenite of the Tanglewood Limestone Member. 

The depositional environment was similar to that of 

the Millersburg Member (Cressman, 1973). 

GREENDALE LENTIL 

This unit is 10-15 ft in thickness. Lithologically it 

i·s similar to the Millersburg Member cons.isting of irregularly bedded to nodular fossiliferous limestone 

and shale. About 75 percent of the unit is limes.tone 

and 25 percent is shale. However, the Greendale Lentil is not continuous with the Millersburg Member; 

it grades laterally in all directions into the Tanglewood Limestone Member (Cressman, 1973). 

DEVILS HOLLOW MEMBER 

This member ranges from 0 to 30 ft in thickness. 

I,t overlies or is interbedded with the Tanglewood 

Limestone Member and underlies the Millersburg 

Member. It consists of two distinctive lithologies, a 

coquina phase and a fine-grained phase. At the type 

locality the lower part consists of porous coarsely 

crystalline light-gray massive limestone containing 

a crowded mass of gastflopod shells overlain by compact limestone (calcilutite) similar to that of the 

Tyrone Limestone and containing ostracodes. These 

two flock types intertongue, and the member may 

consist locally entirely of the calcilutite, entirely of 

the gastropod coquina, or of both types ( Cres,sman, 

1973). 

Cressman (1973, p. 41) noted that: 

*** The calcilutites of the Devils Hollow Member *** were 

deposited at depths of less than a few meters in quiet protected waters of relatively high salinity. The association of 

gastropodal calcirudite with the calcilutite suggests an intertidal environment that had extensive algal mats on which 

gastropods fed; but I have seen no mudcracks or intraformational breccias, and most of the laminated beds do not closely 

resemble those known to be of algal origin. Therefore, the 

calcilutite probably accumulated as very shallow subtidal 

banks as pelletal lime mud and fossil debris *** The gastropodal calcirudite probably accumulated on beaches or possibly in channels between banks. The areal distribution of 

the Devils Hollow Member indicates that the sediments 

formed a narrow *** lagoon *** 

MILLERSBURG MEMBER 

This member ranges fro•m 0 to 90ft thick; it ~verlies and intertongues with the Tanglewood Limestone Member. The Millersburg is characterized by 

nodular bedding of the limestone, abundant whole 

and broken fossils, s.ilt- and clay-sized carbonate 

matrix, and abundant shale (Cressman, 1973). 

In discussing the environment of deposition of this 

member Cressman (1973, p. 43) observed: 

*** The abundance of unbroken fossils, poor sorting, the 

abundance of lime mud, and the large amount of shale suggest that most of the Millersburg was deposited in water of 

only moderate turbulence. The abundance of fossils suggests 

that much of the Millersburg *** was formed at depths of 

less than 15 m. 

The abundance of shale, as compared with the small 

amount in the otherwise similar fossiliferous limestone facies, 

may have resulted from a larger supply of mud in later 

Lexington time * * * 

The nodular structure typical of the Millersburg Member 

resulted from burrowing by a dominantly soft-bodied 

infauna *** 

STRODES CREEK MEMBER 

This member is as much as 30 ft thick and is 

probably a lens within the Millersburg Member. It is 

readily recognized by its bouldery aspect attributable to a combination of pinch-and-swell bedding, 

ball and pillow structure, and bulbous stromato-· 

pofloids. The rock is chiefly limestone with minor 

amounts of gray to reddish-brown fissile shaly argillaceous calcisiltite as partings and in places a.s beds. 

The dominant limestone type is moderate-grayishbrown to gray dense nonfissile rock having the tex-
INTRODUCTION A13 

tural characteristics of a mudstone. It is composed 

mostly of clay- and silt-sized calcite particles and 

commonly contains disseminated rounded mediumto co,arse-sand-sized fossil fragments; fractured surfaces are smooth and subconchoidal (Black and Cuppels, 1973). 

Black and Cuppels (1973) 0ompare the lithology 

of the Strodes Creek Member to that of the Faulconer Bed of the Perryville Limestone Me,mber and 

part of the Devils Hollow Member; it may have developed in a similar depositional environm.ent. 

TANGLEWOOD LIMESTONE MEMBER 

In general this member is between 60 and 100 feet 

thick, it is an extensive irregular body of bioclastic 

calcarenite that makes up much ·Of the upper part of 

the Lexington Limestone. The Tanglewood Limestone Member typkally consists of pinkish-gray 

medium-grained well-sorted bioclastic calca·renite. 

Beds are mostly 0.2-1 ft thick and are generally 

smooth surfaced and planar to wavy. Many beds contain alternating more o·r less phoS'phatic laminae 

from less than 1 to 5 mm thick. Low-angle, small- to 

medi urn-scale crossbedding is common ( Cressm·an, 

1973) 0 

Cressman (1973, p. 31) co·mmented on the envil'lonment of deposition: 

*** The broken and rounded skeletal fragments, the generally good sorting, the abundant sparry calcite cement, the 

lack of clay and silt, and the common crossbedding all indicate that the bioclastic calcarenite of the Tanglewood Limestone Member was deposited in very shallow, turbulent 

water ':'** The organic material was brought in from elsewhere-presumably from less agitated water where the 

Grier Limestone and Millersburg Members were accumulating 

-and was broken, abraded, and sorted in the area of the 

calcarenite deposition *** 

NICHOLAS BED 

This name is applied to the upper tongue of the 

Tanglewood Limestone Member north and northeast 

of Lexington, Ky. The unit is as much as 80 ft thick 

and cannot be distinguished lithologically from the 

rest of the member (Cressman, 1973). 

MIAMITOWN SHALE 4 

This formation was proposed by Ford (1967) ; it 

is as much as 35 ft thick in Ohio but is not distinguishable in northern Kentucky. Ford (1967, p. 

931) defined the unit as follo-ws: 

*** The name Miamitown Shale is proposed here for the 

thin shale that overlies the Fairview Formation. It consists 

of shale and mudstone with a few thin, widely spaced lime4 Miamitown Shale of Ford (1967) herein adopted for U.S. Geological 

Survey usage. 

stone interbeds. The limestone contains a high proportion of 

terrigenous detritus and a diagnostic gastropod-pelecypod 

faunal assemblage *** Nodular bedding is common *** 

Lithologically the Miamitown Shale represents a return to 

conditions of Kope deposition. *** 

OREGON FORMATION 

The Oregon Formation overlies the Camp Nelson 

Limestone and is as much as 60 ft thick. The formation is characterized by finely crystalline calcareous 

dolomite (Cressman, 1973). See High Bridge Group. 

TYRONE LIMESTONE 

The Tyrone Limestone overlies the Oregon Formation and ranges fro-m 60 to 100 ft in thickness. The 

Tyrone i.s typically calcilutite, though in places it 

contains much interlaced dolomite. Mud cracks occur 

throughout the form·ation (Cressman, 1973) . See 

High Bridge Gro-up. 

WHITEWATER FORMATION 

This unit is as much as 85 ft thick and forms the 

top of the Ordovician sequence in southeastern Indiana; it overlies the Saluda Formation. Brown and 

Lineback (1966) defined the formation as follows.: 

*** A variety of limestone types interbedded with calcareous 

shale constitutes the Whitewater. Among the limestone types 

are thin-bedded fossiliferous argillaceous limestone, thinbedded ostracoda! limestone, medium-bedded relatively unfossiliferous limestone, medium-bedded limestone with burrows, 

and rubbly weathering argillaceous limestone. In general, the 

Whitewater contains more limestone than most parts of the 

Cincinnatian below the Saluda.*** 

Fox (1962, p. 640) co·mmented on the depositional 

environment of the Whitewater Formation : 

"*** Earthy limestone members of the Whitewater were 

laid down on submerged, calcareous, mud flats analogous to 

those west of Andros Island on the Bahama Banks." 

MIDDLE ORDOVICIAN-UPPER ORDOVICIAN 

BOUNDARY 

Between 1959 and 1974, faculty and students at 

the Ohio State University Department of Geology, 

along with colleagues at other institutions, have produced a 19-p·art s~tudy of the American Upper Ordovician Standard sequence of rocks (Cincinnatian 

Series) expos.ed in southwestern Ohio and adjacent 

st1ates (Sweet and others, 1959; Weis~s and Norman, 

1960a, b; Pulse and Sweet, 1960; .Weiss, 1961; Carpenter and Ory, 1961; Weiss and others, 1965; Osborne, 1967, 1968, 1969, 1970, 1971a, b; 1973; Kohut 

and Sweet, 1968; Sweet and Bergstrom, 1971; Booth 

and Osborne, 1971; Lobo and Osborne, 1973; and 

Sweet and others, 1974). This study by Ohio State 

University has largely ooncenira.ted on the conodont 
A14 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

biostratigraphy and the sedimentary petrology of 

. the Cincinnatian rocks, but has also dealt with lithostratigraphy and environmental interpretations of 

the rocks. 

Because the Cincinnatian Series is the American 

Upper Ordovician Standard, any rocks that can be 

correlated with this standard are by definition Late 

Ordovician in age. The Cincinnatian Series is divided into three stages, Edenian, Maysvillian, and 

Richmondian in ascending order. In central Kentucky and along the Ohio River are surface exposures of rocks older than Edenian, and it is a matter of deciding where the Middle Ordovician-Edenian boundary falls in these areas. 

Except for conclusions drawn from conodonts 

(Bergstrom and Sweet, 1966; Sweet and Bergstrom, 

1971; Ethington and Sweet, 1977; Sweet, herein), 

little has been published in recent years about the age 

of the Ordovician rocks below the Edenian in the 

area of study. Bucher, Caster, and Jones (1939) 

placed the Mohawkian-Cincinnatian (Middle Ordovician-Upper Ordovician) boundary at Cincinnati, 

Ohio, at the top of the Point Pleasant or River Quarry Beds, which they placed in the "Cynthiana Formation." The base of their Edenian was the Triarthrus 

fauna of the Fulton Beds in what they called the 

"Utica Formation." Their Mohawkian-Cincinnatian 

boundary is essentially equivalent to the Middle Ordovician-Upper Ordovician boundary as used by 

earlier workers (Weiss and Norman, 1960a). Although Caster, Dalve, and Pope (1955, 1961) included the Point Pleasant in the Cincinnatian Series 

(Upper Ordovician) , they did not assign this formation to any stage. They did indicate that Point 

Pleasant beds were older than Edenian, and that they 

belonged to the "Cynthiana Formation." 

Twenhofel and others (1954, correlation chart, 

column 45) placed all of the Ordovician rocks of 

southwestern Ohio, northern Kentucky, and southeastern Indiana in the Cincinnatian Series and regarded all of them as Late Ordovician in age. They 

placed what they called the "Cynthiana Formation" 

of this area in the Edenian (early Late Ordovician) 

Stage. These same workers (correlation chart, column 44) regarded what they called the "Cynthiana 

Limestone" of central Kentucky as crossing the Middle Ordovician-Upper Ordovician boundary. The 

name "Cynthiana Formation" is no longer used py 

the U.S. Geological Survey (Cressman, 1973). The 

beds exposed along the Ohio River formerly assigned 

to this unit are now placed in the Point Pleasant 

Tongue of the Clays Ferry Formation. In central 

Kentucky the name "Cynthiana Formation" was 

used for rocks now placed in the lower part of the 

Clays Ferry Formation and upper part of the Lexington Limestone. 

Bergstrom and Sweet (1966), Karklins (in Cressman and Karklins, 1970), and Sweet and Bergstrom 

(1970) showed that the upper part of the Lexington 

Limestone at its reference section in central Kentucky correlates with the Edenian-age rocks exposed 

around Cincinnati, Ohio. Sweet and Bergstrom 

(1970) suggested that south of Frankfort, Ky., and 

near Clays Ferry, Ky., the upper 70-80 feet of the 

Lexington Limestone correlate with the lower 70-80 

feet of the Kope Formation at Cincinnati, Ohio, and 

are thus Edenian in age. They noted (1970, p. 242): 

"* * * [that] southeastward from Cincinnati the contac-ts between lithic units rise with respect to those 

between conodont-biostratigraphic units." Karklins 

(in Cressman and Karklins, 1970, p. 21) indicated 

that bryozoans of Upper Ordovician aspect occur as 

low as the upper part of the Brannon Member of the 

Lexington at the reference section of the latter formation. As indicated by Cressman (1973) this is 

approximately 100ft below the top of the Lexington 

Limestone. 

Sweet and Bergstrom ( 1971) summarized all of 

the recent biostratigr~phic information available on 

the Middle Ordovician-Upper Ordovician boundary in 

the area of study, particularly with reference to the 

Kope Formation, Lexington Limestone, and Clays 

Ferry Formation, all of which are at or cross this 

boundary. Their fi·gure 2 ( 1971, p. 616) summarized 

their conclusions of the ages of the formations 

throughout the area of this work. In central Kentucky both the Lexington Limestone and the Clays 

Ferry Formation cross the Middle Ordovician-Upper 

Ordovician boundary, although toward the southeast 

the Lexington Limestone is entirely Middle Ordovician in age. The Point Pleasant Tongue of the Clays 

Ferry and the Kope Formation are not shown to be 

older than Edenian (early Late Ordovician), although the Kope Formation ranges upward into 

Maysvillian time (middle Late Ordovician). Sweet 

(1979) (fig. 3) indicates that the Point Pleasant 

Tongue crosses the Middle Ordovician-Upper Ordovician boundary. Thus, all rock units above the Kope 

Formation, Point Pleasant Tongue of the Clays Ferry 

Formation, Clays Ferry Formation, and much of the 

Lexington Limestone are Late Ordovician in age. 

For outcrops of the Clays Ferry Formation, its Poi.nt 

Pleasant Tongue, and the Lexington Limestone, it is 

necessary to determine where the boundary is, although the general ·picture is that the top of the 
INTRODUCTION A15 

Lexington Limestone (bottom of the Clays Ferry 

Formation) 

*** becomes younger southeastward from the northwestern 

part to the center of the Cincinnati Region, then older toward the southeastern part of the area of exposure. These 

correlat' viiS also indicate that, in the central Cincinnati 

Region *** Frankfort Lexington-Cynthiana, Kentucky, area 

*"'"' and at least as far northeast as southern Clermont 

County, Ohio *** the uppermost 21 to 24 m of the Le·xington Limestone is Edenian in age, for this part of the Lexington correlates very well with the lower 21 to 24 m of 

the Kope Formation at Cincinnati *** and the Kope Formation in Cincinnati is the reference standard for the North 

American Edenian Stage *** (Sweet and Bergstrom, 1971, 

p. 619). The lower part of the Lexington Limestone and all 

rock units below it are Middle Ordovician in age. 

OTHER BIOSTRATIGRAPHIC BOUNDARIES 

Sweet and Bergstrom (1971) indicated that the 

top of the Shermanian St:age of New York is at essentially the same stratigraphic level as the bottom 

of the Edenian Stage of Ohio, Indiana, and Kentucky 

and that much of the classical Trentonian Stage 

overlaps. the basal Cincinnatian Series. They suggested (p. 624) that the Shermanian-Edenian boundary be used as the boundary between the Champlainian and Cincinnatian Series, that is as the 

Middle Ordovician-Upper Ordovician boundary. 

They further reco-mmended that the upper Champlainian and Cincinnatian Series be divided into six 

stages : Rocklandian, Kirkfieldian, Shermanian, 

Edenian, Maysvillian, and Richmondian in ascending 

order. In 1974 (p. 194), Sweet and Bergstrom indicated that for the stage below the Rocklandian the 

name Blackriveran be maintained. 

In the interval from the Blackriveran through the 

Richmondi·an Sweet and others (1971) and Sweet 

and Bergstrom (1974) reco·gnized their conodont 

faunas 7 through 12 based on the North American 

midcontinent sequence. In the same interval, Bergstrom (1971) and Sweet and Bergstrom (1974) 

recognized three conodont zones based on the Appalachian and European sequences. Sweet and Bergstrom (1971, fig. 2) placed the Middle Ordovician 

portion of the Lexington Limestone in the Kirkfieldian and Shermanian Stages. Thus, the Lexington 

Limestone ranges in age from Kirkfieldian to Edenian and contains conodont faunas 9 to 11 of Sweet 

and others (1971) and Sweet and Berg,stro·m 

(1974); it is late Middle and early Late Ordovician 

in age. 

The conodonts of rocks below the Lexington Limestone have been little studied to date, and Sweet and 

Bergstrom (1971) did not assign any of the High 

Bridge Group to a particular stage; they merely indicated that it is pre-Kirkfieldian in age and that the 

Tyrone Limestone is separated from the Lexington 

Limestone by an unconformity. Cressman (1973, p. 

12, 13) discussed the disconformity between the Tyrone Lmestone and the Curdsville Limestone Member of the Lexington Limestone and came to the 

conclusions that little or none of the Curdsville could 

be the time equivalent of the uppermost part of the 

Tyrone, and that the Tyrone-Lexington disconformity probably does not indicate any great interval of 

time. Twenhofel and others (1954) placed the Camp 

N:elson Lim·estone in the Blackriveran Stage and correlated the Oregon Formation and Tyrone Limestone 

with the Rockland Limestone of New York State 

usage. Cooper (1956) placed the High Bridge Group 

in the Wildernessian correlating it with the Rockland and Hull Limestones of New York State and 

Ontario, Canada. Sweet (1979) (fig. 3) places the 

Tyrone Limestone in the Kirkfieldian Stage. 

In summary, based largely on the work of Sweet 

and Bergstrom (1971, fig. 2; and Sweet, 1979, fig. 3) 

the outcropping formations in the are:a of study can 

be assigned to the following Middle and Upper Ordovician stages. The High Bridge Group forms the oldest part of the succession and i~s probably Blackriveran, Rocklandian, and Kirkfieldian in age; a disconformity marks the top of the High Bridge Group, but 

it probably does not represent a significant time gap. 

The Lexington Limestone ranges in age fro·m. Kirkfieldian to Edenian. The Clays Ferry Formation including the Point Pleasant Tongue ranges. in age 

from Shermanian to Edenian. The Kope Formation 

at Cincinnati, Ohio, is entirely Edenian in age, although east and west of this city the upper part of 

the Kope is Maysvillian in age. The Garrard Siltstone may span the Edenian-Maysvillian boundary, 

although Sweet (1979) (fig. 3) regards it as Edenian 

in age. The Calloway Creek Limestone is entirely 

Maysvillian in age as is the Fairview Formation 

throughout most of its outcrop; the lower part of the 

latter unit is Edenian in age near Cincinnati, Ohio. 

The Grant Lake Limestone is largely Maysvillian in 

age, although near Maysville, Ky., the upper part of 

this unit i's Richmondian in age. The Dillsboro Formation ranges in age from Maysvillian to Richmondian. The Saluda Formation, Whitewater Formation, Bull Fork Formation, and Drakes F·ormation are all Richmondian in age. The Ashlock Formation is Maysvillian and Richmondian in age. 

MATERIALS AND METHODS 

The bulk of the fossils described here are from 

nearly 1,100 collections made between 1961 and 1972. 
Al6 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

INDIANA 

I 

I ,--...,./ 

/ 

• 

11~1!! 

r' 

I 

I 

I 

I 

I 

I 

~', 

\ , 

, 

OHIO 

KENTUCKY 

I 

, ... ./' 

~ 

, .. _.. .... ~VIRGINIA ------·:·.·._·: ------------------------------~-----------------

TENNESSEE 

10 20 I I 

I 

10 

30 40 50 KILOMETERS 

II I II 

20 30 MILES 

FIGURE 3.-Index to 7 .5-minute quadrangles in the study area from which fossil collections were made. 

Pattern indicates quadrangles whose collections are discussed in chapters of this report. 
INTRODUCTION A17 

About 30 of these collections are from Ohio and Indiana, the rest being from the State of Kentucky. Altogether, collections were made from 87 7.5-minute 

quadrangles (fig. 3). Although all Ordovician formations in the tristate area of Kentucky, Ohio, and 

Indiana were ~sampled for fossils, the bulk of the collections represent three rock units : High Bridge 

Group, 92 collections; Clays Ferry Formation, 186 

collections; and Lexington Limestone, 519 collections. Only those collections specifically cited in the 

paleontological chapters of this report are listed in 

the locality register. 

Early in the collecting program it was discovered 

that silicification of fossils is widespread in the Ordovician rocks of Kentucky, and the bulk of the 

megafossils described is from ·over 200 collections 

having silicified fossils; whether or not a collection 

contained silicified fossils. is noted in the locality 

register. Although each formation in the area of outcrop wa1s examined for the presence· of silicified fossils, most of the silicified specimens are from the 

Lexington Limestone, which has the mo·st widespread silicification both stratigraphically and geographically. Altogether nearly 36,000 pounds of limestone containing silicified fossils was collected. From 

the High Bridge Group we collected 4,576 pounds of 

limestone containing silicified fossils from 25 localities. There were 116 collections, totalling 22,261 

pounds, from the Lexington Limestone containing 

silicified fossils. From the rock units above the Lexington LimestiOne we had 64 collections, totaling 

8,875 pounds, which contained silicified fos·sils. After 

preparation, about 180,000 specimens o.f silicified 

fossils were available for study; these included 

sponges, solitary and colonial corals, bryozoans, 

brachiopods, bellerophonts, other m·onoplacophorans, 

cephalopods, gastropods, pelecypods, polyplacophorans, scaphopods, hyoliths, cnrnulitids, ostracodes, 

trilobites, a~teroids, "carpoids," crinoids, edrinasteroids, other echinoderms, and receptaculitids. The 

three most abundant groups in numbers of specimens were: brachiopods, nearly 90,000 specimens; 

mollusks, more than 55,000 specimens; and bryozoans, nearly 19,000 specimens-. 

It took a great deal of time to acid etch the large 

vo-lume of rock involved and to sort and pick the 

specimens once they were released from the matrix. 

The techniques used to free silicified fossils from the 

limes-tone were largely those developed by G. A. 

Cooper and R. E. Grant, of the National Museum of 

Natural History, in their work on the silicified Permian faunas of west Texas (Cooper and Whittington, 1965). 

The first large-scale acid etching of Kentucky Ordovician limestones was done by R. B. Neuman of the 

U.S. Geological Survey in the early 1960's. In 1965, 

E. L. Yochelson of the U.S. Geological Survey and 

I sampled numerous Ordovician localities in the inner Blue Grass region of Kentucky to determine the 

extent and quality of the silicification of the Ordovici'an fossils of the area. The results of these preliminary samplings indicated that large numbers of 

whole well-silicified fossils could be obtained from 

the Ordovician rocks of Kentucky. From 1966 

through 1972 the bulk of the 36,000 pounds of rock 

was collected and processed in the laboratory. 

After identifying a bed containing silicified fossils 

in the field one has to pry out the largest blocks of 

limestone possible to insure a maximum. number of 

whole specimens for study. After the Ordovician 

blocks were collected, they were wrapped in newspaper, placed in burlap sacks, and shipped to the 

laboratory by motor freight ·as broken rock. After 

the blocks of limestone arrived at the laboratory, the 

first step in processing them was to wash and weigh 

them. After weighing, the underside of the blocks 

were coated with an acid-proof resin so that upon 

etching in add the blocks would only etch from the 

top down and the sides in. If a block were also to 

etch from the bottom up eventually a central core of 

limestone would rema,in, resting on fragile silicified 

fossils below; such a core could collapse and crush 

the fossils below it. 

Once the resin was dry, thP. blocks . of limestone 

were placed in acid-impervious vats of appropriate 

size on a screen made of Mo·nal Metal nr plastic. The 

screen allowed day- and sand-sized particles to be 

washed through it; as fossils etched free from the 

matrix they collected on the screen and could be 

removed en masse by lifting the screen from the vat. 

Ordinarily the screen was placed on top of l-inchthick granite slabs so that the fine insoluble particles released by the etching would not bury the base 

of the limestone block and stop the etching process. 

Once the block o.f limestone was on the screen and 

granite slabs, the block was covered with water and 

enough acid was added to ·create about a 10-percent 

solution of commercial-grade hydrochloric (muriatic) acid. 

Most of the acid etching was done with co.mmercial-grade hydrochloric acid, because i1t is relatively 

cheap and can be readily obtained. However, the 

smaller collections and a sample (usually 25 pounds) 

of larger collections were etched in com.mercialgrade glacial acetic acid to preserve the fossils composed of calcium phosphate. For the first 14,097 
A18 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

pounds of rock etched, we used 2,416 American gallons of acid (2,137 gallons of hydrochloric acid and 

279 gallons of acetic acid) ; this gives an average 

yield of about 6 pounds of rock per gallon of fullstrength acid. 

Once the limestone matrix was. etched away, the 

screen on which the free silicified fossils rested was 

rem•oved from the vat. Sometimes it was necessary to 

slide plexiglass or masonite under the s-~reen to prevent it from collapsing from the weight of the silicified fossils and crushing some of the specimens. 

After a time it became standard practice to place the 

,._.plexiglas'S" or m·asoriTte under the screen before etching of the block began. If there were a significant 

component of clay-sized particles in the blnck being 

etched, these tended to coat the surface being e·tched 

and inhibit or stop the etching process. The clay was 

difficult to remove without damaging specimens already partially freed from the matrix. So,metimes 

the clay particles oould be successfully remo-ved with 

careful scrap~ing or brushing or with a gentle spray 

of water. Blocks with a significant clay or silt content 

were difficult to prepare and took considerably longer 

to etch to completion than did blocks which lacked 

these p1article sizes. 

After the matrix was completely etched away, the 

screen with the silicified fossils was removed from 

the acid vat, and residual acid on the· specimens 

washed away. This was done in a tank of slowly running water in which the specimens and the screen 

were completely immersed ; ordinarily collections 

were left washing in the tank overnight. One could 

readily det·ermine if all of the residual acid had been 

washed away by the odor of the sample, by an olivegreen color which developed on drying specimens 

which still had residual hydr10chloric acid, or by the 

growth of calci urn acetate crystals on specimens 

etched in acetic acid. Once all o.f the residual acid 

was washed away, the screen with the silicified specimens was allowed to dry ; ordinarily our specimens 

were air dried, but various types of heated compartments can be constructed to speed the drying process. It is critically important that specimens be completely dried before they are picked and sorted or 

handled in any way. The specimens are far stronger 

and weigh less when dry than when wet. 

Sometimes when a s~creen was removed from a. vat 

after dissolution of the matrix, the specimens would 

be covered or buried in sediment of fine particle size. 

This clay- and silt-size sediment must be removed 

before drying the specimens ; otherwise the sediment 

would harden around the specimens and it would 

not be pos-sible to remove them from the screen. The 

easiest and quickest way to remove this fine sediment was to slowly wash it through the screen with 

a gentle spray or stream of water, taking care that 

the stream of water was not so strong as to damag·e 

the specimens. 

The length of time it takes to acid etch a sample is 

a function of the type of acid being used, the size of 

the block being etched, and the amount of clay and 

silt in the sample. Hydrochloric acid is cheaper and 

works more rapidly than does acetic or monochloracetic acid, but it destroys the phosphatic fossils. 

Formic acid combines the best features of the above 

acids, but is more expensive than acetic acid, and is 

highly oorrosive to flesh; great care must be taken 

in handling formic acid. The smaller the block being 

etched, the greater its surface area to its volume· and 

the faster it will etch. However, the smaller the block 

the fewer specimens. it will contain and all those 

along the broken edges o.f the block will not be whole·. 

As mentioned above, sediment of fine particle size 

will adhere to the surfac-e being etched and inhibit or 

completely prevent the acid from reaching the calcium carbonate. When effervescence stops, because the 

acid in the vat has been used up, it is not sufficient to 

simply add more acid. Calcium chloride buildup in 

the solution (or impurities in commercial-grade 

acids) will eventually prevent the reaction. After the 

acid has been used up it is necessary to siphon off 

the brine and then add fresh water and acid. 

Once the sample is dry, the insoluble residue must 

be removed from the screen. For fossils which are 

too large to be handled with a camel's-hair brush, it 

is best to use a pair of tweezers made fro-m W!atch 

spring, which allow a genUe but firm hold at their 

tips. At the time the specimens are picked from the 

screen it is also best to sort them biologically. At this 

point it may also be desirable to harden the fossils 

with a solution of an acetone-soluble resin. Hardening decreases the fragility of the specimens; it is 

accomplished by dipping the specimens into the 

solution, placing them on a paper towel, and allowing 

them to air dry. To reduce the acetone fumes, this 

procedure is best done in a chemical hood. The procedures should be used with very fragile material, but 

many specimens, if handled carefully, do not require 

hardening. A point to consider is that hardening of 

the fossils sometimes produces a surface sheen that 

makes them difficult to photograph. 

Throughout the acid-etching process one is dealing 

with potentially injurious chemicals and care must 

be taken to have the basic safety equipment of any 

chemicallaborato·ry: it is absolutely essential to have 

adequate ventilation for the etching and hardening 
INTRODUCTION A19 

processes, to have and use safety goggles and rubber 

aprons and gloves, and to have and maintain a shower with a strong stream of water in the laboratory. 

LOCALITY REGISTER 

Although fossils were collected from nearly 1,100 

localities, this register includes information on only 

the 317 localities from which the specimens described 

in the paleontological sections of this report were 

collected. The 317 localities occur in 55 quadrangles; 

most of these are in the S.tate of Kentucky, although 

some of them span the Kentucky-Ohio border, and 

three quadrangles are entirely in the State of Indiana 

(fig. 3). 

The localities are arranged sequentially by the collection number assigned to each in the U.S. Geological Survey register of Cambrian and Ordovician 

localities (-CO) . This sequence is also approximately 

the order in which the collections were made betw·een 

1961 and 1972. The letter D before a collection number indicates that this number is entered in the U.S. 

Geologic'al Survey 'Cambrian and Ordovician locality 

register kept in Denver, Colo. All other collections 

are entered in the USGS Cambrian and Ordovician 

locality register kept in Washington, D.C. An asterisk after a collection number indicates that the 

locality is published on a 1 : 24,000-scale geologic 

quadrangle map of the area where the collection was 

made. 

I have indicated each locality geographically and 

with a set of coordinates. The coordinates are given 

in millimeters, measured first east and then north 

from the lower left corner of the 1:24,000 quadrangle map on which the locality occurs. Thus, locality 4072-CO is 153 mm east of the southwest corner 

of the Tyrone, Ky., quadrangle and 99 mm north of 

the 153 mm mark. In addition to the locality information, the following data are provided for each 

collection: the formation or member f~om which the 

collection was made, any available data on the 

stratigraphic position of the collection within the 

formation or section being collected, whether or not 

the collection was silicified, the weight (where 

known) of each silicified collection, and the name of 

the quadrangle in which the collection was made. A 

number of the collections are from measured sections 

that have been designated by names and numbers; 

where such data are available they are listed. The 

names and numbers of all measured sections are kept 

at the USGS offices in Lexington, Ky. 

Collection number _____ 4072-CO*. 

Geographic location ____ Proceed east 0.75 mi from Milner, 

Ky., and turn .right (southwest) 

on Shryock Ferry Road. Continue 

down Shryock Ferry road about 

1 mi. to top of section . 

Coordinates ___________ 153 mm east, 99 mm north (base of 

section at 134 mm east, 87 mm 

north). 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 154 ft above the base of the Curdsville Limestone Member, Lexington Limestone·. 

Silicified --------------Yes 

Quadrangle name------Tyrone, Ky. 

Section name ---------Tyrone A. 

Section number ________ 89. 

Collection number _____ 4073-CO*. 

Geographic location ____ The same as for 4072-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lextngton 

Limestone. 

Stratigraphic position __ 148 ft above the base of the Curdsville Limestone Member, Lexington Limestone. 

Silicified --------------Yes (1,160 lbs). 

Quadrangle -----------Tyrone, Ky. 

Section name ----------Tyrone A. 

Section number ________ 89. 

Collection number _____ 4075-CO*. 

Geographic location ____ The same as for 4072-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 133 ft above the base of the Curdsville Limestone Member, Lexing-. 

ton Limestone. 

Silicified --------------Yes. 

Quadrangle -----------Tyrone, Ky. 

Section name ----------Tyrone A. 

Section number ________ 89. 

Collection number _____ 4122-CO*. 

Geographical location __ The same as for 4072-CO. 

Coordinates ___________ 134 mm east; 87 mm north. 

Formation ____________ Curdsville Limestone· Member, Lexington Limestone. 

Stratigraphic position __ 16 ft above the base of the Curdsville Limestone Member, Lexington Limestone. 

Silicified --------------Yes. 

Quadrangle -----------Tyrone, Ky. 

Section name ----------Tyrone A. 

Section number ________ 89. 

Collection number _____ 4123-CO*. 

Geographic location ____ The same as for 4072-CO. 

Coordinates -----------The same as for 4122-CO. 

Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ 12 ft above the base of the Curdsville Limestone Member, Lexington Limestone. 

Silicified --------------Yes. 
A20 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Quadrangle -----------Tyrone, Ky. 

Section name ----------Tyrone A. 

Section number ________ 89. 

Collection number _____ 4124-CO. 

Geographic location ____ ·From east side of Blackburn Memorial Bridge crossing of Kentucky River take first road north 

toward Kentucky Utilities Plant; 

section in railroad and road exposures. 

Coordinates ___________ 108 mm east, 197 mm north (road 

exposures) . 

Formation ____________ Logana Member, Lexington Limestone. 

Stratigraphic position __ 12 ft above base of Logana Member, 

Lexington Limestone 

Silicified --------------Yes. 

Quadrangle -----------Tyrone, Ky. 

Section name ----------Tyrone C. 

Section number ________ 174. 

Collection number _____ 4125-CO. 

Geographic location ____ The same as for 4124-CO. 

Coordinates ----------- Do. 

Formation ____________ Logana Member, Lexington Limestone. 

Stratigraphic position __ 7 ft above base of Lagana Member, 

Lexington Limestone. 

Silicified --------------Yes. 

Quadrangle -----------Tyrone, Ky. 

Section name ----------Tyrone C. 

Section number ________ 174. 

Collection number _____ 4178-CO*. 

Geographic location ____ Road and creek exposures across the 

Kentucky River from the termination of Kentucky Route 595. 

Coordinates ___________ 36 mm east, 274 mm north (base of 

section at 54 mm east, 246 mm 

north). 

Formation ____________ Sulphur Well Member, Lexington 

Limestone. 

Stratigraphic position __ 188 ft above the base of the section. 

Quadrangle name ______ Valley View, Ky. 

Section name ----------Valley View B (Hunters Ferry 

Road). 

Section number ________ 34. 

Collection number _____ 4179-CO*. 

Geographic location ____ The same as for 4178-CO. 

Coordinates ----------- Do. 

Formation ____________ Sulphur Well Member, Lexington 

Limestone. 

Stratigraphic position __ 187 ft above the base of the section. 

Quadrangle name ______ Valley View, Ky. 

Section name ----------Valley View B (Hunters Ferry 

Road). 

Section number ________ 34. 

Collection number _____ 4180-CO*. 

Geographic location ____ The same as for 4178-CO. 

Coordinates ----------- Do. 

Formation ____________ Sulphur Well Member, Lexington 

Limestone. 

Stratigraphic position __ 186 ft above the base of the section. 

Quadrangle name ______ Valley View, Ky. 

Section name ----------Valley View B (Hunters Ferry 

Road). 

Section number ________ 34. 

Collection number _____ 4184-CO*. 

Geographic location ____ The same as for 4178-CO. 

Coordinates ----------- Do. 

Formation ____________ Brannon Member, Lexington Limestone. 

Stratigraphic position __ 180 ft above the base of the section. 

Quadrangle name ______ Valley View, Ky. 

Section name ----------Valley View B (Hunters Ferry 

Road). 

Section number ________ 34. 

Collection number _____ 4191-CO*. 

Geographic location ____ The same as for 4178-CO. 

Coordinates ___________ 54 mm east, 262 mm north. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 104 ft above the base of the ·section. 

Silicified --------------Yes. 

Quadrangle name ______ Valley View, Ky. 

Section name ----------Valley View B (Hunters Ferry 

Road). 

Section number ________ 34. 

Collection number _____ 4194-CO*. 

Geographic location ____ Kentucky Route 52, 0.75 mi south 

of crossing with Taylor Fork. 

Coordinates ___________ 220 mm east, 400 mm north. 

Formation ____________ Back Bed, Tate Member, Ashlock 

Formation. 

Silicified --------------Yes. 

Quadrangle name ______ Richmond South, Ky. 

Collection number _____ 4195-CO*. 

Geographic location ____ U.S. Route 25 crossing of Dog 

Branch of Silver Creek, 3. 7 mi 

south of junction of U.S. Routes 

25 and 421. 

Coordinates ___________ 362 mm east, 36 mm north. 

Formation ____________ Stingy Creek Member, Ashlock Formation. 

Stratigraphic position __ Near base of Stingy Creek Member. 

Silicified --------------Yes. 

Quadrangle name ______ Richmond South, Ky. 

Section name __________ Dog Branch Section. 

Collection number _____ 4197-CO*. 

Geographic location ____ Roadcut on Kentucky Route 52 near 

crossing of Old Town Branch, 0.5 

mi northeast of Caleast, Ky. 

Coordinates ___________ 182 mm east, 327 mm north, 

Formation ____________ Calloway Creek Limestone. 

Stratigraphic position _ _40 ft above the top of the Garrard 

Siltstone. 

Silicified --------------Yes. 

Quadrangle name ______ Richmond South, Ky. 

Collection number _____ 4208-CO. 

Geographic location ____ U.S. Route 150 along west bluff of 

Beech Fork northwest of Fredericktown, Ky. 
INTRODUCTION A21 

Coordinates ___________ Bas.e of section at 81 mm east; 61 

mm north. 

Formation ------------Upper tongue of the Grant Lake 

Formation. 

Stratigraphic position __ 133 ft below the base of the Brass-

. field Dolomite (Silurian). 

Silicified --------------Yes. 

Quadrangle ___________ Maud, Ky. 

Collection number _____ 4209-CO. 

Geographic location ____ The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation ------------Tate Member, Ashlock Formation. 

Stratigraphic position __ 158 ft below the base of the Brassfield Formation (Silurian). 

Silicified --------------Yes. 

Quadrangle ___________ Maud, Ky. 

Collection number _____ 4210-CO. 

Geographic location ----The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation ------------Tate Member, Ashlock Formation. 

Stratigraphic position __ 167 ft below base of the Brassfield 

Dolomite (Silurian). 

Silicified --------------Yes. 

Quadrangle ___________ Maud, Ky. 

Collection number _____ 4211-CO. 

Geographic location ____ Kentucky Route 605 3 mi south of 

junction with U.S. Route 150. 

Coordinates ___________ 356 mm east, 520 mm north. 

Formation ------------Upper part of Grant Lake Limestone. 

Stratigraphic position __ 99 ft below the base of the Brassfield Formation (Silurian). 

Silicified --------------Yes. 

Quadrangle ___________ Loretto, Ky. 

Collection number _____ 4213-CO*. 

Geographic· location ____ Creek exposure 0.55 mi south of 

Kentucky Route 169, 1.35 mi east 

of Nicholasville, Ky. 

Coordinates ___________ 322 mm east, 23 mm north. 

Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ 3 ft below Curdsville Limestone 

Member-Logana Member contact. 

Quadrangle name _____ Nicholasville, Ky. 

Collection number _____ 4464-CO*. 

Geographic location ____ 1.2 mi east and 1 mi south of the 

northwest corner of the Union 

City quadrangle, Kentucky. 

Coordinates ___________ 83 mm east, 513 mm north. 

Formation ____________ Back Bed, Tate Member, Ashlock 

Formation. 

Silicified -------------- Yes. 

Quadrangle name ------Union City, Ky. 

Collection number _____ 4465-CO*. 

Geographic location ____ 1.3 mi north and 3.1 mi west of the 

southeast corner of the Union 

City quadrangle, Kentucky. 

Coordinates ___________ 248 mm east, 87 mm north. 

Formation ____________ Preachersville Member, Drakes Formation. 

Quadrangle name ______ Union City, Ky. 

Collection number _____ 4466-CO. 

Geographic location ____ 7,200 ft south and 9,700 ft east of 

the northwest corner of the Union 

City quadrangle, Kentucky. 

Coordinates ___________ 124.5 mm east, 485 mm north. 

Formation ____________ Reba Member, Ashlock Formation. 

Quadrangle -----------Union City, Ky. 

Collection number ____ _4467-CO'~. 

Geographic location ____ 0.4 mi east and 0.85 mi south of the 

northwest corner of the Palmer 

quadrangle, Kentucky. 

Coordinates ___________ 28 mm east, 517 mm north. 

Formation ____________ Reba Member, Ashlock Formation. 

Quadrangle name ______ Palmer, Ky. 

Collection number _____ 4468-CO*. 

Geographic location ____ 2.6 mi east and 0.1 mi north of the 

southwest corner of the Palmer 

quadrangle, Kentucky. 

Coordinates ___________ 170 mm east, 4 mm north. 

Formation ____________ Otter Creek Coral Bed, Preachersville Member, Drakes Formation. 

Quadrangle name _____ Palmer, Ky. 

Collection number _____ 4491-CO*. 

Geographic location ____ Roadcut about 3.5 mi west of courthouse in Owingsville, Ky., on U.S. 

Route 60, near headwaters of 

Hurricane Creek. . 

Coordinates ___________ 193 mm east, 98 mm north. 

Formation ____________ Sunset Member, Bull Fork Formation. 

Quadrangle name ______ Owingsville, Ky. 

Collection number _____ 4556-CO*. 

Geographic location ____ Buffalo Creek about 0.3 mi south of 

intersection of Kentucky Route 

1156 and Clay Lane Road. 

Coordinates ___________ 23 mm east, 306 mm north. 

Formation ____________ Back Bed, Tate Member, Ashlock 

Formation. 

Silicified --------------Yes. 

Quadrangle, name ______ Richmond North, Ky. 

Collection number _____ 4573-CO. 

Geographic location ____ Exposures along West Run and in 

old quarry about 1.3 mi west of 

Liberty, Ind. 

Coordinates ___________ 159 mm east, 70 mm north. 

Formation _____________ Dillsboro Formation. 

Stratigraphic position _ _40 ft above base of section. 

Silicified --------------Yes. 

Quadrangle name ______ Liberty, Ind. 

Collection number _____ 4574-CO. 

Geographic· location ____ The same as for 4573-CO. 

Coordinates ----------- Do. 

Formation ____________ Dillsboro Formation. 

Stratigraphic position __ 42-43 ft above the base of the 

section. 
A22 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Silicified _____ ;.. ________ Yes. 

Quadrangle name ______ Liberty, Ind. 

Collection number _____ 4575-CO. 

Geographic location ----The same as for 4573-CO. 

Coordinates ----------- Do. 

Formation ____________ Dillsboro Formation. 

Stratigraphic position __ Float 28-44 ft above base of section. 

Silicified --------------Yes. 

Quadrangle name ______ Liberty, Ind. 

Collection number _____ 4852-CO*. 

Geographic location ____ Section along Interstate Route 75, 

1.4 mi south of Georgetown, Ky., 

exit. 

Coordinates -----------364 mm east, 321 mm north. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 25 ft below the top of the Grier 

Limestone Member. 

Silicified --------------Yes (850 lbs). 

Quadrangle name ______ Georgetown, Ky. 

Section name ----------Georgetown A. 

Section number ________ 151. 

Collection number _____ 4871-CO*. 

Geographic location ____ Road exposures between Trinity 

Church and Antioch Church, 

southw·est quadrant Valley View 

quadrangle, Kentucky. 

Coordinates ___________ Base of section at 19 mm east, 176 

mm north. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 25 ft above the base of the section. 

Quadrangle name ------Valley View, Ky.1 

Section name----------Valley View C (Antioch Church 

Road). 

Section number ________ 180. 

Collection number -----4872-CO*. 

Geographic location ----The same as for 4871-CO. 

Coordinates ----------- Do. · 

Formation ------------Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 27 ft above the base of the section. 

Quadrangle name ______ Valley View, Ky. 

Section name----------Valley View C (Antioch Church 

Road). 

Section number ________ 180. 

Collection number _____ 4874-CO*. 

Geographic location ____ The same as for 4871-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 30 ft above the base of the section. 

Quadrangle name ------Valley View, Ky. 

Section name ----------Valley View C (Antioch Church 

Road). 

Section number --------180. 

Collection number _____ 4876-CO*. 

Geographic location ____ The same as for 4871-CO. 

1 Collections 4871-C0-4905-CO are not listed on the map of the Valley 

View quadrangle, their positions are indicated on the stratigraphic section accompanying the map of the Little Hickman quadrangle, Kentucky. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 35 ft above the base of the section. 

Silicified --------------Yes (30 lbs). 

Quadrangle name ------Valley View, Ky. 

Section name ----------Valley View C (Antioch Church 

Road). 

Section number ________ 180. 

Collection number _____ 4879-CO*. 

Geographic location ____ The same as for 4871-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position" __ 43-45 ft above the base of the 

section. 

Silicified --------------Yes (200 lbs). 

Quadrangle name ------Valley View, Ky. 

Section name ----------Valley View C (Antioch Church 

Road). 

Section number ________ 180. 

Collection number _____ 4880-CO*. 

Geographic location ____ The same as for 4871-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 47 ft above the base of the section. 

Silicified --------------Yes (50 lbs). 

Quadrangle name ______ Valley View, Ky. 

Section name ----------Valley View C (Antioch Church 

Road). 

Section number ________ 180. 

Collection number _____ 4898-CO*. 

Geographic location ____ The same as for 4871-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 150 ft above the base of the section. 

Quadrangle name ______ Valley View, Ky. 

Section name----------Valley View C (Antioch Church 

Road). 

Section number ________ 180. 

Collection number -----4905-CO*. 

Geographic location ____ The same as for 4871-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ Float, 190 ft above base of section. 

Quadrangle name------ Valley View, Ky. 

Section name---------- Valley View C (Antioch Church 

Road). 

S·ection number ________ 180. 

Collection number _____ 4929-CO*. 

Geographic· location ____ Road exposures 0.5 mi east and 1.6 

mi south of northwest corner of 

Salvisa quadrangle, Kentucky. 

Coordinates ___________ 32 mm east, 467 mm north. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 8 ft below the base of the Brannon 

Member, Lexington Limestone. 

Silicified --------------Yes (20 Ibs). 
INTRODUCTION A23 

Quadrangle name ______ Salvisa, Ky. 

Section name __________ Salvisa A. 

Section number ________ 175. 

Collection number _____ 4940-CO*. 

Geographic location ____ Road exposure on west side of Kentucky River at bridge crossing of 

Central Kentucky Parkway, on 

north side of parkway. 

Coordinates ___________ Base of section at 186 mm east, 508 

mm north. 

Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ 7 ft above the top of the Tyrone 

Limestone. 

Silicified --------------Yes· (7 lbs)". 

Quadrangle name ______ Salvisa, Ky. 

Section name __________ Salvisa B. 

Section number ________ 176. 

Collection number _____ 4956-CO*. 

Geographic loc-ation ____ The same as for 4940-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 137 ft above the top of the Tyrone 

· Limestone. 

Quadrangle name ------Salvisa, Ky. 

Section name __________ Salvisa B. 

Section number --------176. 

Collection number _____ 4957-CO*. 

Geographic location ____ The same as for 4940-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 144 ft above the top of the Tyrone 

Limestone. 

Quadrangle name ______ Salvisa. Ky. 

Section name __________ Salvisa B. 

Section number ________ 176. 

Collection number _____ 4959-CO*. 

Geographic location ____ The same as for 4940-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 149-152 ft above the top of the 

Tyrone Limestone. 

Silic-ified --------------Yes (1,001 lbs). 

Quadrangle name ______ Salvisa, Ky.2 

Section name __________ Salvisa B. 

Section number ________ 176. 

Collection number _____ 4963-CO*. 

Geographic location ____ Road exposure in east-bound fanes 

of Interstate Route 64, 0.5 mi east 

of Frankfort-Lawrenceburg, Ky., 

interchange. 

~Note on the published geologic map of the Salvisa quadrangle that 

this collection is indicated as coming from the same section as 4929-CO; 

Cressman ( 1973; pl. 1, noted on proper placement of the collection in 

section 176. 

Coordinates ___________ Base of section at 417 mm east, 148 

mm north. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 30 ft below the, base of the Brannon 

Member, Lexington Limestone. 

Quadrangle name ______ Frankfort West, Ky. 

Section name __________ Frankfort West A. 

Section number ________ 88. 

CoUection number _____ 4964-CO*. 

Geographic location ____ The same as for 4963-CO. 

Coordinates ----------- Do. 

Formation ------------Grier Limestone Member, Lexington 

Limestone. 

-' Stratigraphic position __ 27 'ft below the base ·of the Brannon 

Member, Lexington Limestone. 

Quadrangle name ______ Frankfort West, Ky. 

Section name __________ Frankfort West A. 

Section number ________ 88. 

Collection number _____ 4982-CO*. 

Geographic location ____ The .same as for 4963-CO. 

Coordinates ----------- Do. 

Formation ------------Tanglewood Limestone Member, Lexington Limestone. 

Stratigraphic position __ 32 ft above the base of the Brannon 

Member, Lexington Limestone. 

Quadrangle name ______ Frankfort West, Ky. 

Section name __________ Frankfort West A. 

Section number ________ 88. 

Collection number _____ 4998-CO*. 

Geographic location =----The same as for 4963-CO. 

Coordinates ----------- Do. 

Formation ------------Tanglewood Limestone Member, Lexington Limestone. 

Stratigraphic position __ 84 ft above the base of the Brannon 

Member, Lexington Limestone. 

Quadrangle name ______ Frankfort West, Ky. 

Section name __________ Frankfort West A. 

Section number ________ 88. 

Collection number _____ 5015-CO*. 

Geographic location ____ Quarry exposure 0.4 mi south of 

Perryville, Ky., on e-ast side of 

Mitchellsburg Road, east side of 

Chaplin River. 

Coordinates -----------191 mm east, 92 mm north. 

Formation ____________ Salvisa Bed, Perryville Limestone 

Member, Lexington Limestone. 

Stratigraphic position __ 5 ft above base of Salvisa Bed. 

Silicified --------------Yes (1,423 lbs). 

Quadrangle name ______ Perryville, Ky. 

Section name _.:. ________ Perryville B (Perryville South). 

Section number ________ 30B. ' 

Collection number _____ 5016-CO*. 

Geographic location ____ The same as for 5015-CO. 

Coordinates ----------- Do. 

Formation ____________ Cornishville Bed, Perryville Limestone Member, Lexington Limestone. 
A24 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Stratigraphic position __ 14 ft above the base of the Salvisa 

Bed, Perryville Limestone Member, Lexington Limestone. 

Silicified-------------- Yes (7 lbs). 

Quadrangle name ______ Perryville, Ky. 

Section name __________ Perryville B (Perryville South). 

Section number ________ 30B. 

Collection number _____ 5022-CO. 

Geographic location ____ Section in quarry and road exposures near Clear Creek, 0.2 mi 

east and 2.6 mi south of the northwest corner of the Keene quadrangle, Kentucky. 

Coordinates ___________ Base of section at 21 mm east, 326 

mm ·north. 

Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ Float from the lower 22 ft of the 

Curdsville Limestone Member. 

Silicified --------------Yes (75 lbs). 

Quadrangle name ______ Keene, Ky. 

Section name __________ Keene A. 

Section number ________ 150. 

Collection number _____ 5023-CO. 

Geographic location ____ The· same as for 5022-CO. 

Coordinates ----------- Do. · Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ 30 ft above the base of the Curdsville Limestone Member. 

Silicified --------------Yes (75 lbs). 

Quadrangle name ______ Keene, Ky. 

Section name __________ Keene A. 

Section number ________ 150. 

Collection number _____ 5025-CO. 

Geographic location ____ Road exposure west from crossing 

of Kentucky Route 32 and the 

Licking River. 

Coordinates ___________ Base of section at 197 mm east, 499 

mm north. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 4 ft above base of section. 

Quadrangle name ______ Moorefield, Ky. 

Section name __________ Moorefield A. 

Section number ________ 173. 

Collection number _____ 5027-CO. 

Geographic location ____ The same as for 5025-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position -~ 18 ft above base of section. 

Quadrangle name ______ Moorefield, Ky. 

Section name ----------Moorefield A. 

Section number ________ 173. 

Collection number ----- 5030-CO. 

Geographic location ____ The same as for 5025-CO. 

Coordinates _______ ____ Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 27 ft above base of section. 

Quadrangle name ______ Moorefield, Ky. 

Section name __________ Moorefi-eld A. 

Section number ________ 173. 

Collection number -----5031-CO. 

Geographic location ____ The same as for 5025-CO. 

Coordinates ----------- Do. 

Formation ____________ Nicholas Bed, Tanglewood Limestone Member, Lexington Limestone. 

Stratigraphic position __ 50 ft above base of section. 

Quadrangle name ______ Moorefield, Ky. 

Section name __________ Moorefield A. 

Section number ________ 173. 

Collection number _____ 5033-CO. 

Geographic location ____ The same as for 5025-CO. 

Coordinates ----------- Do. 

Formation ____________ Nicholas Bed, Tanglewood Limestone 

Member, Lexington Limestone·. 

Stratigraphic position __ 72 ft above base of section. 

Quadrangle name ______ Moorefield, Ky. 

Section name __________ Moorefield A. 

Section number ________ 173. 

Collection number _____ 5036-CO*. 

Geographic location ____ Small stream exposure on Squires 

Road, 1.8 mi southwest of intersection with U.S. Route 421 (upstream 0.1 mi). 

Coordinates ___________ 151 mm east, 494 mm north. 

' Formation ____________ Devils Hollow Member, Lexington 

Limestone. 

Stratigraphic position __ 60 ft above the base of the Brannon 

Member, Lexington Limestone. 

Silicified --------------Yes (300 lbs). 

Quadrangle name ______ Coletown, Ky. 

Collection number _____ 5039-CO*. 

Geographic location ____ Roadcut on Interstate Route 75, 

north of Clays Ferry Bridge 

crossing of Kentucky River. 

Coordinates ___________ 80 mm east, 94 mm north. 

Formation ____________ Probably Preachersville Member, 

Drakes Formation. 

Stratigraphic position __ Breccia in Elk Lick Creek graben. 

Quadrangle name ______ Ford, Ky. 

Collection number _____ 5058-CO. 

Geographic location ____ Roadcuts west of Sadieville, along 

Interstate Route 75, north of 

Eagle Creek. 

Coordinates ___________ Base of section at 182 mm east, 125 

mm north. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 27-28 ft above the base of the main 

body of the Clays Ferry Formation. 

Quadrangle name ______ Sadieville, Ky.3 

3 Cressman ( 1973, pl. 2) considered this section to be a part of Sadieville A ( 179), which is exposed south of Eagle Creek along Interstate 

Route 75. 
INTRODUCTION A25 

Section name __________ Sadieville B. 

Collection number _____ 5067-CO*. 

Geographic location ____ Hillside pasture exposure on west 

side of U.S. Route 227, 0.4 mi 

south of intersection of FordHampton Road and U.S. 227, 

north of Ford, Ky. 

Coordinates ___________ 423 mm east, 187 mm north. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 140 ft above top of Tyrone Limestone. 

Silicified --------------Yes (795 lbs). 

Quadrangle name ______ Ford, Ky. 

Collection number _____ 5069-CO*. 

Geographic location ____ Exposures along Hanley Lane behind Old Taylor distillery. 

Coordinates ___________ Base of section at 142 mm east, 112 

mm north. 

Formation ------------Upper Curdsville Limestone Member, Lexington Limestone. 

Silicified --------------Yes ( 40 lbs). 

Quadrangle name ______ Frankfort East, Ky. 

Collection number _____ 5071-CO*. 

Geographic location ____ The same as for 5069-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Grie.r Limestone 

Member, Lexington Limestone. 

Silicified --------------Yes (10 lbs). 

Quadrangle name ______ Frankfort East, Ky. 

CoHection number _____ 5072-CO. 

Geographic location ____ Immediately behind Old Crow distillery, north bluff of Glenns 

Creek Road, 0.7 mi west of intersection with Hanley Lane. 

Coordinates ___________ 107 mm east, 102 mm north. 

Formation ____________ Lower part of Lexington Limestone; 

mostly basal Curdsville Limestone 

Member, but with some float 

blocks of the Logana Member included in the sample. 

Silicified --------------Yes (150 lbs). 

Quadrangle name ______ Frankfort East, Ky. 

Section name· __________ Frankfort East B. 

Section number ________ 87. 

Collection number _____ 5073-CO*. 

Geographic location ____ Northwest of Old Crow distillery, on 

first sharp north bend of Glenns 

Creek Road 0.9 mi west of intersection with Hanley Lane. 

Coordinates ___________ 82 mm east, 111 mm north. 

Formation _.;. __________ Upper part of Logana Member, 

Lexington Limestone. 

Stratigraphic position __ Just below 4 ft-thick dalmanellid 

coquina. 

Silicified --------------Yes ( 496 lbs). 

Quadrangle name ______ Frankfort East, Ky. 

Section name· __________ Frankfort East B. 

Section number ________ 87. 

Collection number _____ 5080-CO*. 

Geographic location ____ First crossing of Southern Railroad 

tracks by unnamed road running 

due south from two right-angle 

turns in Kentucky Route 342, 1.2 

mi west of Herrington Lake Spillway. 

Coordinates ___________ 88 mm east, 158 mm north. 

Formation ------------Upper part of Curdsville Limestone 

Member, Lexington Limestone. 

Silicified --------------Yes (250 lbs). 

Quadrangle name ______ Wilmore, Ky. 

Collection number _____ 5081-CO. 

Geographic location ____ From east side of Blackburn Memorial Bridge crossing of Kentucky River take first road north 

toward Kentucky utilities plant; 

section in railroad and road exposures. 

Coordinates ___________ 99 mm east, 214 mm north ('railroad exposures). 

Formation ------------Tyrone Limestone. 

Stratigraphic position __ Float, 35 ft below top of Tyrone 

Limestone. 

Silicified --------------Yes (5 lbs). 

Quadrangle name ______ Tyrone, Ky. 

Section name ----------Tyrone C. 

Section number ________ 174 .. 

Collection number _____ 5084-CO. 

Geographic location ____ The same as for 5081-CO. 

Coordinates ___________ 108 mm east, 214 mm north (railroad exposures) . 

Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ 5 ft above base of Curdsville Limestone Member. 

Silicified --------------Yes (12 lbs). 

Quadrangle name ______ Tyrone, Ky. 

Section name __________ Tyrone C. 

Section number ________ 174. 

Collection number _____ 5086-CO. 

Geographic location ____ The same as for 5081-CO. 

Coordinates -----------The same as for 4124-CO. 

Formation ____________ Logana Member, Lexington Limestone. 

Stratigraphic position __ 18-20 ft above· the base of the 

Logana Member. 

Silicified --------------Yes (100 lbs). 

Quadrangle name ______ Tyrone, Ky. 

Section name ----------Tyrone C. 

Section number ________ 174. 

Collection number _____ 5087-CO*. 

Geographic location ____ Small road exposure on U.S. Route 

421, 0.5 mi east of U.S. Routes 

60 and 421 junction. 

Coordinates ___________ 242 mm .east, 287 mm north. 

Formation ------------Upper part of Devils Hollow Member, Lexington Limestone. 

Silicified -------------- Yes ( 458 lbs). 

Quadrangle name ______ Frankfort East, Ky. 

Collection number _____ 5089-CO*. 
A26 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Geographic loc·ation ____ Road exposure on westbound lanes 

of Interstate Route 64, on traffic 

island south side of west bound 

lanes. 

Coordinates ___________ 97 mm east, 173 mm north. 

Formation ____________ Macedonia Bed, Grier Limestone 

Member, Lexington Limestone. 

Silicified --------------Yes. 

Quadrangle name ____ -__ Frankfort East, Ky.' 

Collection number _____ 5092-CO. 

Geographic location ____ The same as for 5081-CO. 

Coordinates -----------The same as for 4124-CO. 

Formation ____________ Logana Member, Lexington Limestone. 

Stratigraphic position __ 10-12 ft above the base of the 

Logana Member. 

Silicified --------------Yes (997 lbs). 

Quadrangle name ______ Tyrone, Ky. 

Section name ----------Tyrone C. 

Section number ________ 174. 

Collection number _____ 5093-CO*. 

Geographic location ____ 0.3 mi southwest of Kentucky River 

on Devils Hollow Road. 

Coordinates -----------411 mm east, 318 mm north. 

Formation ____________ Mac·edonia Bed, Grier Limestone 

Member, Lexington Limestone. 

Stratigraphic position __ Float. 

Silicified --------------Yes (25 lbs). 

Quadrangle name ______ Frankfort West, Ky. 

Collection number _____ 5095-CO*. 

Geographic location ____ Road exposure on north side of 

westbound lanes of Interstate 

Route 64, about 0.5 mi east of 

bridge over Kentucky River. 

Coordinates ___________ 123 mm east, 195 mm north. 

Formation ------------Devils Hollow Member, Lexington 

Limestone. 

Stratigraphic position __ 6-8 ft above the base of the Devils 

Hollow Member. 

Silicified --------------Yes (542 lbs). 

Quadrangle name ______ Frankfort East, Ky.6 

Section name __________ Frankfort East A. 

Section number ________ 86. 

Collection number _____ 5096-CO. 

Geographic location ____ Just before· ferry crossing of Tates 

Creek Road and Kentucky River, 

take road west toward Daniel 

Boone YMCA Camp; collection 

from near top of north bluff Kentucky River, 0.4 mi southeast of 

YMCA Camp in abandoned railroad bed. 

Coordinates ___________ 151 mm east, 432 mm north. 

Formation ------------Grier Limestone Member, Lexington 

Limestone. 

4 On geologic quadrangle map this locality is marked on the north side 

of the westbound lanes. 6 The geologic map of this quadrangle incorrectly places this collection 

in the Tanglewood Limestone Member, Lexington Limestone. 

Silicified --------------Yes (300 lbs). 

Quadrangle name ------Valley View, Ky. 

Collection number _____ 5100-CO*. 

Geographic location ____ Crisman Mill Road, 0.2 mi west of 

Hickman Creek crossing. 

Coordinates ___________ 411 mm east, 451 mm north. 

Formation ____________ Lower part of Curdsville Limestone 

Member, Lexington Limestone. 

Silicified --------------Yes. (600 lbs). 

Quadrangle' name ______ Little Hickman, Ky. 

Section name __________ Little Hickman B. 

Collection number _____ 5101-CO. 

Geographic location ____ Kentucky Route 169 just west of 

Hickman Creek crossing. 

Coordinates -----------398 mm east, 81 mm north. 

Formation ____________ Lower part of Curdsville Limestone 

Member, Lexington Limestone. 

Silicified --------------Yes (799 lbs). 

Quadrangle name ______ Nicholasville, Ky. 

Collection number ___ ... _5107-CO. 

Geographic location ____ Hillside exposure in farm road leading south from U.S. Route 60, just 

west of Keeneland racetrack collected at 900-ft contour. 

Coordinates __________ _43 mm east, 194 mm north. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Silicified --------------Yes (75 lbs). 

Quadrangle name ______ Lexington West, Ky. 

Collection number _____ 5120-CO. 

Geographic location ____ Hill slopes on farmland 1.2 mi northnortheast of Judio, Ky. Section 

begins near junction of farm access road near mouth of Perry 

Cary Hollow and was measured 

northerly up hill slope, then offset south about 600 ft to outc·rops 

near farmhouse, and then east up 

hill slope· east of farmhouse. 

Coordinates ___________ Coordinates for the base of this section were measured east and then 

south from the northwest corner 

of the Blacks Ferry quadrangle. 

84 mm east, 183 mm south. 

Formation ____________ Leipers Limestone. 

Stratigraphic· position __ 50.5 ft below the base of the· Cumberland Formation. 

Quadrangle name ______ Blacks Ferry, Ky. 

Section name __________ Judio North. 

Section number ________ 703. 

Collection number _____ 5135-CO. 

Geographic location ____ Outcrops at and near abandoned 

Clara Wilham Quarry, about 1.2 

mi south of Dunnville, Ky. and 

about 500 ft east of U.S. Route 

127 (Kentucky Route 35). 

Coordinates ___________ 431 mm east, 262 mm north, 

Formation ------------Reba Member, Ashlock Formation. 

Quadrangle name ______ Dunnville, Ky. 

Section name __________ Dunnville South. 

Section number --------702. 
• 

INTRODUCTION A27 

Collection number _____ 5136-CO. 

Geographic location ____ The same as for 5135-CO. 

Coordinates ----------- Do. 

Formation ____________ Reba Member, Ashlock Formation. 

Quadrangle name ______ Dunnville, Ky. 

Section name __________ Dunnville South. 

Section number --------702. 

Collection number _____ 5137-CO. 

Geographic location ____ Outcrops along U.S. Route· 127 

(Kentucky Route 35) in roadcut 

a few hundred feet north of junction with Kentucky Route 906 on 

west side of the settlement of 

Kidds Store, Ky. 

Coordinates ___________ Base of section at 78.5 mm east, 191 

mm north. 

Formation ____________ Gilbert Member, Ashlock Formation. 

Quadrangle ___________ Hustonville, Ky. 

Section name __________ Kidds Store. 

Section number ________ 101. 

Collection number _____ 5140-CO. 

Geographic· location ____ U.S. Route 27, 0.1 mi northeast of 

crossing of Dix River. 

Coordinates ___________ 42.5 mm east, 342 mm north. 

Formation _ _: __________ Reba Member, Ashlock Formation. 

Quadrangle name ______ Lancaster, Ky. 

Section name __________ Ashlock Cemetery. 

Section number ________ 21B. 

Collection number _____ 5141-CO. 

Geographic location ____ The same as for 5140-CO. 

Coordinates ----------- Do. 

Formation ____________ Stingy Creek Member, Ashlock Formation. 

Quadrangle name ______ Lancaster, Ky. 

Section name __________ Ashlock Cemetery. 

Section number ________ 21B. 

Collection number _____ 5183-CO. 

Geographic location ____ Roadside exposure on northbound 

lanes of Interstate Route 75 south 

of Eagle Creek. 

Coordinates -----------Base of section about 181 mm east, 

108 mm north. 

Formation ____________ Lower tongue of Clays Ferry Formation. 

Stratigraphic position __ 4 ft above base of lower tongue of 

Clays Ferry Formation. 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville A. 

Section number ________ 179. 

Collection number _____ 5308-CO*. 

Geographic location ____ 10,150 ft south and 8,650 ft west of 

the northeast corner of the Union 

City quadrangle. 

Coordinates ___________ 348.5 mm east, 447.5 mm north. 

Formation ____________ Otter Creek Coral Bed. Preachersville Member, Drakes Formation. 

Quadrangle -----------Union City, Ky. 

Collection number _____ 5309-CO*. 

Geographic location ____ About· 4 mi north and 1.4 mi east 

of southwest corner of Union City 

quadrangle, Kentucky. 

Coordinates ___________ 96 mm east, 253 mm north. 

Formation ____________ Otter Creek Coral Bed, Preachersville Member, Drakes Formation. 

Quadrangle name ------Union City, Ky. 

Collection number _____ 5899-CO. 

Geographic location ____ Subsurface section cored just west 

of U.S. Route 27, about 0.3 mi 

northeast of intersection with 

Baker Lane. 

Coordinates ___________ 241 mm east, 185 mm north. 

Formation ------------Upper part of Curdsville Limestone 

Member, Lexington Limestone. 

Stratigraphic position __ 184.4 ft below the top of the core. 

Quadrangle name ______ Nicholasville, Ky. 

Section name __________ Nicholasville 1 (A. J. Denny Heirs). 

Section number ________ 152. 

Collection number _____ 6127-CO. 

Geographic location ____ Southernmost tributary of Landing 

Run, 2,000 ft east of intersection 

of U.S. Route 31E and Kentucky 

Route 46, between Balltown and 

Culvertown, Ky. 

Coordinates ___________ 381 mm east, 436 mm north. 

Formation ____________ Rowland Member, Drakes Formation. 

Silicified --------------Yes (710 lbs). 

Quadrangle name ______ New Haven, Ky. 

Collection number _____ 6128-CO. 

Geographic location ____ Outcrop at farm pond 2,000 ft west 

of intersection of Mt. Horeb and 

Carrick Roads, 1,000 ft north of 

Carrick Road. 

Coordinates ___________ 183 mm east, 387 mm north. 

Formation ____________ Clays Ferry Formation tongue between Millersburg Member, Lexington Limestone, below and 

Tanglewood Limestone Member, 

Lexington Limestone, above. 

Stratigraphic position __ 5-10 ft above base of Clays Ferry 

Formation tongue, 15-20 ft above 

Allonychia flanaganensis Zone in 

the Millersburg Member, Lexington Limestone. 

Silicified --------------Yes (389 lbs). 

Quadrangle name ______ Centerville, Ky. 0 

Collection number _____ 6129-CO. 

Geographic location ____ Lebanon Stone quarry, north side 

Kentucky Routes 49 and 52, 0.3 

mi east intersection of Kentucky 

Route 327 and Kentucky Routes 

49 and 52. 

Coordinates ___________ 163 mm east, 464 mm north. 

0 On the geologic map of the Centerville quadrangle, the part of 

Clays Ferry Formation that intertongues with the upper part of Lexington Limestone is mapped as argillaceous limestone and shale. 
A28 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Formation ____________ Gilbert Member, Ashlock Forma- 1 

. . tion. 

Silicified ______ .;.. _____ . __ Yes (68 lbs). 

Quadrangle name _.;. __ .:__Lebanon West, Ky. 

Collection number _____ 6131-CO*. 

Geographic location ____ Section on Kentucky Route 33, just 

north of bridge crossing of Mocks 

Branch, 2.5 miles north of Danville, Ky. 

Coordinates ___________ 405 mm east, 307 mm north. 

Formation ------------Upper part of Curdsville Limestone 

Member, Lexington Limestone. 

Stratigraphic position __ 23 ft above the Tyrone LimestoneLexington Limestone contact. 

Silicified --------------Yes (707 lbs). 

Quadrangle name ______ Danville, Ky. 

Collection number _____ 6134-CO*. 

Geographic location ____ Road exposures 0.2 mi west of Dix 

River crossing of Kentucky Route 

52. 

Coordinates ___________ 315 mm east, 78 mm north. 

Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ Lower 3 ft of Curdsville Limestone 

Member. 

Silicified --------------Yes (632 lbs). 

Quadrangle name ______ Bryantsville, Ky. 

Section name __________ Bryantsville D. 

Collection number _____ 6135-CO*. 

Geographic location ____ The same as for 6134-CO. 

Coordinates ----------- Do. 

Formation ------------Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ 23 ft above the Tyrone Limestone 

Lexington Limestone contact. 

Silicified --------------Yes (371 lbs). 

Quadrangle name ______ Bryantsville, Ky. 

Section name __________ Bryantsville D. 

Collection number _____ 6136-CO*. 

Geographic location ____ Roadcut on Kentucky Route 52, 1.45 

mi east of junction with U.S. 

Route 150; 0.15 mi east crossing 

of Kentucky Route 52 and Balls 

Branch Run. 

Coordinates -----------74 mm east, 35 mm north. 

Formation ____________ Faulconer ·Bed, Perryville Limestone 

Member, Lexington Limestone. 

Stratigraphic position __ Basal 3-4ft of Perryville Limestone 

Member, immediately above the 

Tanglewood Limestone Member, 

Lexington Limestone. 

Silicified --------------Yes (562 lbs). 

Quadrangle name ______ Bryantsville, Ky.' 

Section name ----------Bryantsville B. 

Collection number _____ 6137-CO*. 

Geographic location ____ The same as for 6136-CO. 

7 The Faulconer Bed of the Perryville is not indicated on the geologic 

map of the Bryantsville quadrangle because it is too thin to map. It is 

present and as much as 4 ft thick in the southwest quadrant of the 

quadrangle. 

Coordinates ----------- Do. 

Formation ____________ Salvisa Bed, Perryville Limestone 

Member, Lexington Limes~tone. 

Stratigraphic position __ 8 ft above the Perryville Limestone 

Member-Tanglewood Limestone 

Member contact. 

Silicified --------------Yes (105 lbs). 

Quadrangle name ______ Bryantsville, Ky. 

Section name __________ Bryantsville B. 

Collection number _____ 6138-CO':'. 

Geographic location ____ The same as for 6136-CO. 

Coordinates ----------- Do. 

Formation ____________ Cornishville Bed, Perryville Limestone Member, Lexington Limestone. 

Stratigraphic position __ 16 ft above the Perryville Limestone 

Member-Tanglewood Limestone 

Me"mbe-r contact. 

Silicified --------------Yes (138 lbs). 

Quadrangle name ______ Bryantsville, Ky. 

Section name __________ Bryantsville B. 

Collection numbe-r _____ 6139-CO. 

Geographic location ____ South bank of Salt Creek, 900 ft 

upstream from covered bridge on 

Enochsburg-Oldenburg, (Indiana) 

Road. 

Coordinates ___________ 328 mm east, 378 mm north. 

Formation ------------Upper part of Dillsboro Formation. 

Silicified --------------Yes (573 lbs). 

Quadrangle name ______ New Point, Ind. 

Collection number _____ 6140-CO. 

Geographic location ____ North bank of Salt Creek, 0.4 mi 

upstream from covered bridge on 

Enochsburg-Oldenburg (Indiana) 

Road. 

Coordinates ___________ 315 mm east, 380 mm north. 

Formation ------------Upper part of Dillsboro Formation. 

Silicified --------------Yes (271 lbs). 

Quadrangle name ______ New Point, Ind. 

Collection number _____ 6141-CO. 

Geographic location ____ South bank of Salt Creek, 50 ft upstream from covered bridge on 

Enochsburg-Oldenburg (Indiana) 

Road. 

Coordinates ___________ 336 mm east, 385 mm north. 

Formation ------------Upper part of Dillsboro Formation. 

Silicified --------------Yes (98 lbs). 

Quadrangle name ______ New Point, Ind. 

Collection number _____ 6142-CO*. 

Geographic location ____ Road exposure on east side of Kentucky Route 982, 0.4 mi south of 

junction of Kentucky Routes 32, 

36, and 982 in Cynthiana, Ky. 

(across highway from River View 

Mission Church and Liggett and 

Myers tobacco warehouse) . 

Coordinates ___________ 290 mm east, 39 mm north. 

Formation ____________ Lower tongue of Clays Ferry Formation. 
INTRODUCTION A29 

Stratigraphic position __ 18-20 ft above the base of the 

section. 

Silicified --------------Yes (353 lbs). 

Quadrangle name------ Cynthiana, Ky. 

Collection number _____ 6143-CO*. 

Geographic location ____ The same as for 6142-CO. 

Coordinates ----------- Do. 

Formation ------------Upper tongue of Clays Ferry For 

mation (separated from lower 

tongue of Clays Ferry Formation 

from which collection 6142-CO 

was made by a tongue of Millersburg Member of Lexington Limestone). 

Stratigraphic position __ 30-35 ft above the base of the 

section. 

Silicified --------------Yes ( 488 lbs). 

Quadrangle name ______ Cynthiana, Ky .. 

Collection number _____ 6144-CO*. 

Geographic location ____ The same as for 6142-CO. 

Coordinates ----------- Do. 

Formation ____________ Base of upper tongue of Millersburg 

Member, Lexington Limestone. 

Stratigraphic position __ 24 ft above the base of the section. 

Silicified --------------Yes (286 lbs). 

Quadrangle name ______ Cynthiana, Ky. 

Collection number _____ 6145-CO*. 

Geographic location ____ Kentucky Route 8, 1 mi south of 

Carntown, Ky. 

Coordinates ___________ 28 mm east, 326 mm north. 

Formation ____________ Point Pleasant tongue, Clays Ferry 

Formation. 

Stratigraphic position __ About 50 ft below the· base of the 

Kope Formation. 

Silicified --------------Yes (141 lbs). 

Quadrangle name ______ Moscow, Ohio-Ky. 

Collection number _____ 6146-CO*. 

Geographic location ____ Section in streamlet immediately 

north of U.S. Route 52, 0.25 mi 

west of the cTossing of Route 52 

and Patterson Run; 2.1 mi west 

of intersection of Route 52 and 

Ohio Route 133. 

Coordinates ___________ 3.5 mm east, 187 mm north. 

Formation ____________ Point Pleasant tongue, Clays Ferry 

Formation. 

Stratigraphic position __ 30-40 ft below the base of the Kope 

Formation. 

Silicified --------------Yes (169 lbs). 

Quadrangle name ______ Felicity, Ohio-Ky. 

Collection number _____ 6211-CO. 

Geographic location ____ Section on east side of Bear Creek 

Road immediately north of intersection with U.S. Route 52, east of 

Chilo, Ohio. 

Coordinates ___________ Base of section at 329 mm east, 233 

mm north. 

Formation ____________ Basal few feet of Kope Formation. 

Quadrangle name ______ Moscow, Ohio-Ky. 

Section name __________ Bear Creek. 

Collection number _____ 6282-CO*. 

Geographic location ____ Northwest side of Interstate Route 

75, Erlanger, Ky., interchange. 

Coordinates ___________ 41 mm east, 125 mm north. 

Formation ____________ Bellevue Tongue of Grant Lake 

Limestone. 

Quadrangle name ______ Covington, Ohio-Ky. 

Collection number _____ 6283-CO':'. 

Geographic location ____ The same as for 6282-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Fairview Formation. 

Quadrangle name ______ Covington, Ohio-Ky. 

Collection number _____ 6284-CO*. 

Geographic location ____ The same as for 6282-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Fairview Formation. 

Quadrangle name ______ Covington, Ohio-Ky. 

Collection number _____ 6286-CO*. 

Geographic location ____ West side of Erlanger Road 4,000 

ft north of collection 6282. 

Coordinates ___________ 41 mm east, 174 mm north. 

Formation ------------Upper part of Fairview Forma,tion. 

Quadrangle ___________ Covington, Ohio-Ky. 

Collection number _____ 6288-CO*. 

Geographic· location ____ The same as for 6286-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Fairview Formation. 

Quadrangle name ______ Covington, Ohio-Ky. 

Collection number _____ 6289-CO*. 

Geographic location ____ The same as for 6286-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Fairview Formation. 

Quadrangle name ______ Covington, Ohio-Ky. 

Collection number _____ 6290-CO*. 

Geographic location ____ The same as for 6286-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Fairview Formation. 

Quadrangle ___________ Covington, Ohio-Ky. 

Collection number _____ 6291-CO*. 

Geographic location ____ The same as for 6286-CO. 

Coordinates -----------The same as for 6286-CO. 

Formation ------------Upper part of Fairview Formation. 

Quadrangle ___________ Covington, Ohio-Ky. 

Collection number _____ 6292-CO*. 

Geographic location ____ The same as for 6286-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Fairview Formation. 

Quadrangle ___________ Covington, Ohi~Ky. 

Collection number _____ 6409-CO. 

Geographic location ____ Hillside exposure south of Kinnard 

Cemetery. along unnamed road 

which runs from Paint Lick Creek 

to Kentucky Route 52, 1.2 mi 

north of Paint Lick, Ky. 
A30 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Coordinates ___________ 367 mm east, 30 mm north. 

Formation ____________ Calloway Creek Limestone. 

Stratigraphic position __ Upper 5 ft of Calloway Creek Limestone, 10 ft below the Back Bed, 

Tate Member, Ashlock Formation. 

Silicified --------------Yes (140 lbs). 

Quadrangle name ______ Kirksville, Ky. 

Section name __________ Kinnard Cemetery. 

Section number ________ 35. 

Collection number _____ 6410-CO. 

Geographic location ____ The same as for 6409-CO. 

Coordinates ----------- Do. 

Formation ____________ Basal part of Back Bed, Tate Member, Ashlock Formation. 

Stratigraphic position __ 10 ft above 6409-CO. 

Silicified --------------Yes (75 lbs). 

Quadrangle ___________ Kirksville, Ky. 

Section name __________ Kinnard Cemetery. 

Section number ________ 35. 

Collection number _____ 6411-CO*. 

Geographic location ____ U.S. Route 27, 0.1 mi northeast of 

crossing of the Dix River. 

Coordinates ___________ 42.5 mm east, 342 mm north. 

Formation ____________ Gilbert Member, Ashlock Formation. 

Stratigraphic position __ 5 ft above the base of the Gilbert 

Member. 

Silicified --------------Yes (236 lbs). 

Quadrangle name ______ Lancaster, Ky. 

Section name __________ Ashlock Cemetery. 

Section number ________ 21B. 

Collection number _____ 6412-CO*. 

Geographic location ____ The same as for 6411-CO. 

Coordinates ----------- Do. 

Formation ____________ Gilbert Member, Ashlock Formation. 

Stratigraphic position __ 11.5 ft above the base of the Gilbert 

Member. 

Silicified --------------Yes (558 lbs). 

Quadrangle name ______ Lancaster, Ky. 

Section name __________ Ashlock Cemetery. 

Section number ________ 21B. 

Collection number _____ 6413-CO*. 

Geographic location ____ U.S. Route 27, 1.1 mi north of junction with Kentucky Route 52, 

north of Lancaster, Ky. 

Coordinates ___________ 160 mm east, 45 mm north. 

Formation ------------Top of Calloway Creek Limestone. 

Silicified --------------Yes ( 421 lbs). 

Quadrangle name ______ Buckeye, Ky. 

Collection number _____ 6414-CO. 

Geographic location ____ Exposures on Kentucky Route 21, 

0.9 mi south of the junction of 

Walnut Meadow Branch and 

Paint Lick Creek. 

Coordinates ___________ 18 mm east, 372 mm north. 

Formation ____________ Gilbert Member, Ashlock Formation. 

Stratigraphic position __ 1-2-ft silicified zone at the top of 

Gilbert Member. 

Silicified --------------Yes (840 lbs). 

Quadrangle name ______ Berea, Ky. 

Collection number _____ 6416-CO. 

Geographic location ____ Road exposures on Interstate Route 

75, just north of crossing of Kentucky Route 169. 

Coordinates ___________ 206 mm east, 57 mm north. 

Formation ____________ Grant Lake· Limestone. 

Stratigraphic position __ 25-30 ft below the top of the 

exposure. 

Silicified --------------Yes (339 lbs). 

Quadrangle name------ Richmond North, Ky. 

Section name __________ Arlington West. 

Section number ________ 98A. 

Collection number _____ 6417-CO. 

Geographic location ____ South entrance L and N Railroad 

tunnel, 0.35 mi north of Boonesbora, Ky. 

Coordinates ___________ 361 mm east, 572 mm north. 

Formation ------------Tanglewood Limestone Member, 

Lexington Limestone. 

Stratigraphic position __ Float, tunnel fill. 

Quadrangle name ______ Richmond North, Ky. 

Collection number _____ 6418-CO. 

Geographic location ____ Kentucky Route 52, 1.5 mi west of 

Reeds Crossing, Ky. 

Coordinates -----------7 mm east, 536 mm north. 

Formation ------------Top of Reba Member, Ashlock Formation. 

Silicified--------------Yes (141 lbs). 

Quadrangle name ______ Moberly, Ky. 

Section name __________ Lake Reba. 

Section number ________ 37. 

Collection number _____ 6419-CO*. 

Geographic location ____ 1.4 mi east of Wilmore, Ky. 500 ft 

north of main road. 

Coordinates ___________ 420 mm east, 534 mm north. 

Formation ____________ Lower part of Logana Member, 

Lexington Limestone. 

Silicified --------------Yes (329 lbs). 

Quadrangle name ------Wilmore, Ky. 

Collection number _____ 6699-CO. 

Geographic location ____ The same as for 6211-CO. 

Coordinates ----------- Do. 

Formation ____________ Point Pleasant tongue, Clays Ferry 

Formation. 

Stratigraphic position __ Float from top 15 ft of the Point 

Pleasant tongue, Clays Ferry Formation. 

Quadrangle name ______ Moscow, Ohio-Ky. 

Section name __________ Bear Creek. 

Collection number _____ 6803-CO. 

Geographic location ____ Exposure on Kentucky Route 11, 1 

mi north of Concord, Ky. 

Coordinates ___________ 357 mm east, 362 mm north. 

Formation ------------Upper part of Grant Lake Limestone. 

Quadrangle name ______ Sherburne, Ky. 
INTRODUCTION A31 

Collection number _____ 6909-CO*. 

Geographic location ____ Road exposure on U.S. Route 27 just 

north of junction with Kentucky 

Route 318, northwest of Falmouth, 

Ky. 

Coordinates ___________ Base of section at 98.5 mm east; 

158 mm north. 

Formation ____________ Point Pleasant Tongue, Clays Ferry 

Formation. 

Stratigraphic position __ Lower 20 ft of section below the 

flow roll beds. 

Silicified --------------Yes (338 lbs). 

Quadrangle name ______ Falmouth, Ky. 

Section name __________ Falmouth A. 

Section number ________ 195. 

Collection number _____ 6915-CO*. 

Geographic location ____ Boyle County quarry, west side of 

U.S. Route 68, 1.3 mi northeast 

of Perryville·, Ky. 

Coordinates ___________ 217 mm east, 176 mm north. 

Formation ____________ Salvisa Bed, Perryville Limestone 

Member, Lexington Limestone. 

Stratigraphic position __ Basal 2 ft of the Salvisa Bed, 42 ft 

above the contact of the Tanglewood Limestone Member and the 

Perryville Limestone Member. Collected from northwest wall of 

quarry. 

Silicified --------------Yes (532 lbs). 

Quadrangle name ______ Perryville, Ky. 

Section name. __________ Perryville A (Perryville North). 

Section number ________ 30A. 

Collection number _____ 6916-CO*. 

Geographic location ____ The same as for 6915-CO. 

Coordinates ----------- Do. 

Formations ___________ Salvisa Bed, Perryville Limestone 

Member, Lexington Limestone. 

Stratigraphic position __ The same as for 6915-CO, but collected from east wall of quarry. 

Silicified --------------Yes (236 lbs). 

Quadrangle name· ______ Perryville, Ky. 

Section name __________ Perryville A (Perryville North). 

Section number ________ 30A. 

Collection number _____ 6945-CO. 

Geographic location ____ East side of Kentucky River, opposite Boonesboro Beach on FordBoonesboro Road. 

Coordinates ___________ 414 mm east, 112 mm north. 

Formation ------------Clays Ferry Formation. 

Stratigraphic position __ 17 ft above main body of Tanglewood Limestone Member, Lexington Limestone. 

Silicified --------------Yes (33 lbs). 

Quadrangle name ______ Ford, Ky. 

Section name ---------- Ford-Boonesboro Road Section. 

Collection number _____ 6990-CO*. 

Geographic location ____ West side of U.S. Route 27, 1,700 ft 

from highway, 0.9 mi south of 

Lair, Ky. 

Coordinates -----------245 mm east, 369 mm north. 

Formation ------------Top of Tongue of Clays Fe.rry Formation which lies between lower 

part of Millersburg Member 

tongue, Lexington Limestone, and 

an upper tongue of Tanglewood 

Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 60 ft above top of Grier Limestone 

Member, Lexington Limestone. 

Silicified --------------Yes (20 lbs). 

Quadrangle name ______ Shawhan, Ky. 

Section name __________ Section at White Farm. 

Collection number _____ 7039-CO*. 

Geographic location ____ 0.7 mi southeast of junction of Kentucky Route 974 and Dry Fork 

Road, on Dry Fork Road. Section 

begins in valley of East Fork of 

Fourmile Creek in the Tanglewood Limestone Member, Lexington Limestone just below the Allonychia flanaganensis Zone of 

Millersburg Member, Lexington 

Limestone. The main part of the 

section is north of East Fork, 

along Dry Fork Road above the 

823-ft elevation mark. 

Coordinates ___________ Base of section at 394 mm east; 

268 mm north. 

Formation ____________ Lowermost tongue of Millersburg 

Member, Lexington Limestone. 

Stratigraphic position __ 15ft above Allonychia flanagancnsis 

horizon. 

Quadrangle name ______ Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7040-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Lowermost tongue of Millersburg 

Member, Lexington Limestone. 

Stratigraphic position __ 16 ft above Allonychia :flanaganensis 

horizon. 

Quadrangle name ______ Winchester, Ky. 

Section name----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7041-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Lowermost tongue of Millersburg 

Member, Lexington Limestone. 

Stratigraphic· position __ 17 ft above Allonychia flanaganensis 

horizon. 

Quadrangle name ------Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

. Collection number _____ 7043-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ------------Tongue of Clays Ferry Formation. 
A32 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Stratigraphic position __ 22 ft above Allonychia flanaganensis 

horizon. 

Quadrangle name ______ Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7044-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ------------Tongue of Clays Ferry Formation. 

Stratigraphic position __ 25 ft above Allonychia flanaganensis 

horizon. 

Quadrangle name ______ Winchester, Ky. 

Section name----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7045-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ------------Tongue of Clays Ferry Formation. 

Stratigraphic position __ 27 ft above Allonychia flanaganensts 

horizon. 

Quadrangle name ______ Winchester, Ky. 

Section name __________ Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7046-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ------------Tongue of Clays Ferry Formation. 

Stratigraphic position __ 30 ft above Allonychia flanaganensis 

horizon. 

Quarlrangle name ______ Winchester, Ky. 

Section name ----------Winche,ster A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7047--CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 33ft above Allonychia .flanaganensis 

horizon. 

Quadrangle name ______ Winchester, Ky. 

Section name----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7049-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 37 ft above Allonychia flanaganensis 

Qaudrangle name ______ Winchester, Ky. 

Section name----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7050-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 39ft above Allonychia .flanaganensis. 

Quadrangle name ______ Winchester, Ky. 

Section name----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7051-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 42-47 ft above Allonychia .flanaganensis. 

Quadrangle name------Winchester, Ky. 

Section name----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7053-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 43ft above Allonychia flanaganensis. 

Quadrangle name ______ Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number ____ ,... ___ 1004. 

Collection number _____ 7054-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 44ft above Allonychia flanaganensis. 

Quadrangle name ______ Winchester, Ky. 

Section name---------- Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7055-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic location __ 47ft above Allonychia flanaga.ncnsis. 

Quadrangle name ______ Winchester, Ky. 

Section name __________ Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7056-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 48ft above Allonychia .flanaganensis. 

Quadrangle name ______ Winchester, Ky. 

Section name __________ Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7057-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 49-52 ft above Allonychia .flanaganensis. 

Quadrangle name ______ Winchester, Ky. 

Section name __________ Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7058-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 
INTRODUCTION A33 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 54-57 ft above Allonychia fianaganensis. 

Quadrangle name ______ Winchester, Ky. 

Section name----------Winchester A (Dry Fork Road). 

Section number --------1004. 

Collection number _____ 7059-CO*. 

Geographic location ----The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 54ft above Allonychia fianaganensis. 

Quadrangle name ------Winchester, Ky. 

Section name----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7060-CO*. 

Geographic location ----The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 57ft above Allonychia fianaganensis. 

Quadrangle name ______ Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7061-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Second tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 58ft above Allonychia fianaganensts. 

Quadrangle name ______ Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number --------1004. 

Collection number _____ 7062-CO*. 

Geographic location ----The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ____________ Middle Tongue of Tanglewood Limestone Member, Lexington Lime~ 

stone. 

Stratigraphic position __ 62ft above Allonychia fianaganensis. 

Quadrangle name ------Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section numbe.r --------1004. 

Collection number -----7066-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ------------Third tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 70-72 ft above Allonychia fianaganensis. 

Quadrangle name------Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number --------1004. 

Collection number _____ 7068-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ------------Third tongue of Millersburg Member, Lexington Limestone. 

Stratigraphic position __ 75ft above Allonychia fianaganensis. 

Quadrangle name ------Winche.ster, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7071-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ------------Upper tongue of Tanglewood Limestone Member, Lexington Limestone. 

Stratigraphic position __ 79ft above Allonychia fianaganensis. 

Quadrangle name ______ Winchester, Ky. 

Section name---------- Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7072-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Formation ------------Uppermost tongue of Mille·rsburg 

Member, Lexington Limestone. 

Stratigraphic position __ 83ft above Allonychia fianaganensis. 

Quadrangle name------Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7079-CO*. 

Geographic location ____ The same as for 7039-CO. 

Coordinates ----------- Do. 

Fonnation ____________ Lowermost tongue of Millersburg 

Member, Lexington Limestone. 

Stratigraphic position __ 18-21 ft above Allonychia .flanaganensis. 

Silicified --------------Yes (156 lbs). 

Quadrangle name ______ Winchester, Ky. 

Section name ----------Winchester A (Dry Fork Road). 

Section number ________ 1004. 

Collection number _____ 7097-CO*. 

Geographic location ____ South bluff of Kentucky Riv·er, 0.6 

mi west of junction with Twomile 

Creek. 

Coordinates ___________ 9 mm east, 36 mm north. 

Formation ____________ Millersburg Member, Lexington 

Limestone, in bed of Tanglewood 

Limestone Member lithology. 

Stratigraphic position __ 44 ft below occurrence of abundant 

Sowerbyella in ov.erlying Clays 

Ferry Formation. 

Silicified --------------Yes (57 lbs). 

Quadrangle name ------Winchester, Ky. 

Collection number _____ 7310-CO. 

Geographic location ____ Outcrop 1,700 :(t east of Kentucky 

Route 89, 1.5 mi southeast of Winchester, Ky. 

Coordinates ___________ 413 mm east, 497 mm north. 

Formation ____________ Strodes Creek Member, Lexington 

Limestone. 

Quadrangle name ______ Winchester, Ky. 
A34 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Collection number _____ 7312-CO. 

Geographic location ____ Outcrop 1,700 ft east of Kentucky 

Route 89, 1.5 mi southeast of Winchester, Ky. 

Coordinates ___________ 413 mm east, 497 mm north. 

Formation ____________ Strodes Creek Member, Lexington 

Limestone. 

Quadrangle· name.:. _____ Winchester, Ky. 

Collection number _____ 7313-CO. 

Geographic loc·ation ____ The same as for 7312-CO. 

Coordinates ----------- Do. 

Formation ____________ Strodes Creek Member, Lexington 

Limestone. 

Qaudrangle name ------Winchester, Ky. 

Collection number _____ 7314-CO. 

Geographic location ____ Roadcuts along Maple Street, U.S. 

Route 227, northern outskirts of 

Winchester, Ky. 

Coordinates ___________ Base of section at 268 mm east, 567 

mm north. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 2.5 ft above base of section. 

Quadrangle name------Winchester, Ky. 

Section name __________ Locality B (Black and Cuppels, 

1973). 

Collection number _____ 7317-CO. 

Geographic position ____ The same as for 7314-CO. 

Coordinates ----------- Do. 

Formation ____________ Strodes Creek Member, Lexington 

Limestone. 

Stratigraphic position __ 10 ft above base of section. 

Quadrangle name ______ Winchester, Ky. 

Section name __________ Locality B (Black and Cuppels, 

1973). 

Collection number _____ 7318-CO. 

Geographic location ----The same as for 7314-CO. 

Coordinates ----------- Do. 

Formation ____________ Strodes Creek Member, Lexington 

Limestone. 

Stratigraphic position __ 11 ft above base of .section. 

Quadrangle name ______ Winchester, Ky. 

Section name __________ Locality B (Black and Cuppels, 

1973). 

Collection number _____ 7319-CO. 

Geographic location ____ The same as for 7314-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 13 ft above base of section. 

Quadrangle name ______ Winchester, Ky. 

Section name __________ Locality B (Black and Cuppels, 

1973). 

Collection number _____ 7321-CO. 

Geographic location ____ The same as for 7314-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 21 ft above base of section. 

Quadrangle name------Winchester, Ky. 

Section name __________ Loc·ality B (Black and Cuppels, 

1973). 

Collection number _____ 7322-CO. 

Geographic location ____ The same as for 7314-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 32 ft above base of section. 

Quadrangle name------Winchester, Ky. . Section name __________ Locality B (Black and Cuppels, 

1973). 

Collection number _____ 7324-CO*. 

Geographic location ____ Exposure on U.S. Route 227 (Maple 

Street, Winchester, Ky., extended) 

0.6 mi north of Interstate Route 

64. 

Coordinates ____________ 266 mm east, 93 mm north. 

Formation ____________ Strodes Creek Member, Lexington 

Limestone. 

Quadrangle name ______ Austerlitz, Ky. 

Collection number _____ 7325-CO*. 

Geographic location ____ The same as for 7324-CO. 

Coordinates ----------- Do. 

Formation ____________ Strodes Creek Member, Lexington 

Limestone. 

Quadrangle name ______ Austerlitz, Ky. 

Collection number _____ 7327-CO*. 

Geographic location ____ Exposure on U.S. Route 227 (Maple 

Street, Winchester, Ky., extended) 

2.6 mi north of Inte·rstate Route 

64. 

Coordinates ___________ 270 mm east, 221 mm north. 

Formation ____________ Strodes Creek Member, Lexington 

Limestone. 

Quadrangle name ______ Austerlitz, Ky. 

Collection number _____ 7328-CO*. 

Geographic location ____ The same as for 7327-CO. 

Coordinates ----------- Do. 

Formation ____________ Strodes Creek Member, Lexington 

Limestone. 

Quadrangle name ______ Austerlitz, Ky. 

Collection number _____ 7330-CO*. 

Geographic location ____ Outcrops on U.S. Route 227 from 

crossing of Strodes Creek to 0.8 

mi southeast of crossing. 

Coordinates -----------Top of section at 268.5 mm east, 

422 mm north. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 93 ft above base of section. 

Quadrangle name ______ Austerlitz, Ky. 

Section name ----------Type section, Strodes Creek Member. 

Collection number _____ 7332-CO*. 

Geographic location ____ The same as for 7330-CO. 

Coordinates ----------- Do. 
INTRODUCTION A35 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 76 ft above base of section. 

Quadrangle name ______ Austerlitz, Ky. 

Section name ----------Type section, Strodes Creek Member. 

Collection number -----7333-CO*. 

Geographic location ----The same as for 7330-CO. 

Coordinates ----------- Do. 

Formation ------------Tongue of Clays Ferry Formation. 

Stratigraphic position __ 71 ft above base of section. 

Quadrangle name ______ Austerlitz, Ky. 

Section name ----------Type section, Strodes Creek Member. 

Collection number -----7334-CO*. 

Geographic· location ____ The same as for 7330-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 66 ft above base of section. 

Quadrangle name ______ Austerlitz, Ky. 

Section name ----------Type section, Strodes Creek Member. 

Collection number _____ 7335-CO*. 

Geographic location ----The same as for 7330-CO. 

Coordinates ----------- Do. 

Formation ------------Tongue of Clays Ferry Formation. 

Stratigraphic position __ 61 ft above base of section. 

Quadrangle name ______ Austerlitz, Ky. 

Section name ----------Type section, Strodes Creek Member. 

Collection number -----7336-CO*. 

Geographic location ____ The same as for 7330-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 32 ft above base of section in Allonychia flanaganensis Zone. 

Quadrangle name ______ Austerlitz, Ky. 

Section name ----------Type section, Strodes Creek Member. 

Collection number _____ 7337-CO*. 

Geographic location ____ The same as for 7330-CO. 

Coordinates ----------- Do. 

Formation ------------Tanglewood Limestone Member, 

Lexington Limestone. 

Stratigraphic position __ 22 ft above base of section. 

Quadrangle name ______ Austerlitz, Ky. 

Section name ----------Type section, Strodes Creek Member. 

Collection number _____ 7343-C0*.8 

Collection number ----- 7344-CO*. 

Geographic location ____ East side U.S. Route 27, 900 ft from 

highway, 0.4 mi north of Lair, Ky. 

Coordinates ___________ 246 mm east, 439 mm north. 

Formation ____________ Near top of lower tongue of Millersburg Member, Lexington Limestone. 

Silicified --------------Yes (7.5 lbs). 

Quadrangle name ______ Shawhan, Ky. 

s This collection number was applied to a recollection of 6900-CO and 

all information which applies to 6990-CO also applies to 7343-CO. 

Collection number _____ 7345-CO*. 

Geographic location _.:.. __ The same as for 6142-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower tongue of Clays Ferry Formation. 

Stratigraphic position __ 20-22 ft above the base of the 

section. 

Silicified --------------Yes (10 lbs). 

Quadrangle name ------Cynthiana, Ky. 

Collection number _____ 7348-CO*. 

Geographic location ____ 4,300 ft east, 6,300 ft south of the 

northwest corner of the Shawhan 

Quadrangle. 

Coordinates ___________ 54 mm east, 493 mm north. 

Formation ------------Tongue of Clays Ferry Formation 

underlain by tongue of Millersburg Member, Lexington Limestone, and overlain by a tongue of 

Tanglewood Limestone Member, 

Lexington Limestone. 

Stratigraphic position __ Float, 4 ft above 810-ft contour. 

Silicified ________ ...; _____ Yes (181 lbs). 

Quadrangle name ______ Shawhan, Ky. 

Collection number _____ 7349-CO*. 

Geographic location ____ The same as for 7348-CO. 

Coordinates ----------- Do. 

Formation ------------ Do. 

Stratigraphic position __ Float, 5 ft above 810-ft contour. 

Silicified --------------Yes (210 lbs). 

Quadrangle name ______ Shawhan, Ky. 

Collection number _____ 7350-CO*. 

Geographic loc-ation ____ The same as for 7348-CO. 

Coordinates ----------- Do. 

Formation ------------ Do. 

Stratigraphic position __ Float, 6 ft above 810-ft contour. 

Silicified --------------Yes (84 lbs). 

Quadrangle name ______ Shawhan, Ky. 

Collection number _____ 7353-CO':'. 

Geographic location ____ 1 mi east northeast junction of Cook 

Road and Lair Road in stock pond. 

Coordinates ___________ 428 mm east, 471 mm north. 

Formation ____________ Lower tongue of Millersburg Member, Lexington Limestone. 

Silicified --------------Yes (354 lbs). 

Quadrangle name ______ Shawhan, Ky. 

Collection number _____ 7448-CO. 

Geographic location ____ Section along road to U.S. Route 25, 

0.4 miles west of Sadieville, Ky. 

Coordinates ___________ Base of section at 295 mm east, 63 

mm north. 

Formation ____________ Clays Ferry Formation tongue. 

Stratigraphic position __ 1 ft above base of section. 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number -----7450-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 
A36 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Formation ____________ Clays -Ferry Formation tongue. 

Stratigraphic position __ 5 ft above the ·base of the section. 

Silicified --------------Yes (50 )bs). 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number _____ 7452-CO*. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation tongue. 

Stratigraphic position __ 10 ft above the base of the section. 

Silicified --------------Yes ( 43 lbs). 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number _____ 7454-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 20 ft :;tbove the base of the section. 

Silicified --------------Yes (70 lbs). 

Quadrangle name ______ Sadieville, Ky. 

Section name ----------Sadieville C. 

Section number ________ 192. 

Collection number _____ 7455-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic· position __ 22 ft above the· base of the section. 

Silicified --------------Yes ( 45 lbs). 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number _____ 7456-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 30 ft above the base of the section. 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number _____ 7457-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 32 ft above the base of the section. 

Silicified --------------Yes (52 lbs). 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number _____ 7458-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation tongue. 

Stratigraphic position __ 35 ft above the base of the section. 

Silicified --------------Yes (16 lbs). 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number _____ 7 459-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation tongue. 

Stratigrapic position __ 50ft above the base of the section. 

Silicified --------------Yes. 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number ----- 7460-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ------------Clays Ferry Formation tongue. 

Stratigraphic position __ 55 ft above the base of the section. 

Silicified --------------Yes. 

Quadrangle name ______ Sadieville, Ky. 

Section name ----------Sadieville C. 

Section number ________ 192. 

Collection number -----7461-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation tongue. 

Stratigraphic position __ 50-55 ft above the base of the 

section. 

Silicified --------------Yes (60 lbs). 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number _____ 7462-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation Tongue. 

Stratigraphic position __ 57 ft above the base of the section. 

Quadrangle name ______ Sadieville, Ky. 

Section name ---------_Sadieville C. 

Section number ________ 192. 

Collection number ----- 7467-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ------------Tanglewood Limestone Member, 

Lexington Limestone. 

Stratigraphic position __ 77 ft above the base of the section. 

Quadrangle name ______ Sadieville, Ky. 

Section name ----------Sadieville C. 

Section number ________ 192. 

Collection number _____ 7468-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 82 ft above the base· of the section. 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 
INTRODUCTION A37 

Collection number ----- 7471-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ------------ Clays Ferry Formation. 

Stratigraphic position __ 97 ft above the base of the section. 

Quadrangle name ______ Sadieville, Ky. 

Section name ---------- Sadieville C. 

Section number-------- 192. 

Collection number _____ 7472-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position --100 ft above the base of the section. 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number _____ 7475-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ------------Clays Ferry Formation. 

Stratigraphic position __ 115 ft above the base of the section. 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number ----- 7477-CO. 

Geographic location ____ The same as for 7448-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 142 ft above the base of the section. 

Quadrangle name ______ Sadieville, Ky. 

Section name ----------Sadieville C. 

Section number ________ 192. 

Collection number _____ 7478-CO. 

Geographic location ____ The same as for '1448-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 145-148 ft above the base of the 

section. 

Quadrangle name ______ Sadieville, Ky. 

Section name __________ Sadieville C. 

Section number ________ 192. 

Collection number -----7702-CO*. 

Geographic location ____ Railroad cut southeast from Agawam station, 1.5 mi south of 

Ruckerville, Ky. 

Coordinates ___________ Base of section at 142 mm east, 

176.5 mm north. 

Formation ------------Grant Lake Limestone. 

Stratigraphic position __ 51.4 ft above base of section. 

Quadrangle name ------Hedges, Ky. 

Section name ----------Agawam South. 

Section number ________ 26. 

Collection number _____ 7703-CO*. 

Geographic location ____ The same as for 7702-CO. 

Coordinates ----------- Do. 

Formation ------------Grant Lake Limestone. 

Stratigraphic position __ 41.6 ft above the base of the section. 

Silicified --------------Yes. 

Quadrangle name ______ Hedges, Ky. 

Section name __________ Agawam South. 

Section number ________ 26. 

Collection number _____ 7704-CO*. 

Geographic· location ____ The same as for 7702-CO. 

Coordinates ----------- Do. 

Formation ____________ Grant Lake Limestone. 

Stratigraphic position __ 38.9 ft above the base of the section. 

Silicified --------------Yes. 

Quadrangle name ______ Hedges, Ky. 

Section name __________ Agawam South. 

Section number ________ 26. 

Collection number _____ 7705-CO*. 

Geographic location ____ The same as for 7702-CO. 

Coordinates ----------- Do. 

Formation ____________ Grant Lake Limestone. 

Stratigraphic position __ 27.2 ft above the base of the section. 

Quadrangle name ______ Hedges, Ky. 

Section name __________ Agawam South. 

Section number ________ 26. 

Collection number _____ 7706-CO*. 

Geographic location ____ The same as for 7702-CO. 

Coordinates ----------- Do. 

Formation ------------Grant Lake Limestone. 

Stratigraphic position __ 21.8 ft above the base of the section. 

Quadrangle name ______ Hedges, Ky. 

Section name __________ Agawam South. 

Section numbe·r ________ 26. 

Collection number _____ 7707-CO*. 

Geographic- location ____ The same as for 7702-CO. 

Coordinates ----------- Do. 

Formation ------------Grant Lake Limestone. 

Stratigraphic position __ 8.3 ft above the base of the· section. 

Quadrangle name ______ Hedges, Ky. 

Section name __________ Agawam South. 

Section number ________ 26. 

Collection number _____ 7708-CO*. 

Geographic postion ____ The same as for 7702-CO. 

Coordinates ----------- Do. 

Formation ____________ Grant Lake Limestone. 

Stratigraphic position __ 7.9 ft above the ba.se of the section. 

Quadrangle name ------Hedges, Ky. 

Section name __________ Agawam South. 

Section number ________ 26. 

Collection number _____ 7782-CO. 

Geographic location ____ The same as for 5081-CO. 

Coordinates ----------- Do. 

Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ Lower 5 ft of Curdsville Limestone 

Member. 

Silicified --------------Yes (655 lbs). 

Quadrangle name ______ Tyrone, Ky. 

Section name ----------Tyrone C. 

Section number ________ 174. 
A38 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Collection number _____ 7784-CO. 

Geographic location ____ U.S. Route 27, 0.3 mi southeast of 

crossing of Kentucky River 

Bridge on south side of road. 

Coordinates ___________ 41 mm east, 75 mm north. 

Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ Basal 2 ft of Curdsville Limestone 

Member. 

Silicified --------------Yes (788 lbs). 

Quadrangle name ______ Little Hickman, Ky. 

Collection number _____ 7785-CO. 

Geographic location ____ The same as for 7784-CO. 

Coordinates ----------- Do. 

Formation ____________ Curdsville Limestone Member, Lexington Limestone. 

Stratigraphic position __ ll-12 ft above the base of Curdsville 

Limestone Member. 

Silicified --------------Yes (359 lbs). 

Quadrangle name ------Little Hickman, Ky. 

Collection number _____ 7789-CO. 

Geographic location ____ Eastbound lanes of Interstate Route 

64 (both north and south sides), 

0.8 mi east of Kentucky River 

bridge crossing. 

Coordinates -----------The same as for 5095-CO. 

Formation ------------Upper part of Devils Hollow Member, Lexington Limestone. 

Silicified --------------Yes ( 422 lbs). 

Quadrangle name ______ Frankfort East, Ky. 

Section name __________ Frankfort East A. 

Section number ________ 86. 

Collection number _____ 7790-CO. 

Geographic location ____ Jones Lane Branch Road, 0.85 mi 

northwest of junction with Watkinsville Road ; west side of Jones 

Lane Branch Road. 

Coordinates ___________ 10.5 mm east, 552 mm north. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Silicified --------------Yes (172 lbs). 

Quadrangle name ______ Midway, Ky. 

Collection number _____ 7791-CO. 

Geographic location ____ The same as for 4940-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Logana Member, Lexington Limestone. 

Stratigraphic position __ 35 ft above Tyrone Limestone-Lexington Limestone contact. 

Silicified ---------- ____ Yes ( 427 lbs). 

Quadrangle name ______ Salvisa, Ky. 

Section name ----------Salvisa B. 

Section number ________ 176. 

Collection number _____ 7792-CO. 

Geographic location ____ The same as for 5067-CO. 

Coordinates -----------The same as for 5067-CO. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 170 ft above the top of the Tyrone 

Limestone. 

Silicified --------------Yes (169 lbs). 

Quadrangle name ______ Ford, Ky. 

Collection number _____ 7793-CO. 

Geographic location ____ U.S. Route 227, 0.2 mi south of road 

to Boonesboro Beach. 

Coordinates ___________ 400 mm east, 82.5 mm north. 

Formation ------------Tongue of Tanglewood Limestone 

Member, Lexington Limestone, 

overlain and underlain by Clays 

Ferry Formation. 

Stratigraphic position __ 15 ft below abundant Sowerbyella 

in Clays Ferry Formation. 

Quadrangle name ______ Ford, Ky. 

Collection number _____ 7805-CO. 

Geographic location ____ The same as for 6211-CO. 

Coordinates ----------- Do. 

Formation ------------Uppermost part of Point Pleasant 

Tongue, Clay Ferry Formation. 

Quadrangle name ______ Moscow, Ohio-Ky. 

Section name __________ Bear Creek. 

Collection number _____ 7806-CO. 

Geographic location ____ The same as for 6211-CO. 

Formation ____________ Point Pleasant Tongue, Clays Ferry 

Formation. 

Stratigraphic position __ 5 ft below top of Point Pleasant 

Tongue, Clays Ferry Formation. 

Quadrangle name ______ Moscow, Ohio-Ky. 

Section name __________ Bear Creek. 

Collection number _____ 7809-CO. 

Geographic location ____ 75 ft south of junction Kentucky 

Route 388 and U.S. Route 227. 

Coordinates ___________ 384 mm east, 113 mm north. 

Formation ------------Tanglewood Limestone Member, Lexington Limestone. 

Stratigraphic position __ First bed above Brannon MemberTanglewood Limestone Member 

contact. 

Silicified --------------Yes (205 lbs). 

Quadrangle name· ______ Ford, Ky. 

Section name __________ Boonesboro Beach. 

Collection number _____ 7812-CO. 

Geographic location ____ Farm pond 250 ft west of U.S. 

Route 27, 500 ft south of junction 

of U.S. Routes 27 and 62. 

Coordinates ___________ 220 mm east, 548 mm north. 

Formation ____________ Clays Ferry Formation. 

Silicified --------------Yes (170 lbs). 

Quadrangle name' ______ Shawhan, Ky. 

Collection number _____ 7834-CO. 

Geographic location ____ U.S. Route 50 1.6 miles east of Versailles, Ind. 

Coordinates ___________ 86.5 mm east, 297 mm north. 

Formation ------------Uppermost part of Dillsboro Formation. 

Silicified --------------Yes (242 lbs). 

Quadrangle· name· ______ Milan, Ind. 
INTRODUCTION A39 

Collection number ----- 7836-CO. 

Geographic location ____ Section on U.S. Route 27, 1 mi south 

of intersection with road to Camp 

Nelson National Cemetery. 

Coordinates -----------Top of section at 60 mm east, 113.5 

mm north. 

Formation ------------Upper part of Camp Nelson Limestone. 

Silicified --------------Yes (217 lbs). 

Quadrangle name ______ Little Hickman, Ky. 

Section name ----------Type section Camp Nelson Limestone. 

Collection number _____ 7875-CO. 

Geographic location ____ Exposures along road up from Kentucky River lock number 7 to 

High Bridge, Ky. and junction 

with Kentucky Route 29; 1,000 ft 

west of high-level railroad bridge 

over Kentucky River. Base of section taken at U-shaped bend in 

road, between two pillars on 

road leading to dam at lock number 7. 

Coordinates ___________ Base of section at 97.5 mm east, 

34 7 mm north. 

Formation ____________ Camp Nelson Limestone. 

Stratigraphic position __ 60.5 ft above base of section. 

Silicified --------------Yes (100 lbs). 

Quadrangle name ------Wilmore, Ky. 

Section name __________ High Bridge. 

Collection number _____ 7936-CO*. 

Geographic location ____ The same as for 7702-CO. 

Coordinates ----------- Do. 

Formation ____________ Grant Lake Limestone. 

Silicified --------------Yes. 

Quadrangle name ______ Hedges, Ky. 

Section name __________ Agawam South. 

Section number ________ 26. 

Collection number _____ 7937-CO*. 

Geographic location ____ The same as for 7702-CO. 

Coordinates ----------- Do. 

Formation ____________ Grant Lake Limestone. 

Silicified --------------Yes. 

Quadrangle name ______ Hedges, Ky. 

Section name __________ Agawam South. 

Section number ________ 26. 

Collection number ----- 7978-CO. 

Geographic location ____ Exposures along Moffett Road, 0.5 

mi west of Kenton, Ky. 

Coordinates ___________ Base of section at 118.5, mm east, 

547 mm north. 

Formation ------------ Kope Formation. 

Stratigraphic position __ 40-43 ft above Point Pleasant 

Tongue of Clays Ferry FormationKope Formation contact. 

Quadrangle name------ De Mossville, Ky. 

Section name __________ Moffett Road. 

Collection number -.,---- 7984-CO. 

Geographic location ____ The same as for 7978-CO. 

Coordinates Do. 

Formation ____________ Kope Formation. 

Stratigraphic position __ 57 ft above Point Pleasant Tongue 

of Clays Ferry Formation-Kope 

Formation contact. 

Quadrangle name ______ De Mossville, Ky. 

Section name __________ Moffett Road. 

Collection number _____ 8068-CO. 

Geographic location ____ The same as for 7978-CO. 

Coordinates ----------- Do. 

Formation ____________ Point Pleasant Tongue, Clays Ferry 

Formation. 

Stratigraphic position __ 2-3 ft above the base of the section. 

Silicified --------------Yes (150 lbs). 

Quadrangle name ______ De Mossville, Ky. 

Section name __________ Moffett Road. 

Collection number _____ D-1106-CO*. 

Geographic location ____ Kentucky Route 35, 0.3 mi southeast 

of crossing with Elkhorn Creek. 

Coordinates ___________ Base of section at 115 mm east, 281 

mm north. 

Formation ____________ Macedonia Bed, Grier Limestone 

Member, Lexington Lime.stone. 

Stratigraphic position __ 20 ft above the base of the section. 

Quadrangle name ______ Switzer, Ky. 

Section name __________ Switzer A. 

Section number ________ 61. 

Collection number _____ D-1115-CO*. 

Geographic location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 

Formation ------------Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 78 ft above the base of the section. 

Quadrangle name ------Switzer, Ky. 

Section name ----------Switzer A. 

Section number --------61. 

Collection number _____ D-1117-CO*. 

Geographic location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 85 ft above the base of the section. 

Quadrangle name ______ Switzer, Ky. 

Section name ____ ------Switzer A. 

Section number --------61. 

Collection number _____ D-1119-CO*. 

Geographic location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 

Formation ____________ Stamping Ground Member, Lexington Limestone. 

Stratigraphic position __ 105 ft above the base of the section. 

Quadrangle name ______ Switzer, Ky. 

Section name ----------Switzer A. 

Section number ________ 61. 

Collection number _____ D-1120-CO*. 

Geographic location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 
A40 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Formation ____________ Base of Stamping Ground Member, 

Lexington Limestone. 

Stratigraphic position __ 101 ft above the base of the .section. 

Quadrangle name _, _____ Switzer, Ky. 

Section name __________ Switzer A. 

Section number ________ 61. 

Collection number _____ D-1121-CO*. 

Geographic location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 

Formation ____________ Stamping Ground Member, Lexington Limestone. 

Stratigraphic position __ 111 ft above the base of the section. 

Quadrangle name ______ Switzer, Ky. 

Section name __________ Switzer A. 

Section number ________ 61. 

Collection number _____ D-1122-CO*. 

Geographic, location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 

Formation ____________ Stamping Ground Membe,r, Lexington Limestone. 

Stratigraphic position __ 120 ft above the base of the section. 

Quadrangle name ______ Switzer, Ky. 

Section name ----------Switzer A. 

Section number ________ 61. 

Collection number _____ D-1123-CO*. 

Geographic location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 

Formation ____________ Stamping Ground Member, Lexington Limestone. 

Stratigraphic position __ 118 ft above the base of the section. 

Quadrangle name ------Switzer, Ky. 

Section name ----------Switzer A. 

Section number --------61. 

Collection number _____ D-1125-CO*. 

Geographic location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 

Formation ------------ Tanglewood Limestone Member, Lexington Limestone. 

Stratigraphic position __ 140 ft above the base of the .section. 

Quadrangle name ______ Switzer, Ky. 

Section name ----------Switzer A. 

Section number ________ 61. 

Collection number _____ D-1129-CO*. 

Geographic location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 175 ft ab~ve the base of the section. 

Quadrangle name ______ Switzer, Ky. 

Section name ----------Switzer A. 

Section number ________ 61, 

Collection number _____ D-1132-CO*. 

Geographic location ____ The same as for D-1106-CO. 

Coordinates ----------- Do. 

Formation ____________ Nicholas Bed, Tanglewood Limestone Member, Lexington Limestone. 

Stratigraphic position __ 195 ft. above the base of the section. 

Quadrangle name ______ Switzer, Ky. 

Section name __________ Switzer A. 

Section number ________ 61. 

Collection number _____ D-1169-CO*. 

Geographic location ____ Old road to lower Clays Ferry, Ky., 

Bridge, section beginning about 

1,750 ft west of the high bridge 

piers for the new Interstate Route 

75 bridge crossing of the Kentucky River. 

Coordinates ___________ Base of section at 132 mm east, 31 

mm north. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 8 ft above top of Tanglewood Limestone Member, Lexington Limestone. 

Quadrangle name ______ Ford, Ky. 

Section name __________ Clays Ferry (lower part); Ford A. 

Section number ________ 22B. 

Collection number _____ D-1170-Co•:•. 

Geographic location ____ The same as for D-1169-CO. 

Coordinates ----------- Do. 

Formation ------------Clays Ferry Formation. 

Stratigraphic position __ 10 ft above top of Tanglewood Limestone Member, Lexingon Limestone. 

Quadrangle name ______ Ford, Ky. 

Section name __________ Clays Ferry (lower part); Ford A. 

Section number ________ 22B. 

Collection number _____ D-1171-CO*. 

Geographic location ____ The same as for D-1169-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 15 ft above top of Tanglewood 

Limestone Member, Lexington 

Limestone. 

Quadrangle name ______ Ford, Ky. 

Section name ----------Clays Ferry (lower part); Ford A. 

Section number ________ 22B. 

Collection number _____ D-1172-CO*. 

Geographic location ____ The same as for D-1169-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 24ft above top of Tanglewood Limestone Member, Lexington Limestone. 

Silicified --------------Yes (109 lbs). 

Quadrangle name ______ Ford, Ky. 

Section name __________ Clays Ferry (lower part); Ford A. 

Section number ________ 22B. 

Collection number _____ D-1173-CO*. 

Geographic- location ____ The same as for D-1169-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 30 ft above top of Tanglewood Limestone Member, Lexington Limestone. 

Quadrangle name ______ Ford, Ky. 
INTRODUCTION A41 

Section name __________ Clays Ferry (lower part); Ford A. 

Section number ________ 22B. 

Collectioti number -----D-1174-Co•:•. 

Geographic location ____ The same as for D-1169-CO. 

Coordinates ----------- Do. 

Formation ------------Clays Ferry Formation. 

Stratigraphic position __ 38 ft above top of Tanglewood Limestone Member, Lexington Limestone. 

Quadrangle name ______ Ford, Ky. 

Section name __________ Clays Ferry (lower part); Ford A. 

Section number ________ 22B. 

Collection number ----- D-1178-CO*. 

Geographic location ____ The same a.s for D-1169-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 56ft above top of Tanglewood Limestone Member, Lexington Limestone. 

Quadrang·le name ------Ford, Ky. 

Section name ----------Clays Ferry (lower part); Ford A. 

Section number ________ 22B. 

Collection number _____ D-1179-CO*. 

Geographic location ____ The same as for D-1169-CO. 

Coordinates -----------The same as for D-1169-CO. 

Formation ____________ Clay Ferry Formation. 

Stratigraphic· position __ 74ft above top of Tanglewood Limestone Member, Lexington Limestone. 

Quadrangle name ______ Ford, Ky. 

Section name __________ Clays Ferry (lower part) ; Ford A. 

Section number ________ 22B. 

Collection number _____ D-1180-CO*. 

Geographic location ____ The same as for D-1169-CO. 

Coordinates ----------- Do. 

Formation ____________ Clays Ferry Formation. 

Stratigraphic position __ 76 ft above top of Tanglewood Limestone Member, Lexington Limestone. 

Quadrangle name ______ Ford, Ky. 

Section name __________ Clays Ferry (lower part); Ford A. 

Section number ________ 22B. 

Collection number _____ D-1196-CO*. 

Geog-raphic location ____ Eastbound lanes of Interstate Route 

64 from Kentucky River bridge 

crossing to end of exposures. 

Coordinates ___________ Base of section at 88 mm east, 164 

mm north. 

Formation ------------Top of Logana Member, Lexington 

Limestone. 

Stratigraphic position __ 50ft above top of Tyrone Limestone. 

Silicified --------------Yes (250 lbs). 

Quadrangle name ______ Frankfort East, Ky. 

Section name __________ Frankfort East A. 

Section number ________ 86. 

Collection number _____ D-1200-CO*. 

Geographic location ____ Westbound lanes of Interstate Route 

64, exposures beginning about 0.5 

mi east of bridge crossing of Kentucky River. 

Coordinates ___________ Base of collected section at 112.5 mm 

east, 188 mm north. 

Formation ------------Tanglewood Limestone Member, Lexington Limestone. 

Stratigraphic position __ 205 ft above top of Tyrone Limestone. 

Quadrangle name ______ Frankfort East, Ky. 

Section name __________ Frankfort East A. 

Section number ________ 86. 

Collection number _____ D-1204-CO*. 

Geographic location ____ The .same as for D-1200-CO. 

Coordinates ----------- Do. 

Formation ------------Tanglewood Limestone Member, Lexington Limestone. 

Stratigraphic position __ 230 ft above top of Tyrone Limestone. 

Quadrangle· name ______ Frankfort East, Ky. 

Section name __________ Frankfort East A. 

Section number ________ 86. 

Collection number -----D-1207-CO*. 

Geographic location ____ The same as for D-1200-CO. 

Coordinates ----------- Do. 

Formation ____________ Devils Hollow Member, Lexington 

Limestone. 

Stratigraphic position __ 256 ft above top of Tyrone Limestone. 

Quadrangle name ______ Frankfort East, Ky. 

Section name __________ Frankfort East A. 

Section number ________ 86. 

Collection number -----D-1239-CO*. 

Geographic location ____ Road exposure running parallel to 

Mason County and Lewis County 

boundary line in the northeast 

corner of the Orangeburg quadrangle and the southeast corner 

of the Maysville East quadrangle. 

Coordinates ___________ Base of section at 425 mm east, 559 

mm north in the Orangeburg 

quadrangle. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 7-13 ft above base of Bull Fork 

Formation. 

Quadrangle name• ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1241-CO*. 

Geographic loc·ation ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 11 ft above base of Bull Fork Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1243-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 
A42 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Stratigraphic position __ 22 ft above base of Bull Fork Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number -----D-1244-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ------------Bull Fork Formation. 

Stratigraphic position __ 23 ft above base of Bull Fork Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number -----D-1246-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 28-35 ft above base of Bull Fork 

Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1247-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 36 ft above base of Bull Fork Formation. 

Quadrangle name------ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1248-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 38 ft above base of Bull Fork Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1250-CO*. 

Geographic location ____ The same a.s for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 56-61 ft above base of Bull Fork 

Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1251-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ Float at 56-61 ft above base of Bull 

Fork Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1252-CO*. 

Geographic loca.tion ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 71 ft above base of Bull Fork Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1253-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic postion __ 91 ft above base of Bull Fork Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1254-CO* 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 101-106 ft above base of Bull Fork 

Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number ----- D-1255-CO*. 

Geographic location ____ The sa!lle as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 96-111 ft above base of Bull Fork 

Formation. 

Quadrangle name ______ Orang"~eburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1256-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratgraphic position __ 106-111 ft above base of Bull Fork 

Formation. 

Quadrangle name ______ Orangeburg, Ky. 

S.ection name __________ County Line. 

Collection number _____ D-1258-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 144 ft above base of Bull Fork Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number _____ D-1259-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 149-154 ft above base of Bull Fork 

Formation. 

Quadrangle name ______ Maysville East, Ohio-Ky. 

Section name __________ County Line. 

Collection number _____ D-1260-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 
INTRODUCTION A43 

Stratigraphic position __ 169 ft above base of Bull Fork Formation. 

Quadrangle name ______ Maysville East, Ohio-Ky. 

Section name __________ County Line. 

Collection number _____ D-1263-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 189-194 ft above base of Bull Fork 

Formation. 

Quadrangle name ______ Maysville East, Ohio-Ky. 

Section name __________ County Line. 

Collection number -----D-1265-CO*. 

Geographic location ____ The same as for D-1239-CO. 

Coordinates ----------- Do. 

Formation ____________ Bull Fork Formation. 

Stratigraphic position __ 126-131 ft above base of Bull Fork 

Formation. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ County Line. 

Collection number -----D-1267-CO. 

Geographic location ____ The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation. ------------Tate Member, Ashlock Formation,, 

Stratigraphic position __ 10 ft above base of the· section. 

Quadrangle name ______ Maud, Ky. 

Section name __________ Fredericktown. 

Collection number _____ D-1273-CO. 

Geographic· location ____ The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation ____________ Gilbert Member, Ashlock Formation. 

Stratigraphic position __ 47 ft above the base of the section. 

Quadrangle name ______ Maud, Ky. 

Section name __________ Fredericktown. 

Collection number _____ D-1276-CO. 

Geographic location ____ The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation ------------Upper tongue of Grant Lake Limestone. 

Stratigraphic position __ 73 ft above the base of the section. 

Quadrangle name ______ Maud, Ky. 

Section name __________ Fredericktown. 

Collection number _____ D-1277-CO. 

Geographic location ____ The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation ------------Upper tongue of Grant Lake Limestone. 

Stratigraphic position __ 81 ft above the base of the section. 

Quadrangle name ______ Maud, Ky. 

Section name __________ Fredericktown. 

Collection number _____ D-1280-CO. 

Geographic location ____ The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation ------------Upper tongue of Grant Lake Limestone. 

Stratigraphic position __ 97 ft above the base of the section. 

Quadrangle name ______ Maud, Ky. 

Section name __________ Fredericktown. 

Collection number _____ D-1288-CO. 

Geographic location ____ The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation · ____________ Bardstown Member, Drakes Formation. 

Stratigraphic position __ 167 ft above the base of the section. 

Quadrangle name ______ Maud, Ky. 

Section name __________ Fredericktown. 

Collection number _____ D-1289-CO. 

Geographic location ____ The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation ------------Top of Bardstown Member, Drakes 

Formation. 

Stratigraphic position __ 175 ft above base of section. 

Quadrangle name ______ Maud, Ky. 

Section name __________ Fredericktown. 

Collection number _____ D-1292-CO. 

Geographic location ____ The same as for 4208-CO. 

Coordinates ----------- Do. 

Formation ____________ Bardstown Member, Drakes Formation. 

Stratigraphic position __ 156 ft above the base of the section. 

Quadrangle name ______ Maud, Ky. 

Section name __________ Fredericktown. 

Collection number _____ D-1295-CO. 

Geographic location ____ 1.7 mi southeast of Gratz, Ky. on 

Kentucky Route 355 (north bluff 

of Clements Bottom). 

Coordinates ___________ Base of .section at 280· mm east, 

416 mm north. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 21 ft above the base of the section. 

Quadrangle name ______ Gratz, Ky. 

Section name __________ Gratz A. 

Section number ________ 62. 

Collection number _____ D-1301-CO. 

Geographic location ____ The same as for D-1295-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington 

Limestone. 

Stratigraphic position __ 32 ft above the base of the section. 

Quadrangle name ______ Gratz, Ky. 

Section name· __________ Gratz A. 

Section number ________ 62. 

Collection number _____ D-1309-CO. 

Geographic location ____ The same as for D-1295-CO. 

Coordinates ----------- Do. 

Formation ____________ Possibly Grier Limestone Member, 

Lexington Limestone, or tongue of 

Clays Ferry Formation. 

Stratigraphic position __ 70 ft above the base of the section. 

Quadrangle name ______ Gratz, Ky. 

Section name __________ Gratz A. 

Section number ________ 62. 
A44 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Collection number _____ D-1310-CO. 

Geographic location ----The same as for D-1295-CO. 

Coordinates ----------- Do. 

Formation ____________ Either Grier Limestone Member, 

Lexington Limestone or tongue of 

Clays Ferry Formation. 

Stratigraphic position __ 75-76 ft above the base of the 

section. 

Quadrangle name ______ Gratz, Ky. 

Section name __________ Gratz A. 

Section number ________ 62. 

Collection number _____ D-1312-CO. 

Geographic location ____ The same as for D-1295-CO. 

Coordinates ----------- Do. 

Formation ____________ Millersburg Member, Lexington 

Limestone. 

Stratigraphic position __ 120 ft above the base of the section. 

Quadrangle name ______ Gratz, Ky. 

Section name __________ Gratz A. 

Section number ________ 62. 

Collection number _____ D-1314-CO':'. 

Geographic location ____ Section along Kentucky Route 1449, 

beginning about 0.7 mi south of 

junction with Kentucky Route 10. 

Section extends along Route 1449 

from southwest corner of the 

Maysville East quadrangle to the 

northwest corner of the Orangeburg quadrangle. 

Coordinates ___________ Base of section at 114.5 mm east, 

12 mm north in the Maysville East 

quadrangle. 

Formation ____________ Kope Formation. 

Stratigraphic position __ 46 ft above the base of the section. 

Quadrangle name ______ Maysville East, Ohio-Kentucky. 

Section name ----------Sleepy Hollow, Sleepy Hollow is the 

name applied to the eastern tributary of Kennedy Creek. The 

name Slee:py Hollow is also applied to the valley immediately 

west of Kennedy Creek Valley. 

The Sleepy Hollow referred to 

here is the eastern tributary of 

Kennedy Creek. 

Collection number _____ D-1327-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Fairview Formation. 

Stratigraphic position __ 122ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name ----------See D-1314-CO. 

Collection number _____ D-1330-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Basal part of Grant Lake Limestone. 

Stratigraphic· position __ 132 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1332-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Grant Lake Limestone .. 

Stratigraphic position __ 135 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1333-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Grant Lake Limestone. 

Stratigraphic position --138 ft above the base of the section. 

(float). 

Quadrangle name ______ Orangeburg, Ky. 

Section name ----------See D-1314-CO. 

Collection number _____ D-1334-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Grant Lake Limestone. 

Stratigraphic position __ 138 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1335-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Grant Lake Limestone. 

Stratigraphic position __ 139 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1336-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Grant Lake Limestone. 

Stratigraphic position __ 140 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number -----D-1337-CO*. 

Geographic location ----The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Grant Lake Limestone. 

Stratigraphic position __ 141 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name ----------See D-1314-CO. 

Collection number -----D-1338-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Grant Lake Limestone. 

Stratigraphic position __ 142 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1339-CO*. 

Geographic· location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Grant Lake Limestone. 
INTRODUCTION A45 

Stratigraphic position __ 152 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1340-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Grant Lake Limestone. 

Stratigraphic position __ 146 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number -----D-1341-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Grant Lake Limestone. 

Stratigraphic position __ 165 ft above the base of the section. 

Quadrangle name ------Orangeburg, Ky. 

Section name---------- See D-1314-CO. 

Collection number _____ D-1342-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Grant Lake Limestone. 

Stl·atigraphic position __ 176 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-Co. 

Collection number _____ D-1343-CO*. 

Geographic· location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Lower part of Grant Lake Limestone. 

Stratigraphic position __ 183 ft above the base of the section. 

Quadrang·le name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1344-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Grant Lake Limestone. 

Stratigraphic position __ 201 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1345-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ---------- __ Upper part of Grant Lake Limestone. 

Stratigraphic position __ 218 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1346-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Grant Lake Limestone. 

Stratigraphic position __ 224 ft above the base of the section. 1 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number -----D-1347-CO*. 

Geographic· location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ------------Upper part of Grant Lake Limestone. 

Stratigraphic position __ 225-230 ft above the base· of the 

section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1348-CO*. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ------------Uppermost part of Grant Lake 

Limestone. 

Stratigraphic position __ 235 ft above the base of the section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1349-CO. 

Geographic location ____ The same as for D-1314-CO. 

Coordinates ----------- Do. 

Formation ____________ Grant Lake Limestone. 

Stratigraphic position __ 140-143 ft above the base of the 

section. 

Quadrangle name ______ Orangeburg, Ky. 

Section name __________ See D-1314-CO. 

Collection number _____ D-1365-CO*. 

Geographic location ____ Section in roadcut on Interstate 

Route 75 beginning 0.4 mi south 

of bridge over Kentucky River. 

Coordinates ___________ Base of section at 150.5 mm east, 

57 4 mm north. 

Formation ____________ Calloway Creek Limestone. 

Stratigraphic position __ 56-61 ft above base of Calloway 

Creek Limestone. 

Quadrangle name ______ Richmond North, Ky. 

Section name ----------Type section Calloway Creek Limestone (Weir, Greene, and Simmons, 1965). 

Collection number _____ D-1367-CO*. 

Geographic location ____ The same as for D-1365-CO. 

Coordinates ----------- Do. 

Formation ____________ Calloway Creek Limestone. 

Stratigraphic position __ 73-94 ft above base of Calloway 

Creek · Limestone. 

Quadrangle name ______ Richmond North, Ky. 

Section name----------The same as for D-1365-CO. 

Collection number _____ D-1368-CO* .. 

Geographic location ____ The same as for D-1365-CO. 

Coordinates ----------- Do. 

Formation ____________ Calloway Creek Limestone. 

Stratigraphic position __ 94-107 ft above base of Calloway 

Creek Limestone. 

Quadrangle name ______ Richmond North, Ky. 

Section name ----------The same as for D-1365-CO. 
A46 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Collection number _____ D-1369-CO*. 

Geographic location ____ The same as for D-1365-CO. 

Coordinates ----------- Do. 

Formation ____________ Calloway Creek Limestone. 

Stratigraphic position __ 107-124 ft above base of Calloway 

Creek Limestone. 

Quadrangle name ______ Richmond North, Ky. 

Section name ----------The same as for D-1365-CO. 

Collection number _____ D-1370E-CO*. 

Geographic location ____ 17,300 ft north and 14,950 ft west 

of the southeast corner of the 

Richmond North quadrangle. 

Coordinates ___________ 269.5 mm east, 222 mm north. 

Formation ____________ Otter C:reek Coral Bed, Preachersville Member, Drakes Formation. 

Stratigraphic position __ 80 ft below the top of the Drakes 

Formation. 

Quadrangle· name ______ Richmond North, Ky. 

Collection number ----- D-1629-CO. 

Geographic location ____ The same as for 4871-CO. 

Coordinates ----------- Do. 

Formation ____________ Grier Limestone Member, Lexington Limestone. 

Stratigraphic position __ 46 feet above the base of the section. 

Q-gac;lrangle name ------Valley View, Ky. 

Section name ----------Valley View .. C (Antioch Church 

Road). 

Section number ________ 180. 

REFERENCES CITED 

Alberstadt, L. P., 1979, The brachiopod genus Platystrophia: U.S. Geol. Survey Prof. Paper 1066-B, 20 p., 7 pls. 

Anstey, R. L., and Fowler, M. L., 1969, Lithostratigraphy 

and depositional environment of the Eden Shale (Ordovician) in tri-state area of Indiana, Kentucky, and 

Ohio: Jour. Geology, v. 77, p. 668-682, 5 figs. 

Bell, B. M., 1979 Edrioasteroids (Echinodermata) : U.S. 

Geol. Survey Prof. Paper 1066-E, 7 p., 2 pls. 

Bergstr9m, S. M., 1971, Conodont biostratigraphy of the 

Middle and Upper Ordovician of Europe and eastern 

North America: Geol. Soc. America Mem. 127, p. 83-162. 

Bergstrom, S. M., and Sweet, W. C., 1966, Conodonts from 

the Lexington Limestone (Middle Ordovician) of Kentucky and its lateral equivalents in Ohio and Indiana: 

Bulls. Am. Paleontology, v. 50, no. 229, p. 267-441, pis. 

29 p., 5 figs. 

Black, D. F. B., 1974, Geologic map of the Winchester quadrangle, Clark and Madison Counties, Kentucky: U.S. 

Geol. Survey Geol. Quad. Map GQ-1159. 

Black, D. F. B., Cressman, E. R., and MacQuown, W. C., 

Jr., 1965, The Lexington Limestone (Middle Ordovician) 

of central Kentucky: U.S. Geol. Survey Bull. 1224-C, 

29 p., 5 figs. 

Black, D. F. B., and Cuppels, N. P., 1973, Strodes Creek 

Member (Upper Ordovician)-A new map unit in the 

Lexington Limestone of north-central Kentucky: U.S. 

Geol. Survey Bull. 1372-C, 16 p., 7 figs. 

Black, D. F. B., and MacQuown, W. C., Jr., 1965, Lithostratigraphy of the Ordovician Lexington Limestone and 

Clays Ferry Formation of the central Bluegrass area 

near Lexington, Kentucky: Geol. Soc. Kentucky Field 

Guide for Annual Spring Field Conference, p. 1-43, 13 

figs. 

Booth, J. S., and Osborne, R. H., 1971, The American Upper 

Ordovician Standard. XV. Clay mineralogy of insoluble 

residues from Cincinnatian Limestones, Hamilton 

County, Ohio: Jour. Sed. Petrology, v. 41, p. 840-843, 

1 fig. 

Branstrator, J. W., 1979, Asteroidea (Echinodermata): U.S. 

Geol. Survey Prof. Paper 1066-F, 7 p., 3 pls. 

Brown, G. D., Jr., and Anstey, R. L., 1968, Lexington Limestone-Kope Formation contact (Ordovician) in southeastern Indiana: Am. Assoc. Petroleum Geologists Bull., 

v. 52, p. 488-493, 3 figs. 

Brown, G. D., Jr., and Lineback, J. A., 1966, Lithostratigraphy of Cincinnatian Series (Upper Ordovician) in 

southeastern Indiana: Am. Assoc. Petroleum Geologists 

Bull., v. 50, p. 1018-1032, 5 figs. 

Bucher, W. H., Caster, K. E., and Jones, Stewart, 1939, 

Elementary description of Cincinnatian fossils and strata 

and plates of commoner fossils in the vicity of Cincinnati, Ohio: Cincinnati, Univ. Cincinnati, 10 p., 8 pis., 

2 figs. 

Carpenter, J. W., and Ory, T. R., 1961, The American Upper 

Ordovician Standard. VI. The Covington sequence at 

Maysville, Kentucky: Ohio Jour. Sci., v. 61, p. 372-378, 

3 figs. 

Caster, K. E., Dalve, E. A., and Pope, J. K., 1955, Elementary 

guide to the fossils and strata of the Ordovician in the 

vicinity of Cincinnati, Ohio: Cincinnati Mus. Nat. History, 47 p., 8 pls., 6 figs. (Reprinted in 1961). 

Cooper, G. A., 1956, Chazyan and related brachiopods: 

Smithsonian Misc. Colin., v. 127, 10·24 p., 269 pis. 

(Bound in two volumes) . 

Cooper, G. A., and Whittington, H. B., 1965, Use of acids 

in preparation of fossils, in Kummel, Bernard, and Raup, 

David, Handbook of paleontological techniques: San 

Francisco, W. H. Freeman and Co., p. 294-300. 

Cressman, E. R., 1973, Lithostratigraphy and depositional 

environments of the Lexington Limestone (Ordovician) 

of central Kentucky: U.S. Geol. Survey Prof. Paper 

768, 61 p., 11 pls. [197 4]. 

Cressman, E. R., and Karklins, 0. L., 1970, Lithostratigraphy 

and fauna of the Lexington Limestone (Ordovician) of 

central Kentucky, Field Trip No. 2 in Guidebook for 

Field Trips 18th Annual Meeting Southeastern Section 

Geological Soc. America; Lexington, Kentucky Geol. 

Survey, p. 17-28, 19 figs. 

Cressman, E. R., and Noger, M. C., 1976, Tidal-flat carbonate 

environments in the High Bridge (Middle Ordovician) 

of central Kentucky: Kentucky Geol. Survey, Rept. Inv. 

18, 15 p., 1 pl. 

Ethington, R. L., and Sweet, W. C., 1977, Guidebook to field 

excursion 2, of the eastern midcontinent: Third International Symposium on the Ordovician System, Columbus, Ohio, 48 p. 

Ford, J. P., 1967, Cincinnatian geology in southwest Hamilton 

County, Ohio: Am. Assoc. Petroleum Geologists Bull., 

v. 51, p. 918-936, 14 figs. 

---1968, Upper Ordovic-ian stratigraphic relations between 

Covington and Clays Ferry, Kentucky: Am. Assoc. Petroleum Geologists Bull. 52, p. 1779-1791, 5 figs. 

---1972, Bedrock geology of the Addyston quadrangle 

and part of the Burlington quadrangle, Hamilton 

County, Ohio (map): Ohio Div. Geol. Survey Rept. 

Inv. 83. 
INTRODUCTION A47 

---1974, Bedrock geology of the Cincinnati West quadrangle and part of the Covington quadrangle, Hamilton 

County, Ohio (map) : Ohio Div. Geol. Survey Rept. 

lnv. 93. 

Fox, W. T., 1962, Stratigraphy and paleoecology of the Richmond Group in southeastern Indiana: Geol. Soc. America 

Bull., v. 73, p. 621-642, 10 figs. 

Gray, H. H., 1972, Lithostratigraphy of the Maquoketa 

Group (Ordovician) in Indiana: Indiana Geol. Survey 

Indiana Spec. Report 7, 31 p. 

Hatfield, C. B., 1968, Stratigraphy and paleoecology of the 

Saluda Formation (Cincinnatian) in Indiana, Ohio, and 

Kentucky: Geol. Soc. America Spec. Paper 95, 34 p., 

4 pls. 

Hay, H. B., 1977, Field trip No. !-Cincinnatian stratiggraphy from Richmond to Aurora, Indiana, in Pope, J. 

K., and Martin, W. D. (ed.), Biostratigraphy and paleoenvironments of the Cincinnatian Series, southeastern 

Indiana: Guidebook, 7th Ann. Field Conference Great 

Lakes Section, Society of Economic Paleontologists and 

Mineralogists, p. I-1-1-33. 

Howe, H. J., 1979, Middle and Late Ordovician plectambonitacean, rhynchonellacean, syntrophiacean, trimerellacean, and atrypacean brachiopods: U.S. Geol. Survey 

Prof. Paper 1066-C, 18 p., 7 pls. · 

Hrabar, S. V., Cressman, E. R., and Potter, P. E., 1971 

Crossbedding of the Tanglewood Limestone Member of 

the Lexington Limestone (Ordovician) of the Blue Grass 

Region of Kentucky: Brigham Young Univ. Geology 

Studies, v. 18, 99-114, 11 figs. 

Kepferle, R. C., 1976, Geologic map of the Fisherville quadrangle, north-central Kentucky: U.S. Geol. Survey Geol. 

Quad. Map GQ-1321. 

King, P. B., and Beikman, H. M., compilers, 1974, Geologic 

map of the United States (exclusive of Alaska and 

Hawaii): Reston, Va. U.S. Geol. Survey, 3 sheets, scale 

1: 2,500,000. 

Kohut, J. J., and Sweet, W. C., 1968, The American Upper 

Ordovician Standard. X. Upper Maysville and Richmond 

conodonts from the Cincinnati Region of Ohio, Indiana, 

and Kentucky: Jour. Paleontology, v. 42, p. 1456-1477, 

pls. 185, 186. 

Lobo, C. F., and Osborne, R. H., 1973, The American Upper 

Ordovician Standard, XVIII: Investigation of micrite 

in typical Cincinnatian limestones by means of scanning 

electron microscopy: Jour. Sed. Petrology, v. 43, p. 478-

483, 3 figs. 

Luft, S. J., 1971, Geologic map of part of the Covington 

quadrangle, northern Kentucky: U.S. Geol. Survey Geol. 

Quad. Map GQ-955. 

MacQuown, W. C., Jr., 1967, Factors controlling porosity 

and permeability in the Curdsville Member of the Lexington Limestone: Kentucky Univ. Water Resources Inst. 

Research Rept. 7, 80 p., 19 figs. 

Neuman, R. B., 1967, Some silicified Middle Ordovician 

brachiopods from Kentucky: U.S. Geol. Survey Prof. 

Paper 583-A, 14 p., 2 pls. 

Osborne, R. H., 1967, The American Upper Ordovician Standard. VIII. R-mode factor analysis of Cincinnatian limestones: Jour. Sed. Petrology, v. 37, p. 649-657. 

---1968, American Upper Ordovician Standard. IX. Bedrock geology of eastern Hamilton County, Ohio: Am. 

Assoc. Petroleum Geologists Bull., v. 52, p. 2137-2152, 

10 figs. 

---1969, The American Upper Ordovician Standard. XI. 

Multivariate classification of typical Cincinnatian calcarenites: Jour. Sed. Petrology, v. 39, p. 769-776, 3 figs. 

---1970, The American Upper Ordovician Standard. XII. 

Time-trend analysis of Cincinnatian calcarenites, Hamilton County, Ohio: Jour. Geology, v. 78, p. 363-371, 

1 fig. 

---1971a, The American Upper Ordovician Standard. 

XIV. Markov analysis of typical Cincinnatian sedimentation, Hamilton County, Ohio: Jour. Sed. Petrology, v. 

41, p. 444-449. 

---1971b, The American Upper Ordovician Standard. 

XVI. Utility of clastic-ratio values to distinguish Kope 

and Fairview Formations, Hamilton County, Ohio: Ohio 

Jour. Sci., v. 71, p. 317-319, 1 fig. 

---1973, The American Upper Ordovician Standard. 

XVII: Areal variation of limestone frequencies in the 

Kope and Fairview Formations, Hamilton· County, Ohio: 

Jour. Sed. Petrology, v. 43, p. 137-146, 4 figs. 

---1974, Bedrock geology of the Cincinnati East quadrangle, Hamilton County, Ohio [map]: Ohio Div. Geol. 

Survey Rept. Inv. 94. 

Peck. J. H., 1966, Upper Ordovician formations in the Maysville area, Kentucky: U.S. Geol. Survey Bull. 1244-B, 

30 p., 8 figs. 

Peterson, W. L., 1970, Bardstown Member of the Drakes 

Formation in central Kentucky, in Cohee, G. V., Bates, 

R. G., and Wright, W. B., Changes in stratigraphic 

nomenclature by the U.S. Geological Survey, 1968: U.S. 

Geol. Survey Bull. 1294-A, p. 36-41, fig. 3. 

---1972, Geologic map of the Maud quadrangle, Nelson 

and Washington Counties, Kentucky: U.S. Geol Survey 

Geol. Quad Map GQ-1043 [1973]. 

Pulse, R. R., and Sweet, W. C., 1960, The American Upper 

Ordovic-ian Standard III. Conodonts from the Fairview 

and McMillan Formations of Ohio, Kentucky, and Indiana: Jour Paleontology, v. 34, p. 237-264, pls. 35-37. 

Ross, R. J., Jr., 1967, Calymenid and other Ordovician trilobites from Kentucky and Ohio: U.S. Geol. Survey 

Prof. Paper 583-B, 19 p., 5 pls. 

---1979, Additional trilobites from the Ordovician of 

Kentucky: U.S. Geol. Survey Prof. Paper 1066-D, 13 p., 

6 pls. 

Simmons, G. C., and Oliver, W. A., Jr., 1967, Otter Creek 

coral bed and its fauna, east-central Kentucky: U.S. 

Geol. Survey Bull. 1244-F, 13 p., 4 figs. 

Swadley, W C, 1975, Geologic map of the Lawrenceville 

quadrangle, Grant and Owen Counties, Kentucky: U.S. 

Geol. Survey Geol. Quad. Map GQ-1204. 

Swadley, W C, Luft, S. J., and Gibbons, A. B., 1975, The 

Point Pleasant Tongue of the Clays Ferry Formation, 

northern Kentucky: U.S. Geol. Survey Bull. 1405-A, p. 

30-31. 

1 Sweet, W. C., 1979, Conodonts and conodont biostratigraphy 

of post-Tyrone Ordovician rocks of the Cincinnati region: U.S. Geol. Survey Prof. Paper 1066-G, 25 p. 

Sweet, W. C., and Bergstrom, S. M., 1970, Stratigraphic 

significance of conodonts from the Lexington Limestone 

and Kope Formation in the Cincinnati region (abs.): 

Geol. Soc. America Abs. with Programs, v. 2, no. 3, p. 

242-243. 

---1971, The American Upper Ordovician Standard XIII: 

A revised time-stratigraphic classification of North 

American upper Middle and Upper Ordovician rocks: 

Geol. Soc. America Bull., v. 82, p. 613-628, 10 figs. 
A48 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

---1974, Provincialism exhibited by Ordovician conodont 

faunas: Soc. Econ. Paleontologists and Mineralogists 

Spec. Pub. 21, p. 189-202, 8 figs. 

Sweet, W. C., Ethington, R. L., and Barnes, C. R., 1971, 

North American Middle and Upper Ordovician conodont 

faunas: Geol. Soc. America Mem. 127, p. 163-193, 2 pls. 

Sweet, W. C., Harper, Howard, Jr .. and Zlatkin, Dennis, 

1974, The American Upper Ordovician Standard. XIX. 

A middle and Upper Ordovician reference standard for 

the eastern Cincinnati region: Ohio Jour. Sci., v. 74, p. 

47-54, 3 figs. 

Sweet, W. C., Turco, C. A., Warner, Earl, Jr., and Wilkie, 

L. C., 1959, The American Upper Ordovician Standard. 

I. Eden conodonts from the Cincinnati region of Ohio 

and Kentucky: Jour. Paleontology, v. 33, p. 1029-1068, 

pls. 130-133. 

Twenhofel, W. H., and others, 1954, Correlation of the Ordovician Formations of North America: Geol. Soc. 

America Bull., v. 66, p. 247-298, 2 figs. 

Van Horn, Richard, and Griffitts, W. R., 1969, Geologic map 

of the Blacks Ferry quadrangle, Monroe and Cumberland Counties, Kentucky: U.S. Geol. Survey Geol. Quad. 

Map GQ-803. 

Weir, G. W., 1971, Geologic map of the Lancaster quadrangle, Lincoln and Garrard Counties, Kentucky: U.S. 

Geol. Survey Geol. Quad. Map GQ-888. 

-·--1975, Geologic map of the Owingsville quadrangle, 

Bath and Montgomery Counties, Kentucky: U.S. Geol. 

Survey Geol. Quad. Map GQ-1242. 

Weir, G. W., and Greene, R. C., 1965, Clays Ferry Formation (Ordovician)-A new map unit in south-central 

Kentucky: U.S. Geol. Survey Bull. 1224-B, 18 p., 7 figs. 

Weir, G. W., Green, R. C., and Simmons, G. C., 1965, Calloway Creek Limestone and Ashlock and Drakes Formations (Upper Ordovician) in south-central Kentucky: 

U.S. Geol. Survey Bull. 1224-D, 36 p., 12 figs. 

Weir, G. W., and Peck, J. H., 1968, Lithofacies of Upper 

Ordovician rocks exposed between Maysville and S.tanford, Kentucky: U.S. Geol. Survey Prof. Paper 600-D, 

p. 162-168, 5 figs. 

Weiss, M. P., 1961, The American Upper Ordovician Standard V. A critical appraisal of the classification of the 

typical Cincinnatian beds: Geol. Soc. America Bull., v. 

72, p. 645-648. 

Weiss, M. P., and Norman, C. E., 1960a, The American 

Upper Ordovician Standard II. Development of stratigraphic classification of Ordovician rocks in the Cincinnati region: Ohio Div. Geol. Survey Inf. Circ. 26, 14 p., 

1 pl. 

---1960b, The American Upper Ordovician Standard IV. 

Classification of the limestones of the type Cincinnatian: 

Jour. Sed. Petrology, v. 30, p. 282-296, 13 figs. 

Weiss, M. P., Edwards, W. R., Norman, C. E., and Sharp, 

E. R., 1965, The American Upper Ordovician Standard. 

VII. Stratigraphy and petrology of the Cynthiana and 

Eden Formations of the Ohio Valley: Geol. Soc. America 

Spec. Paper 81, 76 p., 8 pls. 

Weiss, M. P., and Sweet, W. C., 1964, Kope Formation (Upper Ordovician) : Ohio and Kentucky: Science, v. 145, 

p. 1296-1302, 1 fig. 

Whaley, P. W., 1973, Relation of organic activity to early 

diagenetic changes in the Tyrone Limestone of Kentucky: Kentucky Acad. Sci. Trans, v. 34, p. 1-4. · 

Wolcott, D. E., Cressman, E. R., and Connor, J., 1972, 

Trend-surface analysis of the thickness of the High 

Bridge Group (Middle Ordovician) of central Kentucky 

and its bearing on the nature of the post-Knox unconformity: U.S. Geol. Survey Prof. Paper 800-B, p. 25-33, 

7 figs. 

I 
The Brachiopod Genus Platystrophia 

By LEONARD P. ALBERSTADT 

CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY 

OF KENTUCKY AND NEARBY STATES 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-B 

Prepared in cooperation with the 

Commonwealth of Kentucky, 

University of Kentucky, 

Kentucky Geological Survey 

Discussion of the stratigraphic and geographic 

distribution of Platystrophia and the 

description of eight species 

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON 1979 

PLATE 1. 

2. 

3. 

4. 

5·. 

6. 

7. 

FIGURE 1. 

2. 

8. 

4. 

CONTENTS 

Page 

Albstract ----------------------------------------------------------------- B1 

Introduction ------------------------------------------------------------- 1 

Alcknowledgrnents -------------------------------------------------------- 2 

Stratigraphic distribution ------------------------------------------------- 2 

Geographic distributions and relations to other faunas ---------------------- 6 

Ordovician faunal migrations ______________________________ --- _ _ __ __ _ _ _ 6 

Platystrophia migrations ---------------------------------------------- 7 

North Almerican Platystrophias outside the Ohio Valley ------------------ 7 

Provincialism __________________________________________ --- ____ -- _ _ _ __ 8 

Systematic paleontology ______________________________ --- _ _ __ _ _ _ __ _ __ _ ____ 9 

Platystrophia colbiensis Foerste ______________ · _____ -- ______ --- ____ ---- _ 9 

Platystrophia elegantula McEwan -------------------------------·------ 10 

Platystrophia acutilirata (Conrad) ------------------------------------ 11 

Platystrophia annieana Foerste ---------------------------------------- 12 laticosta (Meek) ________________________________ ------- _ 14 

Platystrophia cypha (James) ----------------------------------------- 15 

Platystrophia ponderosa Foerste --------------------------------------- 16 

Platystrophia cf. P. foerstei Mc·Ewan ----------------------------------- 18 

Platystrophia sp --------------------------------------------~--------- 18 

References cited ---------------------------------------------------------- 18 

ILLUSTRATIONS 

Specimens of Platystrophia ponderosa. 

Specimens of Platystrophia ponderosa. 

Specimens of Platystrophia annieana. 

Specimens of Platystrophia annieana and Platystrophia ponderosa. 

Specimens of Platystrophia colbiensis, Platystrophia annieana, Platystrophia cypha, Platystrophia laticosta, 

Platystrophia cf. P. laticosta, Platystrophia elegantula, Platystrophia cf. P. annieana, and Platystrophia 

cf. P. colbiensis. 

Specimens of Platystrophia laticosta, Platystrophia cypha, Platystrophia cf. P. foerstei, Platystrophia sp., Platystrophia ponde1·osa, and Platystrophia acutilirata. 

Specimens of Platystrophia acutilirata, Platystrophia annieana, Platystrophia unicostata, Platystrophia latic.osta, Platystrophia cypha, Platystrophia clarksvillensis, Platystrophia cf. P. annieana, Platystrophia elegantula, and Platystrophia colbiensis. 

Lithostratigraphic framework of Ordovician strata and vertical distribution of species of Platystrophia 

Phylogeny of the triplicate subgroup of Platystrophia -----------------------------------------------

Scatter diagram showing relationship between width measurements of Platystrophia elegantula and Platystrophia colbiensis _________________________________________________________ ------------ ____ _ 

Scatter diagram showing the relationship between width measurements of Platystrophia elegantula and 

Platystrophia colbiensis -----------------------------------------------------------------------

III 

Page 

B3 

5 

9 

10 
IV 

TABLE 1. 

2. 

3. 

4. 

5. 

6. 

7. 

8. 

9. 

CONTENTS 

TABLES 

Page 

Measurements and number of plications in a suite of specimens of Platystrophia colbiensis Foerste, 

Clays Ferry Formation, Shawhan quadrangle, Kentucky ----------------------------------------- B10 

Measurements and numbers of plications in a suite of specimens of Platystrophia elegantula McEwan, 

Tanglewood Limestone Member of the Lexington Limestone, Frankfort East quadrangle, Kentucky 11 

Measurements and numbers of plications in a suite of specimens of Platystrophia elegantula McEwan, 

Tanglewood Limestone Member of the Lexington Limestone, Frankfort West quadrangle, Kentucky 11 

Measurements and numbers of plications in a suite of specimens of Platystrophia annieana Foerste, 

Dillsboro Formation, Milan quadrangle, Indiana ---------------------------------,--------------- 13 

Measurements and numbers of plications of Platystrophia annieana, from speciments studied by MeEwan 

(1919), and deposited in the collections of the U.S. National Museum ---------------------------- 13 

Measurements and numbers of plications of Platystrophia laticosta, from specimens studied by McEwan 

(1919) and deposited in the collections of the U.S. National Museum ---------------------------- 15 

Measurements and numbers of plications of Platystrophia cypha from specimens studied by McEwan 

(1919) and deposited in the U.S. National Museum ------------------------------------------- 15 

Measurements and numbers of plications of Platystrophia unicostata, from specimens studied by McEwan (1919) and deposited in the U.S. National Museum --------------------------------------- 15 

Measurements of several dimensions (in millilneters) and numbers of plications in a suite of specimens 

of Platystrophia ponderosa Foerste from a single collection (USGS colin. 4556-CO; USNM 189578) 

from the Back Bed, Tate Member of the Ashlock Formation in the Richmond North quadrangle, 

Kentucky ------------------------------------------------------------------------------------ 17 

SYSTEM OF MEASUREMENT UNITS 

The investigations underlying this series of reports were made over a period of 

years, and distances and stratigraphic measurements appear fairly uniformly in 

English units. Measurements of fossil specimens, on the other hand, follow the longstanding convention of appearing in metric units. Because of the dates of the investigations and the amount of resulting data, the English measurements have been retained. Conversions to metric units may be made by using the following conversion 

table. 

To convert To metric· unit: Multiply 

English unit: by: 

Mile (mi) · Kilometer (km) 1.61 

Foot (ft) Meter (m) .305 
CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

THE BRACHIOPOD GENUS PLATYSTROPHIA 

By LEONARD P. ALBERSTADT1 

A·BSTRACT 

The brachiopod genus Platystrophia is one of the most 

conspicuous taxa in the Ordovician strata of Kentucky; it 

can be divided into four easily recognizable nontaxonomic 

groups, referred to as (1) the ponderosa group, (2) the 

colbiensis-elegantula group, (3) the annieana group, and (4) 

the laticosta-cypha group. The species within the colbiensiselegantula group are confined to the Lexington Limestone and 

Clays Ferry Formation. Species in the ponderosa, annieana, 

and laticosta-cypha groups occur in the overlying Calloway 

Creek, Fairview, Ashlock, Grant Lake, Bull Fork, and Drakes 

Formations. 

All the species of Platyst'rophia from Kentucky are members of the "triplicate" group of Cumings (1903). The stratigraphic positions of these .species are generally consistent 

with McEwan's (1919) phylogenetic interpretation of the 

"triplicate" group; the only exception is her interpretation 

that P. laticosta was ancestral to P. cypha. The reported 

stratigraphic positions of these two species in Kentucky do 

not lend support to this sequential history. 

The stratigraphic distribution and morphology of the 

various species in Kentucky suggest that the Richmondian 

species are more closely related to the underlying species 

(Edenian and Maysvillian forms) than they are to those in 

western and arctic faunas. The various species of Platystrophia from Anticosti Island, Quebec; from northern 

Canada; and from Iowa, Idaho, Texas, Wyoming, and Oklahoma, are distinctly different from those in the Cincinnati, 

Ohio, region. This difference makes Upper Ordovician 

brachiopod biostratigraphic correlations difficult, and furthermore makes the rocks of the Cincinnati, Ohio, region 

less effective as the standard for the Upper Ordovician of 

North America. 

INTRODUCTION 

The brachiopod genus PlatystTophia is one of the 

most conspicuous taxa in the Middle and Upper 

Ordovician formations of Kentucky. Its abundance 

and ease of recognition have been used by various 

workers over .the years to help define some of the 

formations. The difficulties that arise· from such a 

procedure have been discussed by others (Weiss, 

1961) and will not be elaborated here. 

James (1881), Cumings (1903), Shaler (1876), 

Foreste (1909a, 1909b, 1910), McEwan (1919), and 

Caster, Dalve, and Pope (1961) are some of the 

workers who have studied Platystrophia from this 

region, :and their work has greatly influenced our 

understanding of the genus, although the work of 

McEwan (1919) is undoubtedly the "standard" 

reference for the genus. Unfortunately her species 

differentiations are based primarily on external 

characters and details of the interiors are lacking. 

Platyst1·ophia is a highly variable genus for which 

many sp·ecies and subspecies have been proposed, as 

McEwan's study well illustrates. However, serious 

question exist.s as t.o .the validity of all of the proposed taxa, and a thorough reevaluation is in order. 

Although it is difficult t:o confidently assign all 

specimens from Kentucky to a previously defined 

species or subspecies, suites of ·specimens with more 

than 25 co·mplete individuals can he properly assigned in most cases. I have avoided erecting any 

new taxa on the basis of this work, because the 

genus needs careful reevaluation; and collections 

other than those from Kentucky must be considered. 

Such a reevaluation is not the purpose here; rather, 

it is t.o determine the stratigraphic occurrences and 

the morphological variability of the several species 

as they are represented in these collections from 

Kentucky, in hopes of increasing our understanding of the biostratigraphy of the Ordovician of 

Kentucky. 

The species of Platystrophia from Kentucky described in this paper form four easily recognizable 

nontaxonom.ic groups. These informal groups are 

designated ( 1) the ponderosa group, (~.) the colbiensis-elegantula group, (3) the annieana group, 

and ( 4) the laticosta-cypha group. Most of the specimens are referred to established species within 

1 Vanderbilt University, Nashville, Tenn. 

B1 
B2 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

these groups. The species described herein are assigned to groups as follows : ( 1) ponderosa group : 

Platystrophia ponderosa; (2) annieana group: 

Platystrophia annieana, P. acutilirata, P. cf. P. 

foerstei; ( 3) colbiensis-elegantula group: P. colbiensis, P. elegantula; ( 4) laticosta-cypha group: P. 

laticosta, P. cypha. 

Characteristics most commonly used in differentiating species of Platystrophia are ( 1) hinge-line 

width, (2) shell thickness (dorsal to ventral dimension of articula.ted specimens) , ( 3) ratio of thicknes's to width, ( 4) number of plications. in sinus, 

on fold, and on flanks, ( 5) size and shape of plications and furrows, ( 6) size of specimen at maturity, 

(7) height of fold and depth of sinus, (8) position 

and method of addition of plicati~ns, and (9) appearance of cardinal extremities. As evidenced from 

the literature and from studies of the specimens in 

these collections all of the above-mentioned features, 

show some degree of intraspecific variation. Also, 

that a great deal of interspecific overlap exists appears undoubted; this is one reason a reevaluation 

of the genus is needed. 

A good example of such interspecific overlap· is 

the similarity of Platystrophia laticosta, P. cypha, 

and specimens commonly referred by other workers 

to P. unicostata and P. crassa. This overlap is particularly true of small and medium-sized specimens .. 

McEwan (1919, p. 432) pointed out that the difference between P. laticosta and P. cypha is one of 

degree. Mature and old specimens of P. crassa have 

a gibbosity that is slightly more pronounced than 

that of P. laticosta or P. cypha, but overall great 

similarity exists among all three species. 

P. colbiensis, P. elegantula, and smaller individuals of other species, particularly P. annieana and 

P. ponderosa, also exhibit similarities. Species differentiation of ~small and medi urn sized specim.ens is 

difficult. As an example compare the following: 

figures 8 and 9 (P. annieana) on plate 3, figure 3 

(P. colbiensis) on plate 5, and figures 55 and 60, 

(P. elegantula) on plate 5. Species distinctions are 

much easier when large numbers of specimens are 

available so that complete growth series can be assembled and variations better evaluated. However, 

large suites of specimens commonly contain several 

distinctly atypical individuals. Such specimens commonly have a different appearance because of variations in overall shell shape, and :the number and 

shape of plications, particularly in the number of 

plications on the fold. Figures 29, 30, 32, and 33 on 

plate 4 illustrate this point. All the above-mentioned 

sp·ecimens on plate 4 are from the same collection, 

and all are referred toP. ponderosa. The· specimen 

shown in figure 29 has fewer and more angular pHcations than that of figure 32, which has many more 

plications distributed slightly unevenly across the 

shell. The specimen shown in figure 33, plate· 4, has 

"typical" plkations on its flanks but a fold with 

seven plications compared to four plications in most 

specimens of P. ponderosa. Figures 37 and 38 on 

plate 5 are the best examples showing the differences that can occur in the number of fold plications in a single collection; figure 37 has two large 

angular pHcations and figure 38 has. six uniformly 

developed plications. The best illustration of variations in flank plications is shown by figures 43 and 

44 on plate 5. These are specimens from. a small 

collection and are tentatively referred to P. cypha; 

plate 5, figure 43, has 15 to 16 flank plications and 

plate 5, figure 44, has 10 flank plications. Such variation has long been recognized in Platystrophia of the 

Ohio Valley, and until appropriate statistical studies 

are done to help define the species, their biostratigraphic value will be limited. 

ACKNOWLEDGMENTS 

I want to express my sincere appreciation to 

Alwyn Williams, P.M. Sheehan, R. Peter Richards, 

John Poj·eta, and J. K. Pope for reading the manuscript and making ~suggestions for its improvement. 

Many of their suggestions were followed, but any 

shortcomings or misinterpretations. in this report 

are mine alone. 

STRATIGRAPHIC DISTRIBUTION 

The vertical distributions of species of Platystrophia as determined from the Kentucky collections are shown in figure 1. The most conspicuous 

aspect of these distributions is the restriction of the 

elegantula-colbiensis group to the Lexington Limestone and Clays Ferry Formation, and the oc·currence in the overlying Calloway Creek, Fairview, 

Ashlock, Grant Lake, Bull Fork, and Drakes For;.. 

mations of members of the ponderosa group, 

annieana group, and laticosta-cypha group·. In addition, two other aspects of the stratigraphic distribution may be meaningful. First, the lowermost appearance of the laticosta-cypha group is ne,ar the 

bas·e of the Ashlock Formation-Grant Lake Limestone. Second, P. annieana appears to be restricted 

to the uppermost part o.f the Ordovician; the Drakes 

and Bull Fork Formations. 

The nonoverlapping occurrence of the elegantulacolbiensis group and the ponderosa, annieana, and 
P. ct. foerstei 

P. ponderosa 

P. aft. annieana 

P. annieana 

P. acutilirata 

P. ct. laticosta 

P. laticosta 

P. ct. cypha 

P. cypha 

P. colbiensis 

P. elegantula 

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FIGURE 1.-General lithostratigraphic framework of the Ordovician strata in Kentucky and the vertical distribution of the brachiopod species. The 

position of the Middle-Upper Ordovician boundary is taken from Sweet and Bergstrom (1971). 
B4 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

laticosta-cypha groups may be of importance in interpreting the phylogenetic history of species of 

Platystrophia. It is interesting to note that the termination of the elegantula-colbiensis group and the 

beginning 'of the ponderosa group is separated by 

the Garrard Silts:tone. Such stratigraphic evidence 

should be considered in any interpretation that Late 

Ordovic.ian species in Kentucky were derived from 

either of these two Middle Ordovician species. 

All of the specimens in the Kentucky collections 

fall within the "triplicate" group of Cumings 

( 1903). Figure 2 is a modified version of the phylogeny of the triplicate .subgroup as interpreted by 

McEwan (1919), showing the low-fold subgroup 

well established in the Shermanian, and characterized by such species as P. elegantula, colbiensis, 

and amoena. The low-fold subgroup gave rise to the 

ponderosa subgroup shortly after the beginning of 

the Maysvillian; during late Maysvillian and early 

Richmondian time the low-fold subgroup gave rise 

to the high-fold subgroup of laticosta-unicostatacypha. The concepts underlying McEwan's phylogeny are based on interpretations of orthogenesis, 

racial development, and the "biogenic law," so·me 

of which are not as absolute as once thought. 

According to McEwan (1919) the distinction of 

the low-fold, high-fold, and ponderosa subgroups is 

based on hinge-line width, thickness of articulated 

specimen, nature of the fold, and overall size. The 

low- and high-fold subgroups have long hinge lines 

relative to their thickness and have a similar 

ontogenetic development. However, in late neanic 

development, members of the high-fold subgroup depart markedly from those of the low-fold subgroup 

in developing a high, compressed fold and weak 

lateral fold plications. Species that develop to a large 

size (30-35 mm average) with a hinge line shorter 

than or approximately equal to the shell width are 

referred to the ponderosa subgroup. 

The modified phylogenetic diagram of McEwan 

(fig. 2 herein) contains most of the species found 

in the Kentucky collections and described in this. 

paper. They are incorporated into the diagram at 

their approximate stratigraphic position as reported 

by McEwan (1919). Note the similarity between 

this modified diagram of McEwan's and the stratigraphic o~ccurrences of these species as determined 

from a study of the Kentucky material (fig. 1). 

With the exception of the specimens referred to in 

this paper as P. cf. P. foerstei and P. aff. P. annieana the stratigraphic distribution of the Kentucky· 

species is in general agreement with the superpositional occurrence required by McEwan's phylogenetic scheme. 

The validity and utility of McEwan's phylogenetic scheme has been questioned and undoubt·edly needs revision (Williams, 1963). In discussing 

the Ordovician brachiopods of the Bala District of 

Wales, Williams pointed out that, according to 

McEwan's interpretation, a homogeneous sample of 

Platystrophia cf. P. sublimis Opik would be assigned to three species based on the numher and 

mode of origin of the costae (Williams' term) within the sulcus. The same association is found in the 

rocks of Kohtla, Estonia, where Williams (1963) 

cited Opik and described two species based on the 

presence of either two or three costae (Williams' 

t~erm) in the ventral sulcus (Williams, ·.1963). 

It is not unreasonable to expect that McEwan's 

phylogenetic proposals need revision, based as it is 

on faunas now known to have a history of co·mplex 

mixings and migrations. Whether the plication patterns can help unravel the details of the evolution of 

Pla.tystrophia remains to be seen. 

I have not attempted to make any specific phylogenetic interpretations based on my work with the 

Kentucky specimens. With the exception of the 

laticosta-unicostata-cypha line, McEwan gave little 

indication of the ancestor-descendant relationships 

among the various· triplicate speci€1S of the genus. 

In general, she pointed out that many of the species 

from the Richmondian are remarkably similar in 

appearance to those in the Trentonian ( Sher~ 

manian ?) , and that great ~care is needed to differentiate them. In the Kentucky collections, with 

the exception of small specimens of P. ponderosa 

and annieana, there is little difficulty in differentiating Richmondian species from the two common 

Shermanian species, P. colbiensis and P. elegantula. 

I agree with McEwan's observation that specimens 

from the Richmondian appear to have fewer flank 

plications than those from the Shermanian. 

McEwan ( 1919) stated that little in the morphology of P. ponderosa indicates its ancestry except the 

lowfold growth pattern of the early growth stages. 

This suggests the derivation of P. ponderosa from 

some member of the low-fold subgroup. She further 

speculated that P. ponderosa may be polyphyletic. 

It is my belief, however, that the presence of a 

"crurali urn-like" structure in almost all brachial 

valves of this species negates the idea of a polyphyletic origin, unless one is willing to entertain 

the idea of a multiple development of this structure. 

Such a conclusion is not warranted at this tim·e. 
THE BRACHIOPOD GENUS PLATYSTROPHIA 

en Ill ~- Q) Q) ·- ..c. ·u 

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, \.... -----~ ..... ----.... ~\... ... _____ v-----~~\...-----.... v------

High-fold Low-fold Ponderosa 

subgroup subgroup subgroup 

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FIGURE 2.-Phylogeny of the triplicate subgroup (modified from McEwan, 1919). 

B5 
B6 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

The stratigraphic occurrence of Platystrophia 

species as determined from the Kentucky collections 

is generally consistent with the phylogenetic history of the triplicat~e group as presented by McEwan 

(1919). However, her interpretation that within 

the high-fold subgroup, P. laticosta was ancestral 

to P. unicostata (which in turn gave rise to P. 

cypha) is not entirely compatible with the stratigraphic occurrence of the species in Kentucky. P. 

laticosta and P. cypha seem to appear at about the 

same stratigraphic horizon (fig. 1). 

The overall morphology and stratigraphic distribution of Platystrophia species in the Middle and 

Upper Ordovician rocks of Kentucky indicates that 

the Richmondian species are more' closely related 

to underlying Edenian-Maysvillian forms. of the 

Ohio Valley region rather than to species of the 

western and arctic faunas of North America. Species in the Drake's and Bull Fork Formations commonly range into the underlying units, exceptions 

being P. annieana and P. acutilirata. The inter. 

preted phylogeny of the Platystrophia laticostacypha line helps accentuate the fact that Richmondian Platystrophias have more Edenian-Maysvillian affinities than some of the other brachiopods. 

The range of P. ponderosa also suggests such a conclusion. 

The boundary between the Middle and Upper 

Ordovician is interpreted to be somewhere in the 

upper part of the Lexington Limest.one (fig. 1). 

The lower part of the Clays Ferry is believed to be 

equivalent to the uppe·r part of the Lexington Limestone (Black, Cressman, and MacQuown, 1965). 

Platystrophia elegantula and Platystrophia colbiensis occur in many parts of the Lexington and the 

Clays Ferry. Howeve,r, they do not appear to be 

sufficiently restricted stratigraphically to be considered valid taxa for interpreting the Middle 

Ordovician ( Shermanian) . 

All of the species of Platystrophia in the overlying lithostratigraphic· units can be used as an assemblage to characterize the Upper Ordovician 

(Edenian, Maysvillian, and Richmondian Stages?). 

With the exception of P. annieana, none of them appears to have the necessary stratigraphic restriction or the morphological distinctness to use them 

as stadial markers. However, the association of P. 

annieana, P. ponderosa, and P. cypha can be us·ed 

to charac.terize the upper part of the Upper Ordovician ( Richmondian) , although P. ponderosa is not 

reported from the Preachersville Membe·r of the 

Drakes Formation. Other evidence suggests. that P. 

ponderosa does not range above the lower part of 

the Richmondian in western Ohio and Indiana (John 

Pope, written commun., 1975). 

GEOGRAPHIC DISTRIBUTIONS AND 

RELATIONS TO OTHER FAUNAS 

The many species and morphological variants of 

Platystrophia are a conspicuous part of the brachiopod faunas o.f Ordovician rocks of Kentucky and 

nearby States, and are probably nowhere better developed than in this region. However, there still 

exist significant uncertainties about the evolutionary history of Late Ordovician brachiopod faunas, 

particularly the Richmondian faunas of the Ohio 

Valley. Many of the questions regarding this history Were initially raised by Twenhofel (1928) in 

his study of Upper Ordovician and Silurian rocks of 

Anticosti Island. Macomber (1970) presented an 

excellent summary of this problem as well as 

additional data suggesting the likelihood that the 

Richmondian brachiopod faunas in the type area of 

the Ohio Valley are mixtures of Edenian-Maysvillian 

descendants and migrants from western and "arctic" 

faunas. He rightly pointed out that such a situation reduces the effectiveness of the Ohio Valley as 

a standard for the Upper Ordovician. 

ORDOVICIAN FAUNAL MIGRATIONS 

Much work has been done recently to indicate 

that from Middle Ordovician through Late Ordovician time the North American continent was subjected to various faunal migrations. For example, 

Macomber (1972) pointed out the almost simultaneous occurrence of the same species of H eterorthis 

in Wales and eastern North America, owing to 

"overflow" from a flood of H eterorthis in the Upper 

Longvillian of Britain. Cooper (1956) referred to 

a migration in describing the Porterfieldian Stage 

in the southern Appalachians. The Porterfieldian is 

characterized by "a prolific and exotic fauna that 

floods into the Appalachians and blots out and 

absorbs the Lincolnshire fauna" (Cooper, 1956, p. 

8). 

Williams. (1973) stated that faunal interchange 

between European and North American re,alms began during middle Caradocian time and that by 

Ashgillian time (Richmondian) a cosmopolitan 

fauna had e·merged. Based on prersent correlations, 

this middle Caradocian interchange is appreciably 

later than the Porterfieldian "flooding" described by 

Cooper (1956). The middle Ashgillian faunal alinement resulted in the North American province being primarily a western and midcontinent province, 
THE BRACHIOPOD GENUS PLATYSTROPHIA B7 

but in eastern North America being European in 

its overall taxonomic composition. 

Undoubtedly these migrations and interchanges 

have greatly influenced biostratigraphic interpretations of Middle and Upper Ordovician rocks of 

North Am·erica. Detailed studies of North American 

conodonts (Berg.strom and Sweet, 1966, Sweet and 

Bergstrom, 1971; Schopf, 1966; Sweet and others, 

1970) and the gradual recognition that the type 

Richmondian is a mixed assemblage (Macomber, 

1970) helped imm·ensely in clarifying certain 

troublesome correlations of Edenian, Maysvillian, 

and Richmondian rocks of the Western United 

States with the type area of the Ohio Valley. 

PLATYSTROPHI A MIGRATIONS 

The Platystrophia of the Ohio Valley form part 

of this "mixed" assemblage brought about by the 

migration of different taxa into the· region throughout Maysvillian and Richmondian time, probably 

from western and northern sources from what is 

commonly refe·rred to as the "arctic" fauna. 

The earliest reported occurrence of Platystrophia 

is from the Leningrad district of Russia and is 

probably Arenigian in age (Neuman, 1964). 

The consensus is that the appearance of Platystrophia in Britain is due to its westerly spread from 

the Baltic provinces (MacGregor, 1961; Whittington and Willia.m.s, 1955). Whittington and Williams 

(1955) described many of the brachiopods, including Platystrophia, in the .Gerfel Limestone (lower 

Caradocian, Coston ian) of North Wales as "exotics," 

probably Russian. MacGregor (1961) reported the 

same species of Platystrophia from the upper 

Ll·andeilian of Wales. Bates (1968) described the 

same species from. the N ernagraptus gTacilis zone 

of Anglesey (middle-upper Llandeilian). However, 

several other species of Platystrophia (P. scotica and 

P. caelata) of Caradocian Age have been described 

from. Britain (Williams, 1962; 1974). 

Neuman (1963, 1964, and 1968) described Platystrophia from sediments associated with volcanic 

rocks around ancient volcanic islands in Maine and 

N e·wfoundland. Those from Maine (Shin Brook Formation (Arenigian to Llanvirnian ?) ) are similar to 

P. precedens McEwan (1919) and P. prece·dens 

maior Williams (in Whittington and Williams, 

1955). Overall the Shin Brook fauna is most like 

the Arenigian of the Baltic region (Neuman, 1964). 

Neuman (1964, 1968) believed that the volcanic 

islands s~erved as st·eppingstones for faunal migrations in a general east-to-west direction, thus allowing the European species to migrate westward to 

North America. 

The two species of Platystrophia from Anticosti 

Island (Ellis Bay Formation) described by Twenhofel (1928) resemble externally some of the species from the Ohio Valley. However, on Anticosti, 

the P. ponderosa, P. laticosta, P. crassa, P. cypha, 

and P. annieana forms so characteristic of the type 

Cincinnatian are completely absent. Twenhofel 

(1928) assigned a post-Richmondian to pre-Silurian 

age to the Ellis Bay primarily because it lacks certain faunal similarities with the type areas of the 

midcontinent. More recent studies by Bolton (1971) 

suggest that the Ellis Bay is probably Richmon.dian, 

although some conflicting opinion remains. 

The age of the Ellis Bay Formation is not important as such; it is important to substantiate the fact 

that the few Platyst1·ophia species from Anticosti 

Island are more like the western forms. and much 

younger than those reporbed by Neuman from adjacent areas of Maine and Newfoundland. 

Twenhofel's (1928) studies of the Anticosti 

Island faunas led him to believe that a westwardtrending current during the Ordovician •enabled a 

westward spre•ad of species from a North Atlantic 

source, but prevented a concentrated eastward 

spread of North American faunas. This he believed 

explained the absence in the Anticosti succession of 

certain prominent Richmondian midcontinent taxa 

such as the numerous species of Platystrophia. 

This explanation of current directions was made 

with the belief that the North American and European continents were posi;tioned in the Ordovician 

as they are now. More recent geophysical evidenc•e 

and new data on Ordovician brachiopod distributions 

indicate. that the European and North Am·erican 

continents were much closer together (Williams, 

1969) , but s·eparated by a narro·w seaway (ProtoAtlantic?). According to Williams (1969), the 

North American side was dominated by an easterly 

flowing current and the European-African side by 

a westerly current. This Williams believed to be the 

pattern that hes:t explained the distributions and 

first occurrences. of certain Ordovician brachiopod 

genera. However, superimposed on this model are 

the various sedimentary facies, which certainly must 

be considered along with circulation patterns in 

any explanation of faunal provinces and the distribution of taxa. 

NORTH AMERICAN PLATYSTROPHIAS OUTSIDE 

THE OHIO VALLEY 

In addition to the prolific Platystrophia fauna of 

the Ohio Valley, various other species of this genus 
B8 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

have been described from the midcontinent and 

western areas of North America. The foB owing discussion is by no means an exhaustive presentation, 

but only a brief summary of those species pertinent 

to substantiate the uniqueness cof the Ohio Valley 

fauna and its possible origin. The speculations. regarding this origin should be viewed as only the 

present state of thinking of some of the worke·rs 

who have addressed themselves to this problem. 

Undoubtedly other viewpoints are possible, and 

much additional evidence is needed to clarify the 

histo·ry of these faunas. 

Wang (1949) described a single species, P. 

equiconvexa, from the Maquoketa Shale of Iowa. 

Ross ( 1959) considered the only species in the 

Saturday Mountain Formation to resemble P. 

equiconvexa Wang more than any other known 

species of the genus. Howe (1966) described a new 

species, P. prayi, from the Aleman Limestone 

(Montaya Group) of the Trans-Pecos region of 

Texas. T~e specimens reported by Macomber (1970) 

from the Bighorn Dolomite of Wyo·ming are referred to P. equiconvexa Wang and P. prayi Howe, 

although· Macomber pointed out that the latter is 

very similar toP. Tegularis globata Twenhofel from 

the Ellis Bay Formation on Anticosti Island. He suggested that the Ellis Bay species evolved fro·m the 

western form. The fauna on Anticosti Island contains P. camerata Twenhofel and P. regularis 

Shaler. Alberstadt (1973) described three new species from the Viola Limestone of Oklahoma, all of 

which are clearly distinct from previously described 

forms. Ludvigsen (1975) reported an unnamed species of Platystrophia from the Whittaker Formation (Shermanian-Maysvillian ?) from western and 

northern Canada. 

All these more recent brachiopod studies show 

that the Platystrophia species of the northern and 

western areas of North America are distinctly different from the highly variable forms found in the 

Ohio Valley. It is not presently possible to tell 

which, if any, were ancestral to the Richmondian 

forms of the Ohio Valley. With the exception of the 

species in southern Oklahoma (Alberstadt, 1973), 

strong ho·mogeneity marks the occurrences of 

Platystrophia from Iowa, Anticosti Island, Wyoming, Idaho, and Trans-Pecos Texas. 

PROVINCIALISM 

Evidence that Late Ordovician brachiopod faunas 

were provincial in their distribution is unmistakable; such provincialism is now recognized as partly responsible for past difficulties in correlating 

Upper Ordovician rocks throughout North America. 

Howe (1973) maintained that part of the reason 

for this provincial aspect was variation between 

sedimentary basins. One can onlY'speculate as to the 

reasons for the development of such isolated or 

semi-isolated sedimentary basins during part of the 

Late Ordovician followed by a sudden influx of outside sp·ecies near the end of the Late Ordovician. 

Two phenomena of the Ordovician bear directly on 

this question of provinciality. First, it has be·en 

proposed that the Proto-Atlantic gradually closed 

during the Ordovician, bringing European and 

North American faunal province·s closer together 

and helping to break down faunal barriers and to 

permit mixing. Various paleontological studies seem 

to support this general conclusion by showing that 

faunal distinctness was substantially reduced during the Ordovician (Williams, 1973), culminating 

in the more cosmopolitan faunas of the Silurian. 

Second, the discovery of Late Ordovician glaciation has led some workers to suggest that sea level 

was lowered sufficiently to subject the shallow-water 

epicontinental faunas to unique stress conditions, 

resulting in the extinction of many forms. (Sheehan, 

1973). Although Sheehan's work is aim·ed at understanding the faunal changeover fro·m the Ordovician 

to the Silurian, it seems reasonable to believe that 

such glaciations and the resultant strong climatic 

zonation helped maintain endemism. 

It is also possible that marked differences between 

the Ohio Valley species and thos·e from the "surrounding" regions of North America represent different environmental realms in a manner similar to 

that proposed by Ross and Ingham (1970) to explain the occurrenc·es of Whiteroekian (Middle 

Ordovician) trilobites in the Northern Hemisphere. 

According to these workers, the composition of the 

fauna is as much related to paleoenvironment as to 

time, and they proposed that faunal differences reflect the overall different conditions of the interior 

continental platforms and the bordering continental 

margins ( miogeosyncline to eugeosyncline) . Ross 

(1975) presented a summary showing that this general ~setting existed for western and central North 

America during much of the Ordovician. The shallow 

carbonate banks of the midcontinent could have restricted circulation, which may partly account for 

faunal differences across the platform-shelf transect. 

Us,ing this model, then, the different assemblages of 

Platystrophia from Oklahoma, Texas, Idaho, Wyoming, and Canada may represent a marginal shelflike paleotectonic setting much different from the 
THE BRACHIOPOD GENUS PLATYSTROPHIA B9 

midcontinent carbonate platform setting of the Ohio 

Valley. 

SYSTEMATIC PALEONTOLOGY 

I have followed the classification of the Treatise 

on Invertebrate Paleontology (Part H; Williams and 

others, 1965) ; therefore, suprageneric details are 

not repeated here. 

Genus PLA TYSTROPHIA King, 1850 

Diagnosis.-Subquadrate to spiriferoid in outline; 

hinge line straight, equal to or greater than midwidth. Strongly biconvex; pro·minent plications, fold 

plications co·mmonly accentuated and larger than 

flank plications; plications smooth or pustulose. 

Muscle field in pedicle valve well impressed; elongate, extends almost to middl'e of valve. Adductor 

scars in brachial valve moderately impressed, ellipsoidal to narrowly elongate in shape, some curved 

slightly; posterior scars better impressed than 

anterior ones. N otothyrial cavity deep and commonly narrow; low bladelike cardinal process; brachiophores well developed, bases strongly to weakly 

convergent. 

Platystrophia colbiensis Foerste 

Plate 5, figures 1-36; plate 7, figures 36-38, 40, 41 

Platystrophia colbiensis Foerste, 1910, Denison Univ. Sci. 

Lab. Bull., v. 16, p. 55, pl. 4, figs. 2A, B. 

Platyst1·ophia colbiensis Foerste. McEwan, 1919, U.S. Natl. 

Mus. Proc., v. 56, p. 414, pl. 44, figs. 8-11. 

Platyst1·ophia colbiensis var. mutata Foerste. McEwan, 1919, 

U.S. Natl. Mus. Proc., v. 56, p. 414-415, pl. 44, fig. 12. 

Species small to medium size for genus (table 1); 

subrectangular in outline with right angle cardinal 

extremities in most, in some rounded; hinge line 

straight and slightly less than maximum width 

(which occurs at middle lateral position), anterolateral margins evenly curved, anterior margin 

slightly curved or straight. Lateral profile equi-biconvex with even curvature from posterior to anterior; pedicle valve slightly flatter in some. Typical specimen has four plications on fold and three 

in sulcus (table 1); six to nine plications on flanks. 

Plications well defined, V-shaped profile with 

straight steep sides, rounded tops. Growth lines 

absent in most specimens. 

Brachial valve interarea orthocline, curved; beak 

slightly incurved to erect. No:tothyrium triangular, 

open. Floor of cavity curved and sloping st1e·eply 

toward anterior; part of floor formed by the curved 

lateral margins of the brachiophore bases (pl. 5, figs. 

34-36). Brachiophores thin, well defined, diverging, 

distinct upward curvature. Sockets deep, triangular 

slits (pl. 5,.fig. 34) in som,e, pit-like in most. Cardinal process a thin lo·w ridge. Posterior adductor 

scars well to moderately impressed ( pL 5, figs. 26-

30), some absent (pl. 5, figs. 34, 35), elongate ellips·oidal in outline with straight to moderately curved 

sides and distinctly pointed ant,erior ends (pl. 5, 

figs. 26-30). Anterior scars absent or very poorly 

defined in all specimens. Interior of valve crenulated throughout; crenula:tions are reflections of external plications (pl. 5, figs. 26-30, 34, 35). 

Pedicle valve interarea apsacline, slightly curved; 

beak erect. Teeth triangular; dental plates thin, descending straight to floor of valve and joining margins of ellipsoidal to oval-shaped muscle field (pl. 

5, figs. 32, 33). Field extends approximately onethird t.o one-half length of valve. Field elevated 

slightly above floor and defined by thin rims; some 

specimens with faint reflections of external plications. Interior of valve crenulated throughout. 

Discussion.-Platystrophia colbiensis is most like 

P. elegantula in size and g·eneral morphology. P. colbiensis is most easily distinguished from P. elegantula by its longer hinge line and slightly larger size 

at maturity. Figures 3 and 4 are scatter diagrams 

com·paring s·everal measur·ed parameters of these 

two species. See the discussion of P. elegantula for 

additional statements of these two spedes. 

20 0 

18 

• • 

• 

:::r: 16 • 1- 0 

0 

~14 • 0 

w 0 0 

(.!) 12 • • 

z • oo 

:::r: • 0 

10 • I 0 

0 

0 

0 

8 

0 

6 • 0 

4 • 

6 8 10 12 14 16 18 

MAXIMUM WIDTH 

20 22 24 

FIGURE 3.-Scatter diagram showing the relationship between the maximum width and width at the hinge line 

of specimens of P. elegantula and P. colbiensis. The specimens of P. elegantula (open circles) are from the Tanglewood Limestone Member of the Lexington Limestone 

(USGS colln. D1204-CO and 4982-CO; USNM 189575 

and 189576). The specimens of P. colbiensis (solid circles) 

are from the Clays Ferry Fonnation; (USGS colln. 

7812-CO; USNM 189574). All measurements are in 

millimeters. 
B10 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

22 

20 

18 

I 

b16 

~ 

~14 

::::> 

~ 

>< <! 12 

~ 

10 

8 

6 

• 

• 

4 6 

• • 

•o 

• 

0 0 

eo 

I 

0 

0 

8 10 12 

SHELL LENGTH 

0 

• • 

~ • 0 

14 16 

FIGURE 4.-Scatter diagram showing the relationship between the maximum width and shell length of specimens of Platystrophia elegantula and P. colbiensis. 

The specimens of P. elegantula (open circles) are from 

the Tanglewood Limestone Member of the Lexington 

Limestone (USGS colin. D1204-CO and 4982-CO; 

USNM 189575 and 189576). The specimens of P. colbiensis (solid circles) are from the Clay.s Ferry Formation (USGS colin. 7812-CO USNM 189574). All 

measurements are in millimeters. 

Occurrence and stratigraphic distribution.-

Platystrophia colbiensis Foerste is the most abundant species of the genus occurring in the Middle 

Ordovician of Kentucky. Numerous specimens occur 

in the Lexington Limestone, particularly the Millersburg and Perryville Lim·estone Members, and 

the Clays Ferry Formation. 

Platystrophia colbiensis occurs in the following 

USGS collections: 4178-CO to 4180-CO, 4940-CO, 

5015-CO, 5016-CO, 5071-CO, 6128-CO, 6138-CO, 

6142-CO to 6144-CO, 6990 ?-CO, 7044 ?-CO, 7049 ?-

CO, 7050 ?-CO, 7051-CO, 7056 ?-CO, 7057-CO, 7079-

CO, 7310 ?--CO, 7314 ?~co, 7327-CO, 7328 ?-CO, 

7332-CO, 7335-CO, 7343 CO, 7344-CO, 7348-CO, 

7349--"CO, 7353-CO, 7812-CO, D1367?-CO, D1172?-

CO, D1173-CO. 

Platystrophia elegantula McEwan 

Plate 5, figures 54-65, 70, 71; plate 7, figure 39 

Platystrophia elegantula McEwan, 1919, U.S. Natl. Mus . 

Proc., v. 56, p. 410-411, pl. 43, figs. 44-47. 

Platystrophia elegantula var. triplicata McEwan, 1919, U.S. 

Natl. Mus. Proc., v. 56, p. 411, pl. 43, fig. 48. 

Playstrophia elegantula var. amplisulcata McEwan, 1919, 

U.S. Natl. Mus. Proc., v. 56, p. 411-412, pl. 43, fig. 49. 

Species small for the genus (tables 2 and 3) : 

• ellipsoidal in outline with cardinal extremities obtusely rounded (pl. 5, figs. 56, 57, 61, 62) ; hinge 

line straight and two-thirds as wide as the maximum shell width (which occurs slightly anterior of 

the middle) (pl. 5, figs. 56, 61) . Lateral margins 

rounded and leading evenly into a rounded anterior 

margin. Lateral profile biconvex with brachial valve 

slightly thick·er (pl. 5, fig. 60) ; pedicle valve typically flatter across middle than brachial valve. Beak 

of pedicle valve extends slightly more to posterior 

than brachial beak. Plications on fold range from 

4 to 6 (me·asurements, tables 2, and 3), from 3 to 

5 in sulcus; plications on flanks range from 7 to 

12. Plications low and rounded. Growth lines absent. 

Brachial valve inter area anacline, curved. N otothyrium open, triangular; cardinal process low ridge 

TABLE 1.-Measurements, in millimeters, and number of plications in a suite of specimens of Platystrophia colbiensis 

Foerste, Clays Fe1·ry Formation, Shawhan quadrangle, Kentucky 

[USGS collection 7812-CO; all specimens cataloged as USNM 189574. Collected from east side of U.S. Highway 27 just south of junction with U.S. 

Highway 62. Leaders ( ___ ) indicate not countable] 

Length Hinge width Mid-width Thickness Plications on Plications in Plications on fold sulcus flank 

4.5 ---------------------- 4.3 6.3 2.8 

5.5 ---------------------- 6.1 7.2 3.6 4 3 8 

8.0 ---------------------- 10.4 11.0 4.5 4 3 7 

8.5 ---------------------- 10.7 11.5 5.9 4 3 7 

8.3 ---------------------- 10.0 12.1 6.2 4 3 6 

9.0 ---------------------- 10.2 12.1 5.8 4 3 7 

10.0 ---------------------- 11.7 13.3 12.9 4 3 8 

11.0 ---------------------- 12.3 15.0 8.8 4 3 8 

11.0 ---------------------- 14.0 15.2 9.3 4 3 7 

11.2 ---------------------- 12.5 15.7 7.9 4 3 7 

12.9 ---------------------- 16.0 18.0 10.2 4 3 9 

14.0 ---------------------- 17.5 18.0 12.0 4 3 8 

14.1 ---------------------- 17.6 19.3 12.6 4 3 8 

13.5 ---------------------- 17.1 18.7 13.6 4 3 8 
THE BRACHIOPOD GENUS PLATYST~OPHIA Bll 

that extends entire length of cavity; cavity floor 

elevated above valve floor and sloping ant~eriorly. 

Brachiophores thick with prominent shelf on inner 

face. Sockets deep. Posterior adductor scars faintly 

preserved as small oval impressions in a few specim,ens; most specimens lack obs·ervable scars. Interior of valve faintly crenulated. 

Pedicle valve interarea anacline. Delthyrium triangular and open; cavity walls. sloping outward. 

Dental plates moderately thin, join margins of 

muscle field; field small, ~ellipsoidal with straight 

sides, extends only about one-third length of valve. 

Interior of valve crenulated in anterior two-thirds 

of valve. 

D'iscussion.-Platystrophia elegantula has some 

easily recognizable characteristics that differentiate 

it from P. colbiensis, the only other small species in 

the Kentucky collections. (See figs. 3, 4 for a comparis'on of P. elegantula and P. colbiensis.) P. elegantula is characterized by its regular ·ellipsoidal to 

almost oval outline, its short hinge line, and the 

variation :Shown by the number of plications on the 

fold, in the sulcus, and on the flanks (tables 2, 3). 

Internally P. elegantula is differentiated from P. 

colbiensis by the presence of only faint internal 

crenulations-compared to the prominent crenulations in P. colbiensis. 

Occurrence and stratigraphic distribution.-Platystrophia elegantula McEwan is not an abundant species in the Kentucky collections. It occur:S most 

abundantly in the upper parts of the Lexington 

Limestone, particularly in the Millersburg and Tanglewood Limestone Members. Specimens that are 

questionably referred to P. elegantula (because of 

too few specimens and poor pr·eservation) also occur in the Perryville Limestone Member of the Lexington Limestone and the Clays Ferry Formation. 

Platystrophia elegantula occurs in the following 

USGS collections: 4898~CO, 4982--CO, D1204-CO. 

Platystropbia acutilirata (Conrad) 

Plate 6, figures 50-54; plate 7, figures 1-3 

Delthyris acutilirata Conrad, 1842, A cad. N atl. Sci. Philadelphia Jour. v. 8, p. 260, pl. 14, fig. 15. (fide McEwan, 

1919, U.S. Nat!. Mus. Proc., v. 56, p. 424). 

Orthis (Platystrophia) biforata var. acutilirata Conrad. 

Meek, 1873, Ohio Geol. Survey, Repts., v. 1, pt. 2, p. 

119-121, pl. 10, figs. 5a-g. 

Platystrophia acutilirata (Conrad). McEwan, 1919, U.S. 

Nat!. Mus. Proc., v. 56, p. 424-425, pl. 45, figs. 20-21. 

Platy;trophia acutilirata var. prolongata Foerste, 1910, Denison Univ. Sci. Lab. Bull., v. 16, p. 67, pl. 3, figs. Sa-b. 

Platystrophia acutilirata var. inflata, Foerste, 1910, Denison 

Univ. Sci. Lab. Bull., v. 16, p. 67, pl. 4, fig. 8. 

Platystrophia acutilirata var. senex Cumings. McEwan, 1919, 

U.S. N atl. Mus. Proc., v. 56, p. 426, pl. 45, fig. 23. 

TABLE 2.-Measurements, in millimeters, and numbers of plications in a suite of specimens of Platystrophia elegantula 

McEwan, Tanglewood Limestone Member of the Lexington Limestone, Frankfort Bast quadrangle, Kentucky 

[USGS collection 01204-CO; all specimens cataloged as a suite as USNM 189575. Collected from 229 ft above the top of the Tyrone Limestone along Interstate Highway 64 East, at the Kentucky River crossing (Frankfort East A Section). Leaders ( ___ ) indicate not measureable] 

Length Maximum width Hinge width Thickness Plications on Plications in Plications on fold sulcus flank 

9.0 ---------------------- 11.4 6.2 5.5 6 5 8 

10.9 ---------------------- 12.8 7.0 7.0 5 4 7 

11.6 ---------------------- 15.8 8.9 8.8 5 4 8 

13.0 ---------------------- 17.7 12.0 10.8 6 5 8 

13.0 ---------------------- 17.2 11.8 11.4 5 4 8 

14.9 ---------------------- 20.5 10.2 6 5 7 

12.9 ---------------------- 17.8 10.0 10.5 5 4 8 

TABLE 3.-Measurements, in millimeters, and numbers of plications in a suite of specimens of Platystrophia elegantula 

McEwan, Tanglewood Limestone Member of the Lexington Limestone, Frankfort West quadrangle, Kentucky 

!"USGS collection 4982-CO; all specimens cataloged as USNM 189576. Collected from 32 ft above the base of the Brannon Member of the Lexington Limestone along Interstate Highway 64, west of the Kentucky River Bridge crossing (Frankfort West A Section). Leaders ( ---) indicate not measurable] 

Length Maximum width Hinge width Thickness Plications on Plications in Plications on fold sulcus flank 

10.0 ---------------------- 13.3 13.0 6.6 6 5 8 

10.7 ---------------------- 14.4 9.2 7.7 4 3 8-9 

11.3 ---------------------- 17.0 13.2 9.2 5 4 9 

12.0 ---------------------- 17.0 10.8 9.5 5 4 9 

14.2 ---------------------- --- 10.5 9.8 6 5 7 

12.8 ---------------------- 17.7 9.7 9.6 4 3 12 

13.1 ---------------------- --- 14.0 9.3 6 5 9 

14.0 ---------------------- 15.2 10.9 5 4 10 

14.7 ---------------------- 20.4 14.0 13.0 6 5 10 

15.7 ---------------------- 21.0 15.6 13.5 5 4 9 
B12 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Species moderate size for the genus. (The measurements for the most ·Complete specimen are: 

length, 19.2 mm; hinge width, 28.7 mm; thickness, 

18.0 mm.) Sub rectangular in outline with cardinal 

extremities slightly acute. Hinge line straight and 

marks widest part of shell. Lateral margins straight 

to slightly curved, anterior margin straight. Brachial and pedicle valves evenly convex in lateral profile, brachial valve slightly thicker. Little increase 

in fold height from posterior to anterior; 4 plications on fold, 3 in sulcus, 12-14 on flanks. Fold and 

sulcus plications larger than flank plications; flank 

plications low and well rounded, fold and sulcus pHcations more angular. Brachial valve interarea 

anacline, pedicle valve int·erarea apsacline. Brachial 

and pedicle beaks :slightly incurved. 

Discussion.-This species is rare in the Kentucky 

collections; only about five specimens were identified. 

The one outstanding external feature about P. 

acutilirata is the conspicuous difference betw·een the 

size of the plications on the fold and sulcus and 

those on the flanks. No interiors were present in the 

collections, and thus no conclusions can be made regarding internal characteristics. 

The tw·o varieties, P. acutilirata prolongata 

Foerste and P. acutilirata senex Cumings, are regarded here as intraspecific variants of P. acutilirata, and no useful purpose is served by designating 

them separate taxa. McEwan stated (1919, p. 426) 

that both varieties are commonly found associated 

with typical P. acutilirata specimens. . 

The specimens of P. acutilirata studied by 

McEwan (1919) are like those occurring in the 

K·entucky collections except for a difference in outline. McEwan's specimens have a much longer hinge 

line which makes the cardinal extremities extremely 

acute (pl. 7, fig. 1). The specimens from Kentucky 

are more subquadrate in outline. (Compare pl. 6, 

fig. 50 with pl. 7, fig. 1.) 

Occurrence and stratigraphic distribution.-This 

species is rare in Kentucky and is found only in the 

Bull Fork Formation. Platystrophia acu.tiUrata occurs in USGS collection 5309-CO. 

PlatystropLia annieana Foerste 

Plate 3, figures 1-45; plate 4, figures 1-15, plate 5, figures 37, 

38; plate 7, figures 4-8 

Platystrophia annieana Foerste, 1910, Denison Univ. Sci. 

Lab. Bull., v. 16, pl. 6, fig. 14. 

Platystrophia annieana Foerste. McEwan, 1919, U.S. Natl. 

Mus. Proc., v. 56, p. 423, pl. 46, figs. 20-24. 

Species medium to large for the genus (measurements, table 4) ; subquadrate to subrectangular in 

outline; cardinal extremities vary from slightly 

rounded to right angle to acut;e. Lateral margins 

more typically curved leading smoothly into curved 

anterior margin. Biconvex in lateral profile with 

brachial valve slightly deeper, S·Ome specimens almost twice as deep; rate of curvature decreases in 

anterior half of shell and is distinctly less than in 

posterior half (pl. 3, figs. 37-45) . Most specimens 

have 4 plications on fold and 3 in sulcus; flanks 

have 6 to 11. Plications broad with well-rounded 

tops, interplication troughs well rounded also; pHcations tend to "flare out" in anterior parts of shell. 

Growth lines absent in most specimens. 

Brachial interarea orthocline to slightly anacline, 

curv·ed and about one-half as long as pedicle interarea. Notothyrium open, triangular. Cavity deep, 

some elevated high above valve floor. Inner faces of 

brachiophores concave with inward-projecting 

ledges along lower parts, help·ing to form floor of 

cavity. Cardinal proc,ess a low ridge that extends 

full length of cavity, slightly thicker ant,eriorly. 

Brachiophores thick, curved upward and outward, 

pointed. Sockets triangular pits, poorly defined in 

most. Inside of valve crenulated throughout. Posterior adductor scars circular in outline (pl. 4, fig. 

3), anterior scars somewhat triangular with gently curved margins (pl. 4, fig. 3). 

Pedicle interarea apsacline, curved. Delthyrium 

triangular, open; walls of cavity sloping slightly 

outward. Dental plates thin to thick, join margins 

of ellipsoidal muscle field; field extends about onefourth length of valve and defined by thin to moderately thick rim. Interior of valve crenulat,ed. 

Discussion.-The largest specimens of this species slightly resemble intermediate-size specimens 

of P. ponderosa. However, P. annieana is easily differentiated from P. ponderosa by its smaller size 

(tables 4, 9), slightly more subrectangular outline 

compared to a more quadrate outline in P. ponderosa. Internally, P. annieana lacks a cruralium-like 

structure so charact,eristic of the brachial valves of 

P. ponderosa. Compare the brachial interiors of P. 

annieana (pl. 4, figs. 1-3 and 13, 14) and P. ponderosa (pl. 2, figs. 15-19). 

The specimens studied by McEwan (1919) agree 

in overall size, outline, and convexity with thos·e in 

the Kentucky collections. The one noticeable difference is that some of the Kentucky specimens have 

lower, much broader, and therefore less numerous 

plications than McEwan's specimens. Low broad 

plications like this are identical to those oc·curring 

in P. laticosta. The difference in number of plications is indicated somewhat by tables 4 and 5, although the size of the sample of McEwan's speci-
THE BRACHIOPOD GENUS PLATYSTROPHIA B13 

mens is much smaller than the suit~e from Kentucky. 

The average number of flank plications in the specimens studied by McEwan (table 5) is 10.5; the 

average number for the Kentucky specimens (table 

4) is 8. 

Occurrences and stratigraphic distribution.-

Platystrophia annieana Foerste is an abundant species in the uppermost part of the Kentucky Ordovician. Almost all of the large coHections in the. area 

are from the Preachersville Member of the Drakes 

TABLE 4.-Measurements in millimeters, and numbers of plications in a suite of specimens of Platystrophia annieana Foerste, 

Dillsboro Formation, Milan quadrangle, Indiana 

[USGS collection 7834-CO; all specimens cataloged as USNM 189577. Collected from section along U.S. Highway 50 east of Versailles, Ind. Leaders 

( ___ ) indicate not countable] 

Length Hinge width Mid-width Thickness Plication on Plications in Plications on fold sulcus flank 

9.0 ---------------------- 9.2 12.6 7.2 

10.3 ---------------------- 12.9 15.1 9.3 5 4 9 

11.4 ---------------------- 11.7 15.0 9.0 5 4 7 

8.5 ---------------------- 14.5 12.7 6.5 4 3 9 

10.0 ---------------------- 11.0 9.3 13.4 4 3 7 

11.3 ---------------------- 12.1 15.6 8.9 5 4 7 

11.7 ---------------------- 10.6 15.0 9.9 4 3 7 

12.9 ---------------------- 11.4 15.2 9.6 4 3 6 

11.9 ---------------------- 13.8 16.2 10.1 4 3 7 

12.8 ---------------------- 13.1 17.1 10.5 4 3 8 

13.4 ---------------------- 12.0 17.8 11.0 4 3 7 

11.9 ---------------------- 12.0 16.0 10.0 4 3 6 

11.7 ---------------------- 15.0 17.2 9.9 4 3 7 

13.0 ---------------------- 16.2 18.3 12.4 4 3 9 

14.4 ---------------------- 15.8 20.5 12.7 4 3 7 

13.0 ---------------------- 13.8 18.0 11.4 4 3 8 

13.7 ---------------------- 15.5 19.8 12.2 4 3 7 

13.2 ---------------------- 15.2 18.3 11.4 4 3 9 

12.6 ---------------------- 16.0 18.7 11.7 4 3 6 

13.5 ---------------------- 15.3 18.6 12.0 4 3 7 

13.8 ---------------------- 18.5 20.6 12.8 4 3 8 

13.5 ---------------------- 22.2 20.4 13.7 4 3 11 

14.0 ---------------------- 20.6 20.9 12.7 4 3 9 

15.7 ---------------------- 16.3 20.8 13.3 4 3 8 

14.4 ---------------------- 20.3 21.0 12.0 4 3 9 

16.0 ---------------------- 19.3 23.4 15.0 5 4 11 

16.3 ---------------------- 17.8 21.8 13.7 5 4 8 

17.3 ---------------------- 20.0 23.3 13.7 4 3 7 

15.5 ---------------------- 20.5 22.0 12.5 4 3 10 

16.9 ---------------------- 20.3 23.8 17.8 4 3 9 

18.0 ---------------------- 27.1 26.7 16.2 4 3 6 

18.5 ---------------------- 28.3 27.3 18.9 4 3 9 

20.3 ---------------------- 29.0 30.0 20.1 6 5 9 

TABLE 5.-Measurements, in millimeters, and numbers of plications of Platystrophia annieana from specimens studied by 

McEwan (191.9), and deposited in the U.S. National Museum 

Length Hinge width 

19.2 ---------------------- 28.7 

17.8 ---------------------- 32.0 

17.8 ---------------------- 29.3 

16.8 ---------------------- 23.9 

16.9 ---------------------- 30.4 

16.3 ---------------------- 25.0 

[Leaders (_ __ ) indicate not measurable] 

Mid-width 

25.6 

27.5 

26.0 

23.8 

25.0 

Thickness 

18.0 

15.0 

14.8 

15.5 

15.2 

18.2 

Plications in 

fold/sulcus 

4/3 

6/5 

4/3 

4/3 

4/3 

4/3 

Plications on Catalog number 

flanks (average) (USNM) 

11 

12 

13 

8 

10 

9 

65664 

65664 

65651 . 

65651 

39041 

.39041 
Bl4 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Formation in Kentucky and from Dillsboro Formation of Indiana. Well-preserved specim:ens and larg·e 

suites also occur in the lower parts of the Drakes. 

This species is conspicuously absent from all of the 

underlying formations. However, one collection 

from the Millersburg Member of the Lexington 

Limestone contains specimens that are very similar 

to specimens of P. annieana identified by McEwan. 

A typical specimen from this Millersburg suite is 

figured on plate 7 (figs. 34, 35). Figures of P. 

annieana identified by McEwan are also shown on 

plate 7 (figs. 4-8) for comparison. Platystrophia 

annieana occurs in the following USGS collections : 

4468--CO, 5308-CO, 6139-CO, 6140-CO, D1370eCO, 7834-CO. 

Platystrophia laticosta (Meek) 

Plate 5, figures 45-49; plate 6, figures 1-13, 19-28; plate 7, 

figures 17-21 

Orthis laticostata James, 1871, Catalog Lower Silurian Fossils, Cincinnati Group, p. 10 (fide F. B. Meek, 1873, 

Ohio Geol. Survey Repts., v. 1, pt. 2 (Paleontology), p. 

116). 

Orthis (Platystrophia) biforata var. laticosta Meek, 1873, 

Ohio Geol. Survey Repts., v. 1, pt. 2 (Paleontology), 

p. 116, pl. 10, fig. 4. 

Platystrophia laticosta (Meek). Foerste, 1903, Am. Geologist, 

v. 31, p. 334. 

Platystrophia unicostata Cumings, 1903, Am. Jour. Sci., 4th 

ser., v. 15, p. 28-29, pl. 31, fig. 15. 

Platystrophia laticosta Cumings. Foerste, 1910, Denison 

Univ. Sci. Lab. Bull., v. 16, pl. 3, figs. 1, 2. 

Platystrophia laticosta (Meek). McEwan, 1919, U.S. Natl. · 

Mus. Proc., v. 56, p. 432-433, pl. 48, figs. 11-13. 

Platystrophia unicostata Cumings. McEwan, 1919, U.S. Natl. 

Mus. Proc., v. 56, p. 433-434, pl. 48, figs. 4-7. 

Platystrophia unicostata var. crassiformis McEwan, 1919, 

U.S. Natl. Mus. Proc., v. 56, p. 434, pl. 48, figs. 8-10. 

Subquadrate to rectangular in outline·; rounded 

cardinal extremities, right angled to obtuse in some. 

Hinge line straight and shorter than mid-width. 

Fold and sulcus well developed and having an anterior 'thrust" when viewed laterally; prominence 

of fold accentuated by high, straight-sided marginal 

plications that descend to the flanks of the valve. In 

some specimens fold is elevat,ed high above flanks of 

valve (pl. 5, fig. 50) with flanks sloping steeply to 

cardinal extremities; in some specimens extremities 

concave. Plications are pronounced, sharply angular 

(pl. 6, figs. 25-27). Fold with four plications in 

most specimens and three in sulcus; som'e specimens having prominent plication in sulcus (pl. 5, 

fig. 51). In lateral view curvature from posterior 

to anterior rather straight in both valves (pl. 5, fig. 

49) ; lateral commissure rectimarginate, anterior 

commissu~e strongly uniplicate. Pedicle and brachial 

beaks erect to suberect, a few strongly incurved. 

Flanks with six to eight angular plications. 

No interiors of either brachial or pedicle valves. 

Discussion.-The entire range of forms normally 

~eferred to by most workers as either Platystrophia 

laticosta, P. unicostata, or P. cypha comprises a 

highly variable group having numerous intermediates that are sometimes difficult to identify with 

any degree of confidence. McEwan (1919) clearly 

intimated the pres·ence of such intermediates and 

variations by erecting several varieties of P. unicostata and P. cypha and by such statements as 

(1919, p. 432), "The chief distinction between 

Platystrophia laticosta and P. cypha is one of degre,e" and (1919, p·. 433), 11Platystrophia unicostata 

is connected with Platystrophia laticosta by all degrees of variants." 

None of these species i,s abundantly present in the 

Kentucky collections; approximat.ely 10 specim,ens 

were · identified from 2 or 3 localities and stratigraphic intervals. It is difficult to properly evaluate 

intermediates, ranges of variation, and degr,ees of 

overlap from such limited data. Nevertheless, granting that clear demarcation among these three 

"species" is difficult, I have chosen to refer to 

members of this group as either P. laticosta or P. 

cypha. I interpret P. unicostata to be synonomous 

with P. laticosta. This interpretation is made because P. laticosta and P. unicostata are more similar 

in outline and profile and have approximately the 

same num.bers of plications in the sulcus, on the fold, 

and on the flanks. P. cypha has a re;ctangular outline 

with an elongated hinge line and pronounced elevation of the fold. P. cypha is the only one with a 

marked concavity to the flanks of the pedicle valve. 

I have examined specimens of all three species 

studied by McEwan (1919) and deposited in the 

United States National Museum. P. laticosta and P. 

unicostata are more similar to each other than either 

is to P. cypha. The data presented in tables 6-8 give 

some indication of these similarities and differences. 

The outstanding difference that distinguishes P. 

cypha from P. laticosta and P. unicostata is the number of plications on the flanks of the shell. The plications on P. laticosta and P. unicostata tend to be 

broader with long gentle slopes; tho·se on P. cypha 

tend not to be as angular and are closer together 

(pl. 7, figs. 28 and 29). 

Occurrence and stratigraphic distribution.-

Platystrophia laticosta is about as abundant as P. 

cypha in the Kentucky collection, occurring mostly 

in the Ashlock Formation, although specimens 

questionably referred to P. laticosta are also found 
THE BRACHIOPOD GENUS PLATYSTROPHIA B15 

in the Bull Fork Formation and Grant Lake Lime .. 

stone. PlatystTophia laticosta occurs in the following USGS collections: 5135-CO, 5136-CO, 5140-CO, 

D1244-CO, D1253 ?-CO, D1288-CO, D1289-CO, 

D1367-CO. 

Platystropbia cypba (James) 

Plate 5, figures 39, 40, 43, 44, 50, 52; plate 6, figures 14-18, 

29-32; plate 7, figures 22-29 

Orthis (Platystrophia) cypha James, 1874, Cincinnati Quart. 

Jour. Sci., v. 1, p. 20, not figured (fide McEwan, 

1919, U.S. Natl. Mus. Proc., v. 56, p. 435). 

TABLE 6.-Measurements, in millimeters, and numbers of pl1cations of Platystrophia laticosta, from specimens studied by 

McEwan (1919) and deposited in the U.S. National Museum 

Length Hinge width 

20.6 ---------------------- 34.6 

21.2 ---------------------- 37.0 

18.2 ---------------------- 28.1 

18.8 ---------------------- 32.5 

20.0 ---------------------- 31.9 

18.2 ---------------------- 30.6 

20.4 ---------------------- 32.3 

16.9 ---------------------- 26.0 

Mid-width 

28.2 

29.9 

27.5 

26.8 

27.9 

26.7 

30.2 

24.0 

Thickness 

29.6 

27.5 

18.1 

16.4 

22.8 

17.2 

19.0 

15.5 

Plications in Plications on Catalog number 

fold/sulcus flank (average) (USNM) 

4/3 5 50946 

4/3 8 50946 

4/3 6 50946 

4/3 8 50946 

4/3 6 50946 

4/3 6 48605 

4/3 7 48605 

4/3 8 48605 

TABLE 7.-Measurements, in millimeters, and numbers of plications of Platystrophia cypha, from specimens studied by 

McEwan (1919) and deposited in the U.S. National Museum 

Length Hinge width 

19.0 ---------------------- 34.4 

17.1 ---------------------- 31.9 

18.2 ---------------------- 34.4 

17.0 ---------------------- 30.6 

19.0 ---------------------- 32.1 

15.6 ---------------------- 28.4 

18.0 ---------------------- 32.9 

17.1 ---------------------- 29.5 

16.0 ---------------------- 31.9 

18.7 ---------------------- 32.8 

15.0 ---------------------- 27.9 

16.3 ---------------------- 28.9 

16.7 ---------------------- 25.3 

16.1 ---------------------- 25.2 

[Leaders ( ___ ) 

Mid-width 

29.6 

26.0 

27.2 

24.1 

28.9 

23.0 

20.0 

23.4 

25.0 

24.9 

22.4 

24.2 

25.8 

22.4 

indicate not measurable] 

Thickness 

14.9 

17.4 

20.9 

16.5 

19.1 

17.8 

25.6 

·16.0 

19.5 

14.4 

18.5 

17.5 

15.7 

Plications in 

fold/sulcus 

4/3 

4/3 

4/3 

4/3 

6/5 

4/3 

4/3 

4/3 

4/3 

4/3 

4/3 

4/3 

4/3 

Plications on Catalog number 

flank (average) (USNM) 

15 

8 

11 

12 

10 

8 

10 

11 

9 

10 

9 

10 

6 

6 

66001 

66001 

66001 

66001 

66001 

66001 

66001 

66009 

66009 

66009 

66009 

66009 

66009 

66009 

TABLE B.-Measurements, in millimeters, and numbers of plications of Platystrophla unicostata, from specimens studied by 

McEwan (1919) and deposited in the U.S. National Museum 

Length Hinge width Mid-width Thickness Plications in Plications on Catalog number 

fold/sulcus flank (average) (USNM) 

16.9 ---------------------- 26.0 22.3 19.0 4/3 6 65969 

17.8 ---------------------- 26.8 22.4 18.3 3/2 7 65969 

19.7 ---------------------- 27.7 21.0 17.4 4/3 6 65970 

18.4 ---------------------- 26.2 25.2 20.5 4/3 6 39037 

23.0 ---------------------- 32.1 26.9 24.4 4/3 6 39037 

22.4 ---------------------- 33.5 27.6 20.2 4/3 6 39037 

18.6 ---------------------- 27.9 25.4 20.8 3/2 6 39037 

23.2 ---------------------- 30.4 23.8 22.3 2/1 7 65968 

19.7 ---------------------- 29.0 25.0 21.4 3/2 6 65968 

19.4 ---------------------- 28.9 26.7 18.8 3/2 5 65968 

15.0 ---------------------- 24.5 21.2 19.1 2/1 5 65968 

18.5 ---------------------- 26.8 24.1 18.2 4/3 7 65968 

21.5 ---------------------- 27.6 25.6 18.2 4/3 6 65968 

" 
B16 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Platystrophia cypha Cumings. Foerste, 1910, Denison Univ. 

Sci Lab. Bull., v. 16, p. 61, pl. 4, fig. lOa, b; 12 pl. 5, 

fig. 11. 

Platystrophia cypha (James). McEwan, 1919, U.S. Nat!. 

Mus. Proc., v. 56, p. 435-436, pl. 47, figs. 22-25; pl. 

48, figs. 14-16. 

Platystrophia cypha var. tumida McEwan, 1919, U.S. Nat!. 

Mus. Proc., v. 56, p. 436-437, pl. 48, figs. 17-20. 

Platystrophia cypha var. arcta McEwan, 1919, U.S. Natl. 

Mus. Proc., v. 56, p. 437, pl. 48, figs. 1-3. 

Platystrophia cypha var. bellatula McEwan, 1919, U.S. Natl. 

Mus. Proc., v. 56, p. 438, pl. 47, figs. 28-30. 

Moderate size for genus (best preserved specimen: length, 16.0 mm; hinge width, 26.8 mm; midwidth, 23.7 mm; thickness, 16.1 mm; cardinal extremities acute to right angle. Hinge line the widest 

part, lateral margins straight, anterior margin 

straight. La.teral profile unequally biconvex with 

brachial valv~e about twice as deep; fold rises steadily from posterior to highest anterior extremity. 

Fold has four plications, two middle ones prominent 

with two lateral ones only poorly to, moderately 

developed; six to seven plications on flank. Sulcus 

deep, bordered on each side by two prominent highly elevated plications. Flank of pedicle valve, distinctly concave with asymm·etrical pHcations; plication slopes facing cardinal extremities twice as long 

as opposite slopes. Flanks of brachial valve slightly 

convex, uneven plications. 

No interiors preserved. 

Discussion.-As pointed out in the discussion of 

P. laticosta, all degrees of intermediates exist between P. cypha, P. unicostata, and P. laticosta, 

which makes interpr,etation of these species difficult. 

I have studied many of the types designated by 

McEwan (1919) and deposited in the U.S. National 

Museum. In addition to the similarities between P. 

cypha, P. unicostata, and P. laticosta, certain specimens designated by McEwan as P. clarksvillensis 

are nearly identical to some designated as P. cypha. 

I have tried to show this. similarity by figuring 

several of McEwan's specimens (pl. 7, figs. 30-33) 

of P. clarksvillensis. Also, McEwan (1919, p. 422) 

claimed that P. clarksvillensis "bears a marked resemblanc~e to Platystrophia laticosta." In my opinion 

just as much similarity exists between P. cypha 

and P. clarksvillensis as between P. cypha and P. 

laticosta. Such degrees of variation and similarities 

p1oint up the need for a complete reevaluation of 

the genus, as well as the difficulty of specific 

des.igna tions. 

Occurrence and stratigraphic distribution.-Platystroph?:a cypha occurs in a s.cattering of collections 

throughout the upper part of the Upper Ordovician 

in the Ashlock Fonnation, Grant Lake Limestone, 

and Bull Fork Form~ation and the Preachersville 

Member of the Drakes For.m.a;tion. Platystrrophia 

cypha occurs in the fo.llowing USGS colle·ctions: 

4466-CO, 6418-CO, D1248 ?-CO, D1253-CO, D1280-

CO, D1370e--CO. 

Platystrophia ponderosa Foerste 

Plate 1, figures 1-21; plate 2, figures 1-27; plate 4, figures 

16, 18-33 

Platystrophia ponderosa Foerste, 1909a, Denison Univ. Sci. 

Lab. Bull., v. 14, p. 225, pl. 4, fig. 14. 

Platystrophia ponderosa Foerste, 1912, Ohio Naturalist, v. 

12, p. 453, pl. 22, fig. 11 (fide McEwan, 1919, U.S. 

Natl. Mus. Proc., v. 56, p. 427). 

Platystrophia ponderosa Foerste. McEwan, 1919, U.S. Natl. 

Mus. Proc., v. 56, p. 427-428; pl. 49, figs. 1-5; pl. 50, 

figs. 4-7; pl. 51, figs. 1-5; pl. 52, figs. 1-3, 7-10. 

Platystrophia ponderosa var. auburnensis Foerste. McEwan, 

1919, U.S. Natl. Mus. Proc., v. 56, p. 428, pl. 49, figs. 

9-12. 

Platystrophia ponderosa var. arnheimensis McEwan, 1919, 

U.S. Nat!. Mus. Proc., v. 56, p. 428, pl. 51, figs. 6-8. 

Species large for the genus (measurements, table 

9). Shell thick in mature spedmens. Quadrate to subquadrate in outline; cardinal extremities at a right 

angle in most specimens but slightly acute or "spirif.eroid" in others, some small specimens obtuse. Pedicle sulcus and brachial fold prominent, shallow to 

moderat~ely deep. Most specim~ns with four plications on fold and three in sulcus (t:able 9, range of 

variation) ; six to eight plications on flanks. Plications broad with gently rounded tops. Hinge line 

straight and :approxi,mately the widest part ( measurements, table 9) . Lateral profile evenly biconvex 

with thickest part in or near middle; rate of curvature from posterior to anterior nea.rly equal in both 

valves. Lateral commissure rectimarginate, anterior 

com.missure uniplicate. Growth lines weak or absent. 

Brachial and pedicle interareas slightly curved; pedicle interar.ea apsacline and slightly longer than anacline brachial interarea. Brachial beak slightly incurved, pedicle beak suherect. 

Delthyrium triangular, open, moderately deep; 

walls slightly farther apart at base of ·cavity than at 

top. Dental plates thin in small specimens, thick in 

large specimens; anterior margins of plates descend 

straight to floor of valve, some slope to po.steTior. 

Plates join margins of muscle field; field elliptical in 

outline and extends about one-third length of valve 

(pl. 2, fig. 24) . Faint rim around field in s·mall and 

medium-sized specimens; rim more pronounced in 

larger specimens (pl. 2, fig. 22). Margins of field 

parallel, diverging slightly in some specimens. Adductor sears not visible or poorly developed in most 

specimens. Faint groove along base of each dental 

plate might be adjustor soor. 
THE BRACHIOPOD GENUS PLATYSTROPHIA B17 

TABLE 9.-Measurements of several dimensions (in millimeters) and numbers of plica,tions in a suite of Platystrophia 

ponderosa Foerste f'rom a single collection (USGS colln.-4.556-CO; USNM 189578) from the Back Bed, Tate Member 

of the Ashlock Formation in the Richmond North quadrangle, Kentucky 

Length Hinge width 

20.9 --------------------------- 27.8 

20.2 --------------------------- 25.2 

27.7 --------------------------- 29.4 

29.1 --------------------------- 34.5 

32.5 --------------------------- 33.7 

33.7 --------------------------- 35.0 

26.0 --------------------------- 30.5 

27.5 --------------------------- 28.5 

27.2 --------------------------- 35.3 

24.8 --------------------------- 33.3 

28.4 --------------------------- 34.0 

28.4 --------------------------- 30.7 

25.6 --------------------------- 31.5 

28.8 --------------------------- 35.7 

29.6 --------------------------- 36.5 

28.0 --------------------------- 34.5 

28.5 --------------------------- 32.0 

20.4 --------------------------- 27.6 

20.5 --------------------------- 30.7 

24.8 --------------------------- 32.4 

23.0 --------------------------- 22.4 

19.3 --------------------------- 23.8 

28.2 --------------------------- 29.1 

28.7 --------------------------- 24.3 

29.5 ----------------·----------- 36.1 

23.0 --------------------------- ~0.4 27.5 --------------------------- 30.0 

17.0 --------------------------- 19.2 

19.4 --------------------------- 25.0 

20.7 --------------------------- 27.5 

30.9 --------------------------- 38.7 

27.8 --------------------------- 37.8 

26.0 --------------------------- 31.0 

23.7 --------------------------- 31.8 

Mid-width 

25.7 

24.5 

33.5 

37.0 

37.1 

36.5 

31.0 

31.5 

34.0 

32.3 

33.8 

33.3 

33.0 

35.8 

35.3 

32.5 

35.6 

27.3 

27.7 

29.8 

21.8 

25.4 

33.6 

33.2 

35.2 

37.7 

30.7 

20.0 

23.8 

26.5 

37.2 

36.0 

31.4 

29.6 

Thickness 

17.3 

15.0 

24.6 

20.7 

26.9 

31.0 

24.0 

23.5 

22.9 

20.4 

22.0 

23.5 

19.0 

24.0 

27.3 

23.2 

24.5 

15.8 

17.0 

18.3 

18.3 

15.2 

24.8 

24.4 

24.9 

27.5 

27.0 

12.0 

14.5 

15.4 

26.3 

24.5 

19.6 

18.3 

Plications on fold 

4 

4 

4 

4 

4 

4 

4 

5 

5 

4 

4 

4 

4 

4 

6 

4 

4 

4 

4 

5 

4 

4 

4 

6 

4 

4 

5 

5 

4 

4 

4 

4 

6 

5 

Plications in sulcus 

3 

3 

3 

3 

3 

4 

3 

4 

4 

3 

3 

3 

3 

3 

5 

3 

3 

3 

3 

4 

3 

3 

3 

5 

3 

4 

4 

4 

3 

3 

3 

3 

5 

4 

Notothyrium open, triangular; floor of cavity 

steeply sloping to anterior. Cardinal process a thin 

blade about one-fi£th as high as cavity is deep. Inner 

faces of brachiophores have variable slope, most 

slope inwa.rd and join a median ridge to form a. cruralium-like s·tructure (pl. 2, figs. 17-19). Brachiophores thick, moderat.ely de·ep sockets positioned on 

outer face at hinge line. Underside of brachiophores 

strongly curved to the posterior, many with keel-like 

ridge. Posterior adductors oval in outline, more deeply impressed ~and larger than anterior adductors (pl. 

2, fig. 27). Anterior adductors somewhat triangular 

and .straight sided. Faint median ridge extends from 

anterior .margin of notocavity to anterior margin of 

m usde field, joins with a more pronounced ridge that 

is a reflection of external plication. Interior of valve 

crenulated. 

Discussion.-Platystttophia pondettosa is the most 

abundant species of the genus in the Kentucky collections. Unlike many of the other species, specimens of 

P. pondettosa are easier to identify because of their 

distinctively large size, quadrate outline, and presence of a cruralium-like structure in the brachial 

valve. Not all the brachial valves, however, have the 

cruralium-like structure developed to the same degree a.s is shown on plate 2, figures 17-21. Figures 

15 and 16 on plate 2 show the differences in the 

appearance of this structure, although in both specimens it is unmistakably present. The pres·ence of 

such a structure in small specimens is not as obvious, 

but indications of it do occur in some. Figure 21 on 

plate 2 is an enlarged view of a specimen 2-3 mm 

wide, in which the inward-sloping brachiophore 

bases and the median ridge are clearly visible. 
B18 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

The variable appearance of the cruralium is due ;to 

the difference in the degree of slope of the brachiophore bases and the degree to which the undersides 

of the brachiophores curve toward the posteTior. 

Some of the brachiophore bas.es are distinct plates 

(pl. 2, figs. 18 and 19), but others are not as well 

developed and the undersides of the· brachiophores 

have a distinct posterior curvature (plate 2, fig. 17). 

Many specimens are represented by large broken 

fragments of Platystrophia ponderosa with only the 

beak regions preserved (·pl. 4, figs. 24--27). Nevertheless, these fragments have characteristics such as 

a robust shell, ·cruralium-like appearance of the 

brachial valve, and long muscle-scar region of .the 

pedicle valv-e, which make it relatively ·easy to identify them as P. ponderosa. 

Platystrophia annieana is the only other species in 

the Kentucky collection that approaches. the size o.f 

P. ponderosa, although none of the largest specimens 

is nearly as large as full-sized P. ponderosa. Also, 

the brachial valves o.f P. annieana lack the cruraliumlike structure so prominent in P. ponderosa. P. annieana is more rectangular in outline compar·ed to 

the more quadrate outline of P. ponderosa. 

Occurrence and stratigraphic distribution.-In the 

Upper Ordovician o.f Kentucky, Platystrophia pon-

. derosa is probably the most widely distributed and 

most eas.ily recognizabl·e :species of the genus. It is 

well represented in the Calloway Creek, Fairview, 

Ashlock, Grant Lake, Bull Fork, and Drakes Formations, but it is. nost found in the Preachersville Member of the Drak·es (the uppermost Ordovician strata 

in Kentucky). Platyst1·ophia ponderosa occurs in the 

following USGS collections: 4194-CO, 4195-CO, 

4208-CO to 4211--CO, 4464-CO, 4467 -CO, 4556-CO, 

5039-CO, 5120-CO, 5137?-CO, 5141-CO, 6127-CO, 

6284-CO, 6409 ?-CO, 6410-CO to· 6412-CO, 6414--CO, 

6416--CO, 7702 ?-CO, 7703-CO, 7704--CO, 7705 ?-CO, 

7706--CO, 7707_.CO, 7708 ?-CO, 7936 ?-CO, 7937-CO, 

D12·39_JCO, D1241 ?-CO, D1244-CO, D1247-CO, 

D1267--CO, D1273--CO, D1276-CO, D1277-CO, 

D1327-CO, D1333-CO, D1334--CO, D1336--CO to 

D1341--CO,. D1344--CO, D1345?-CO, D1347-CO, 

D1349-CO, D1365--CO, D1367-CO to D1369--CO. 

Platystropbia cf. P. foerstei McEwan 

Plate 6, figures 33-41 

Platystrophia foerstei McEwan, 1919, U.S. Natl. Mus. Proc., 

v. 56, p. 420-421, pl. 46, figs. 9-12. 

Platystrophia foerstei var. ampla McEwan, 1919, U.S. Natl. 

Mus. Proc., v. 56, p. 421, pl. 46, figs. 13-16. 

Species moderate s:ize for genus; measurements 

for the two most ·complete specimens are as follows: 

Length 

(mm) 

Mid-width 

(mm) 

15.7 ------------ 23.0 

15.0 ------------ 20.2 

Hinge width 

(mm) 

17.0 

15.9 

Thickness 

(mm) 

14.0 

14.4 

Subquadrate in outline with cardinal extremities 

distinctly rounded. Hinge line straight and shorter 

than maximum width, which is at mid-line; lateral 

margins rounded, anterior margin fairly straight. In 

lateral view, brachial and pedicle valves evenly 

rounded from posterior to anterior; brachial valve 

slightly thicker. Brachial int.erarea curved and orthocline, pedide interarea ·curved and apsacline; both 

beaks erect. Lateral .co•mmissure rectimarginat·e, anterior commissure uniplicat•e. Brachial fold with 4-6 

plications, flanks with 10 or 11; fold moderate in 

height, increases slightly toward anterior. 

No interiors in collections. 

Discussion.-Few·er than 10 articulated specimens 

are pres,ent in the Kentucky collections; all from the 

same sample. All are about the same size and outline 

but several .incomplete spedmens are considerably 

thinner than the figured (pl. 6, figs. 33-41) and 

measured s.peeimens. Platystrophia ·Cf. P. foerstei 

occurs in the following USGS collection D1347-CO. 

Platystropbia sp • 

Plate 6, figures 42-46 

Discussion.-The specimen figured on plate 6, 

figures 42-46 occurs .about 150 feet above the base 

of the Tate M·ern.ber of the Ashlock Formation in a 

s,mall colle·ction of broken and articulated .spedmens. 

The other specimens. in the suite are not nearly so 

bulbous but .are like the specimens figured on plate 6, 

figures 1-13; they are referred to Platystrophia laticosta. The specimen figured here· (figs. 42-46) resembles ·externally Platystrophia p1·ecursor Foerste, 

but because it is the only s:pecim·en in a suite that is 

predominantly Platystrophia laticosta, a specific 

designation seems unj usti•fied. A-ccording to McEw:an 

(1919), P. precursor Foerste is a Middle Ordorvician 

( Trentonian) species in Kentucky occurring in the 

Cynthiana Limestone. The specimen fi~gured here is 

from the Ashlock Formation, which is considered to 

be Upper Ordovician (May.svillian). Platystrophia 

sp. occurs in USGS collection D1292--CO. 

REFERENCES CITED 

Alberstadt, L. P., 1973, Articulate brachiopods of the Viola 

Formation (Ordovician) in the Arbuckle Mountains, 

Oklahoma: Oklahoma Geol. Survey Bull. 117, 67 p., 

pis. 1-9. 
THE BRACHIOPOD GENUS PLATYSTROPHIA B19 

Bates, D. E. B., 1968, The lower Paleozoic brachiopod and 

trilobite faunas of Anglesey: British Mus. (Nat. History) Bull., Geology, v. 16, no. 4, p. 125-199. 

Bergstrom, S. M., and Sweet, W. C., 1966, Conodonts from 

the Lexington Limestone (Middle Ordovician) of Kentucky, and its lateral equivalents in Ohio and Indiana: 

Bulls. Am. Paleontology v. 50, no. 229, p. 269-441. 

Black, D. F. B., Cressman, E. R., and Mac·Quown, W. C., Jr., 

1965, The Lexington Limestone (Middle Ordovician) of 

central Kentucky: U.S. Geol. Survey Bull. 1224-C., p. 

C1-C29. 

Bolton, T. E., 1971, Geological map and notes on the Ordovician and Silurian litho- and biostratigraphy, Anticosti 

Island, Quebec: Canada Geol. Survey Paper 71-19, 44 

p., 12 pis. 

Caster, K. E., Dalve, E. A., and Pope, J. K., 1961, Elementary guide to the fossils and strata of the Ordovician 

in the vicinity of Cincinnati, Ohio: Cincinnati Mus. Nat. 

History, 47 p., 8 pis. 

Cooper, G. A., 1956, Chazyan and related brachiopods: 

Smithsonian Misc. Colin., v. 127, Pts. 1 and 2, 1,245 p. 

Cumings, E. R., 1903, The morphogenesis of Platystrophia 

-A study of the evolution of a Paleozoic brachiopod: 

Am. Jour. Sci., 4th ser., v. 15, p. 1-48. 

Foerste, A. F., 1903, The Richmond group along the western 

side of the Cinc·innati anticline in Indiana and Kentucky: Am. Geologist, v. 31, p. 333-361, pis. 20-22. 

---1909a, Preliminary notes on Cincinnatian fossils: 

Denison Univ. Sci. Lab. Bull., v. 14, p. 208-231, pl. 7. 

---1909b, Preliminary notes on Cincinnatian and Lexington fossils: Denison Univ. Sci. Lab. Bull., v. 14, p. 

289-333, pis. 7-11. 

---1910, Preliminary notes on Cincinnati and Lexington 

fossils in Ohio, Indiana, Kentucky, and Tennessee: Denison. Univ. Sci. Lab Bull., v. 16, p. 17-99, pls. 1-6. 

Howe, H. J., 1966, Orthacea from the Montoya Group (Ordovician) of Trans-Pecos Texas: Jour. Paleontology, v. 

40, no. 2, p. 241-257. 

---1973, Stratigraphic significance of brachiopods from 

"Arnheim" and Fernvale Formations (Upper Ordovician) of Tennessee: Geol. Soc. America Abs. with Programs v. 5, no. 5, p. 406. 

James, U. P., 1881, Fossils of the Lower Silurian formation, 

Ohio, Indiana, and Kentucky: Paleontologist, no. 5, p. 

33-44. 

Ludvigsen, Rolf, 1975, Ordovician formations and faunas, 

Southern Mackenzie Mounta.Jins: Canadian Jour. Earth 

Sci., v. 12, no. 4, p. 663-697. 

Macgregor, A. R., 1961, Upper Llandeilo brachiopods from 

the Berwyn Hills, North Wales: Palaeontology, v. 4, 

p. 177-209. 

Macomber, R. W., 1970, Articulate brachiopods from the 

Upper Bighorn Formation (Late Ordovician) of Wyoming: Jour. Paleontology, v. 44, no. 3, p. 416-450, pis. 

75-80. 

---1972, Simultaneous occurrence of Late Ordovician 

brachiopod species in Britain and North America: Soc. 

Geol. et Mineral. Bretagne Bull., ser. C, v. 4, p. 17-24. 

McEwan, E. D., 1919, A study of the brachiopod genus 

Platystrophia: U.S. Natl. Mus. Proc., v. 56, p. 383-448, 

pis. 42-52. 

Meek, F. B., 1873, Description of invertebrate fossils of the 

Silurian and Devonian systems, in Report of the Geological Survey of Ohio: Ohio Geol. Survey, v. 1, pt. 2, 

p. 1-243, 23 pls. 

Neuman, R. B., 1963, Caradocian (Middle Ordovician) fossiliferous rocks near Ashland, Maine: U.S. Geol. Survey Prof. Paper 475-B, p. Bl17-B119. 

---1964, Fossils in Ordovician tuffs, northeastern Maine 

with a section on Trilobita, by H. B. Whittington: U.S. 

Geol. Survey Bull. 1181-E, 38 p., 7 pls. 

---1968, Paleogeographic implications of Ordovician 

shelly fossils in the Magog Belt of the Northern Appalachian region, in Zen, E-An, White, W. S., Hadley, J. B., 

and Thompson, J. B., Jr., eds., Studies of Appalachian 

geology, northern and maritime: New York, Interscience, 

Publishers, p. 35-48. 

Ross, R. J., Jr., 1957, Ordovician fossils from wells in the 

Williston Basin, eastern Montana; U.S. Geol. Survey 

Bull. 1021-M. p. 439-510, pls. 37-43. 

---1959, Brachiopod fauna of Saturday Mountain Formation, southern Lemhi Range, Idaho: U.S. Geol. Survey Prof. Paper 294-L, p. 441-461, pis. 54-56. 

---1975, Ordovician sedimentation in the western U.S.A., 

in Bassett, M. G., ed. The Ordovician System: Paleont. 

Assoc. Symposium, Birmingham, England, 1974, Proc: 

p. 73-105. 

Ross, R. J., Jr., and Ingham, J. Keith, 1970, Distribution of 

the Toquima-Table Head (Middle Ordovician Whiterock) faunal realm in the northern hemisphere: Geol. 

Soc. America Bull., v. 81, no. 2, p. 393-408. 

Schopf, T. J. M., 1966, Conodonts of the Trenton Group 

(Ordovician) in New York, southern Ontario, and Quebec: New York State Mus. and Sci. Service Bull. 405, 

105 p. 

Shaler, N. S., 1876, On the fossil brachiopods of the Ohio 

Valley: Kentucky Geol. Survey Mem. 1, pt. 3, 44 p. 

Sheehan, P. M., 1973, The relation of Late Ordovician glaciation to the Ordovician-Silurian changeover in North 

American brachiopod faunas: Lethaia, v. 6, p. 147-154. 

Sweet, W. C., and Bergstrom, S. M., 1971, The American 

Upper Ordovician Standard, XIII-A revised timestratigraphic classification of North American Upper 

Middle and Upper Ordovician rocks: Geol. Soc. America 

Bull., v. 82, p. 613-628. 

Sweet, W. C., Ethington, R. L., and Barnes, C. R., 1970, 

North .American Middle and Upper Ordovician conodont 

faunas, in Sweet, W. C., and Bergstrtsm, S. M., Symposium on conodont biostratigraphy: Geol. Soc. America 

Mem. 127, p. 163-194. 

Twenhofel, W. H., 1928, Geology of Anticosti Island: Canada 

Geol. Survey Mem. 154, 351 p., 60 pl. 

Wang, Y., 1949, Maquoketa brachiopoda of Iowa: Geol. Soc. 

America Mem. 42, 55 p., 12 pis. 

Weiss, M. P., 1961, The American Upper Ordovician standard V. A critical appraisal of the classification of the 

typical Cincinnatian beds: Geol. Soc. America Bull., v. 

72, p. 645-648. 

Whittington, H. B., and Williams, A., 1955, The· fauna of the 

Derfel limestone of the Arenig District, North Wales: 

Royal Soc. London Philos. Trans., ser. B, v. 238, no. 

658, p. 397-430. 

Williams, Alwyn, 1962. The Barr and Lower Ardmillan 

Series (Caradoc) of the Girvan District, Southwest 

Ayrshire, with descriptions of the brachiopoda: Geol. 

Soc. London Mem. 3, 267 p., 35 pl. 
B20 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

---1963, The Caradocian brachiopod faunas of the Bala 

District, Merionethshire: British Mus. (Nat. History) 

Bull., Geology, v. 8, no. 7, 471 p., 16 pis. 

---1969, Ordovician faunal provinces with reference to 

brachiopod distribution, in Wood, Alan, ed., The PreCambrian and lower Palaeozoic rocks of Wales: Cardiff, 

Univ. Wales Press, p. 117-154. 

---1973, Distribution of brachiopod assemblages in relation to Ordovician palaeogeography, in Organisms and 

continents through time: Systematics Assoc. Pub. no. 9, 

p. 241-269. . 

---1974, Ordovician brachiopoda from the Shelve District, 

Shropshire: British Mus. (Nat. History) Bull., Geology, 

Supp. II, p. 1-163, 28 pis. 

Williams, Alwyn, and others, 1965, in Moore, R. C., ed. 

Treatise on Invertebrate Paleontology, pt. H, Brachiopoda, 

2 v.: New York and Lawrence, Kans., Geol. Soc. America 

and Univ. Kansas Press, 927 p. 
Plates 1-6 are of species occurring in the Ordovician rocks of Kentucky and deposited in the collections of the United States National Museum. Plate 7 is primarily 

a selection of specimens of the species studied by McEwan (1919) and are presented 

for general comparison with the ones from Kentucky. Several of the specimens on 

plate 7, however, are from the Ordovician Kentucky collections of the U.S.G.S. 

PLATES 1-7 

Contact photographs of the plates in this ._report are available, at cost from the U.S. 

Geological Survey Library, Federal Center, Denver, Colorado 80225 
PLATE 1 

[All figures X 1.1. Figures 1-21 are from USGS CQllection 4•556-CO] 

FIGURES 1-7. Platystrophia ponderosa Foerste (p. B16). 

Figures 1-7 are a growth series showing the brachial exteriors 

1. Figured specimen USNM 189449. 

2. Figured specimen USNM 189450. 

3. Figured specimen USNM 189451. 

4. Figured specimen USNM 189452. 

5. Figured specimen USNM 189453. 

6. Figured specimen USNM 189454. 

7. Figured .specimen USNM 189455. 

8-14. Platystropkia ponderosa Foerste (p. B16). 

Figures 8-14 are a growth series showing the pedicle exteriors 

8. Figured specime-n USNM 189449. 

9. Figured specimen USNM 189450. 

10. Figured specimen USNM 189451. 

11. Figured specimen USNM 189452. 

12. Figured specimen USNM 189453. 

13. Figured specimen USNM 189454. 

14. Figured specimen USNM 189455. 

15-21. Platystrophia p.onderosa Foerste (p. B16). 

Figures 15-21 are a growth serie.s showing the posterior view 

15. Figured specimen USNM 189449. 

16. Figured specimen USNM 189450. 

17. Figured specimen USNM 189451. 

18. Figured specimen USNM 189452. 

19. Figured specimen USNM 189453. 

20. Figured specimen USNM 189454. 

21. Figured specimen USNM 189455. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-B PLATE 1 

15 

8 

2 9 

3 10 

17 

18 

4 

11 

5 

6 

7 14 

SPECIMENS OF PLATYSTROPHIA PONDEROSA 
PLATE 2 

[Figures 1-14 and 22-27 are from USGS collection 4556-CO. Figures 15-17 and 19 are from USGS collection 7834-CO] 

FIGURES 1-7. Platystrophia ponderosa Foerste (p. B16). 

Figures 1-7 are a growth series showing the lateral views (X 1.1). 

1. Figured specimen USNM 189449. 

2. Figured specimen USNM 189450. 

3. Figured specimen USNM 189451. 

4. Figured specimen USNM 189452. 

5. Figured specimen USNM 189453. 

6. Figured specimen USNM 189454. 

7. Figured specimen USNM 189455. 

8-14. Platystrophia ponderosa Foerste (p. B16). 

Figures 8-14 are a growth series showing the anterior views (X 1.1). 

8. Figured spedmen USNM 189449. 

9. Figured specimen USNM 189450. 

10. Figured specimen USNM 189451. 

11. Figured specimen USNM 189452. 

12. Figured specimen USNM 189453. 

13. Figured specimen USNM 189454. 

14. Figured specimen USNM 189455. 

15. Platystrophia ponderosa Foerste (p. B16). 

Enlarged view (X 8) of cardinalia showing the brachiophore bases elevated above the floor of the valve 

and positioned on a ridge to form a cruralium like structure. Specimen tilted. Figured specimen 

USNM 189456. 

16. Platystrophia ponderosa Foerste (p. B16). 

Figured specimen U SNM 189457; (X 8). Enlarged view of cardinalia showing a slight elevation of the 

brachiophore bases on a poorly defined ridge. Specimen tilted. 

17-19. Platystrophia ponderosa Foerste (p. B16). 

Specimens showing the various appearances of the cardinalia in which the bases of the brachiophores 

are elevated on a ridge to fo·rm a cruralium-like structure. All specimens are tilted (X 1.1). 

17. Figured specimen USNM 189458. 

18. Figured specimen USNM 189459; USGS colin. 6411-CO. 

19. Figured specimen USNM 189460. 

20, 21. Platystrophia ponderosa Foerste (p. B16). 

Small valves showing the appearance of the early stages of the formation of the cruralium-like structure. In specimen 20 the bases of brachiophores extend to the floor of the valve and apparently a 

central ridge is not formed. In specimen 21 the central ridge is present and the brachiophore· bases 

are tilted toward it. Both specimens (X 3.5). 

20. Figure.d specimen USNM 189461; USGS colln. 4908-CO. 

21. Figured specimen USNM 189462; USGS colln. 4908-CO. 

22-24. Platystrophia ponderosa Foerste (p. B16). 

View of pedicle interior of three valves of different size and shell thickness. Specimen 22 has the thickest 

shell and, therefore, the poorest delineation of pli ~a tions in the posterior part. Specimen 24 is the 

smallest and thinnest and the plications are refl~cted on the inside to a greater degree than in specimen 22. All figures X 1.1. 

22. Figured specimen USNM 189463. 

23. Figured specimen USNM 189464. 

24. Figured specimen USNM 189536. 

25. Platystrophia ponderosa Foerste (p. B16). 

View of brachial exterior of a specimen in which the cardinal extremities are distinctly different. The 

right cardinal extremity is right angled; the left extremity is evenly rounded. Figured specimen 

USNM 189465. (X 1.1). 

26, 27. Platystrophia ponderosa Foerste (p. B16). 

View of brachial interior showing muscle field. Spe"'imen in figure 26 not tilted; photograph taken normal to line of commissure. Specimen in figure 27 is one of largest; tilted to show the posterior scars 

better. Both figures X 1.1. 

26. Figured specimen USNM 189466. 

27. Figured specimen USNM 189467. 
GEOLOG ICAL SURVEY PROFESSIONAL PAPER 1066- B PLATE 2 

2 

3 10 

4 

•. ' 

5 12 20 

18 19 

13 

22 

7 14 

25 24 

26 27 

SPECIMENS OF PLATYSTROPHIA PONDEROSA 
/1 

PLATE 3 

[All figures X 1.1. All figured specimens are from USGS collection 7834-CO] 

FIGURES 1-9. Platyst'rophia annieana Foerste (p. B12). 

Growth series showing brachial exteriors. 

1. Figured specimen USNM 189468. 

2. Figured specimen USNM 189469. 

3. Figured specimen USNM 189470. 

4. Figured specimen USNM 189471. 

5. Figured specimen USNM 189472. 

6. Figured specimen USNM 189473. 

7. Figured specimen USNM 189474. 

8. Figured specimen USNM 189475. 

9. Figured specimen USNM 189476. 

10-18. Platystrophia annieana Foerste (p. B12). 

Growth series showing pedicle exteriors. 

10. Figured specimen USNM 189468. 

11. Figured specimen USNM 189469. 

12. Figured specimen USNM 189470. 

13. Figured specimen USNM 189471. 

14. Figured specimen USNM 189472. 

15. Figured specimen USNM 189473. 

16. Figured specimen·:USNM 189474. 

17. Figured specimen USNM 189475. 

18. Figured specimen USNM 189476. 

19-27. Platystrophia annieana Foerste (p. B12). 

Growth series showing posterior views. 

19. Figured specimen USNM 189468. 

20. Figured specimen USNM 189469. 

21. Figured specimen USNM 189470. 

22. Figured specimen USNM 189471. 

23. Figured specimen USNM 189472. 

24. Figured specimen USNM 189473. 

25. Figured specimen USNM 189474. 

26. Figured specimen USNM 189475. 

27. Figured specimen USNM 189476. 

28-36. Platystrophia annieana Foerste (p. B12). 

Growth series showing the anterior views. 

28. Figured specimen USNM 189468. 

29. Figured specimen USNM 189469. 

30. Figured specimen USNM 189470. 

31. Figured specimen USNM 189471. 

32. Figured specimen USNM 189472. 

33. Figured specimen USNM 189473. 

34. Figured· specimen USNM 189474. 

35. Figured specimen USNM 189475. 

36. Figured specimen USNM 189476. 

37-45. Platystrophia annieana Foerste (p. B12). 

Growth series showing the lateral views. 

37. Figured specimen USNM 189468. 

38. Figured specimen USNM 189469. 

39. Figured specimen USNM 189470. 

40. Figured specimen USNM 189471. 

41. Figured specimen USNM 189472. 

42. Figured specimen USNM 189473. 

43. Figured specimen USNM 189474. 

44. Figured specimen USNM 189475. 

45. Figured specimen USNM 189476. 
GEOLOGJCAL SURVEY PROFESSIONAL PAPER 1066-B PLATE 3 

37 

2 11 29 38 

1t~ ~. 3 J" 12 21 30 39 

·1ff4 ~~ 13 31 40 

5 14 41 

15 33 42 

7 16 43 

17 35 

18 27 36 45 

SPECIMENS OF PLATYSTROPHIA ANNIEANA 
PLATE 4 

[All figures X 1.1. Figures 1-5 are from USGS collection 7834-CO. Figures 6-10, 15· are from USGS collection 6140-CO. Figures 11-14, 17 are from 

USGS collection number 6139-CO] 

FIGURES 1, 2. Platystrophia annieana Foerste (p. B12). 

Brachial interior. Figure 1 taken normal to line of commissure. Figure 2 tilted to .show faint posterior adductor scars. 

1. Figured specimen USNM 189477. 

2. Figured specimen USNM 189477. 

3. Platystrophia annieana Foerste (p. B12). 

View of brachial interior showing nature of muscle field. Specimen tilted. Figured specimen USNM 

189478. 

4. Platystrophia annieana Foerste (p. B12). 

View of pedicle interior. Figure is normal to line of commissure. 

Figured specimen USNM 189479. 

5. Platystrophia annieana Foerste (p. B12). 

View of pedicle interior of specimen with rounded cardinal extremities. This specimen has a distinctly 

different outline than the normal P. annieana with the elongated hinge line. Figured specimen USNM 

189480. 

6-10. Platystrophia annieana Foerste (p. B12). 

Brachial exterior, pedicle exterior, posterior, anterior, and lateral views. Figured specimen USNM 

189481. 

11. Platystrophia annieana Foerste (p. B12). 

View of pedicle interior of an intermediate-size spec-imen. Figure normal to line of commissure. 

Figured specimen USNM 189482. 

12. Platystrophia annieana, Foerste (p. B12). 

View of pedicle interior of a small specimen. Figure normal to line of commissure. Figured specimen 

USNM 189483. 

13. Platystrophia annieana Foerste (p. B12). 

View of brachial interior; specimen tilted to show posterior adductor scars. Figured specimen USNM 

189484. 

14. Platystrophia annieana Foerste (p. B12). 

View of brachial interior; specimen tilted to show posterior adductor scars. Figured specimen USNM 

189485. 

15. Platystrophia annieana Foerste (p. B12). 

View of brachial exterior. Figured specimen USNM 189486. 

16. Platystrophia ponderosa Foerste (p. B12). 

View of pedicle interior of a short-hinge line form. Figured specimen USNM 189487; USGS colin. 6411-

CO. 

17. Platystrophia cf. P. annieana Foerste (p. B12). 

View of pedicle interior. Figure normal to line of commissure. 

Figured specimen USNM 189488. 

18-20. Platystrophia ponderosa Foerste (p. B16). 

Brachial interior of three immature specimens. All tilted to show muscle scars. 

18. Figured specimen USNM 189489; USGS colin. 4556-CO. 

19. Figured specimen USNM 189490; USGS colin. 4556-CO. 

20. Figured specimen USNM 189491; USGS colin. 4210-CO. 

21-23. Platustrophia ponderosa Foerste (p. B16). 

Pedicle interior of three small specimens. All figures taken normal to line of commissure. 

21. Figured specimen USNM 189492; USGS colin. 6411-CO. 

22. Figured specimen USNM 189493; USGS colin. 4556-CO. 

23. Figured specimen USNM 189494; USGS colin. 4556-CO. 

24-28. Platystrophia ponderosa Foerste (p. B16). 

Normal appearance of brachial and pedicle valves preserved as fragments. Many of the collections contain fragmented specimens still recognizable as P. ponderosa. This is due to the thick shell material 

around the beak region. 

24. Figured specimen USNM 189495; USGS colin. 6409-CO. 

25. Figured specimen USNM 189496; USGS colin. 6412-CO. 

26. Figured specimen USNM 189497; USGS colin. 6410-CO. 

27. Figured specimen USNM 189498; USGS colin. 6410-CO. 

28. Figured specimen USNM 189499; USGS colin. 6412-CO. 
29. Platystrophia ponde'rosa Foerste (p. B16). 

Pedicle exterior of a specimen with broad plications. Compare this specimen to figure 30 in which the 

plications' are more numerous and closer together. Both specimens are from the same suite. Figured 

specimen USNM 189500; USGS c<>lin. 6416-CO. 

30. Platystrophia ponderosa Foerste (p. B16). 

Pedicle exterior showing a typical plication pattern. Figured specimen USNM 189501; USGS colin. 

6416-CO. 

31. Platystrophia ponderosa Foerste (p. B16). 

Pedicle exterior of a specimen in which a "scar" appears across several of the plications suggesting 

that some damage occurred which was later repaired by the individual. Figured specimen USNM 

189502; USGS colin. 6416-CO. 

32. Platystrophia ponderosa Foerste (p. B16). 

Brachial exterior of a spec.jmen having a peculiar plication pattern. Note that the three plications in 

the region of the cardinal extremity have a distinct "cleft" running from the hinge line to the 

lateral margin. Figured specimen USNM 189503; USGS colln. 6416-CO. 

33. Platystrophia ponderosa Foerste (p. B16). 

Brachial exterior of a specimen with seven plications on the fold. Figured specimen USNM 189504; 

USGS colln. 6416-CO. 
GEOLOGICAL SU RVEY PROFESSIONAL PAPER 1066-B PLATE 4 

2 3 4 

5 6 7 

9 

15 17 

10 

24 

21 

18 

19 27 

22 

20 

23 

30 

SPECIMENS OF PLATYSTROPHIA ANNIEANA AND PLATYSTROPHIA PONDEROSA 
PLATE 5 

[All figures X 1.2. Figures 1-30 are from USGS collection 7353-CO. Pigures 31-36 are from USGS collection 7812-CO] 

FIGURES 1-5. Platystrophia colbiensis Foerste (p. B9). 

Brachial views of a growth se-ries. 

1. Figured specimen USNM 189505. 

2. Figured specimen USNM 189506. 

3. Figured specimen USNM 189507. 

4. Figured spec-imen USNM 189508. 

5. Figured specimen USNM 189509. 

6-10. Platystrophia colbiensis Foerste (p. B9). 

Pedicle views of a growth series. 

6. Figured specimen USNM 189505. 

7. Figured specimen USNM 189506. 

8. Figured specimen USNM 189507. 

9. Figured specimen USNM 189508. 

10. Figured .specimen USNM 189509. 

11-15. Platystrophia colbiensis Foerste (p. B9). 

Anterior views of a growth series. 

11. Figured specimen USNM 189505. 

12. Figured specimen USNM 189506. 

13. Figured specimen USNM 189507. 

14. Figured specimen USNM 189508. 

15. Figured specimen USNM 189509. 

16-20. Platystrophia colbiensis Foerste (p. B9). 

Posterior views of a growth series. 

16. Figured specimen USNM 189505. 

17. Figured specimen USNM 189506. 

18. Figured specimen USNM 189507. 

19. Figured specimen USNM 189508. 

20. Figured specimen USNM 189509. 

21-25. Platystrophia colbiensis Foerste (p. B9). 

Lateral views of a growth series. 

21. Figured specimen USNM 189505. 

22. Figured specimen USNM 189506. 

23. Figured specimen USNM 189507. 

24. Figured specimen USNM 189508. 

25. Figuved specimen USNM 189509. 

26-30. Platystrophia colbiensis Foerste (p. B9). 

Brachial interiors of several valves of different sizes. All tilted. slightly to the posterior. 

26. Figured specimen USNM 189510. 

27. Figured specimen USNM 189511. 

28. Figured specimen USNM 189512. 

29. Figured specimen USNM 189513. 

30. Figured specimen USNM 189514 

31. Platystrophia colbiensis Foerste (p. B9). 

Brachial exterior. Figured specimen USNM 189515. 

32, 33. Platystrophia colbiensis Foerste (p. B9). 

Pedicle interiors. 

32. Figured specimen USNM 189516. 

33. Figured specimen USNM 189517. 

34-36. Platystrophia colbiensis Foerste (p. B9). 

Brachial interiors. Figure 34 is normal to line of commissure; figures 35 and 36 are tilted to the 

posterior. 

34. Figured specimen USNM 189518. 

35. Figured specimen USNM 189518. 

36. Figured specimen USNM 189519. 
g7, Platystrophia annieana Foerste (p. B12). 

Brachial exterior of a specimen with two large plications on the fold and more numerous smaller 

plications on the flanks. This is an atypical specimen of P. annieana. Figured specimen USNM 

189520; USGS colln. 6139-CO. 

38. Platystrophia annieana Foerste (p. B12). 

Brachial exterior of a specimen with six plications on the. fold; plic·ations on flanks are same size. 

Compare this figure with figure 37; both specimens are from the same suite. Figured specimen 

USNM 189521; USGS colin. 6139-CO. 

39, 40, 50. Platyst'rophia cypha (James) (p. B15). 

Pedicle exterior, brachial exterior, anterior views. Figured specimen USNM 189522; USGS colln. 4060-

CO. 

41. Platyst?·ophia cf. P. laticosta (Meek) (p. B14). 

Pedicle exterior of a small specimen with one plication in the sulcus like that found in specimens 

referred by some to P. unicostata. Figured specimen USNM 189523; USGS colln. 6418-CO. 

42. Platyst?·oph·ia cf. P. laticosta (Meek) (p. B14). 

Brachial exterior of a medium-sized specimen having two large inner plications on the fold and two 

smaller marginal fold plications. Figur.ed specimen USNM 189524; USGS colln. 6418-CO. 

43. Platyst?·oph-ia cypha (James) (p. B15). 

Pedicle exterior of a small .specimen showing a greater than normal number of plications along the 

flanks. Compare this with figure 44, which is a specimen of about the same size but with a typical 

number of flank plications for P. cypha. Figured specimen USNM 189525; USGS colln. 4060-CO. 

44, 52. Platystroph·ia cypha (James) (p. B15). 

Small specimen. Pedicle exterior, anterior views. Figured specimen USNM 189526; USGS colin. 4060-

CO. 

45-49. Platystrophia laticosta (Meek) (p. B14). 

Pedicle exterior, brachial exterior, posterior, anterior, lateral views. Figured specimen USNM 189527. 

USGS colln. 4067-CO. 

51, 53. Platyst?·ophia cf. P. laticosta (Meek) (p. B14). 

Anterior view and brachial exterior of a slightly crushed specimen. Figured specimen USNM 189528; 

USGS colln. 4060-CO. 

54. Platystrophia elegantula McEwan (p. BlO). 

Brachial interior. Figure normal to line of commissure. Figured specimen USNM 189529; USGS 

colln. 5015-CO. 

55. Platyst?·ophia elegantula McEwan (p. BlO). 

Pedicle interior. Figure normal to line of commissure. Figured specimen USNM 189530; USGS 

colln. 5015-CO. 

56-60. Platystrophia elegantula McEwan (p. BlO). 

Brachial exterior, pedicle exterior, anteTior, posterior, lateral views. Figured specimen USNM 189531; 

USGS colln. D1204-CO. 

61-65. Platystrophia elegantula McEwan ( p. BlO). 

Brachial exterior, pedicle exterior, anterior, posterior, lateral views. This specimen is from a different stratigraphic section than the specimen figured in 56-60. Figured specimen USNM 189532. 

66, 67. Platystrophia. aff. P. annieana Foerste (p. B12). 

Brachial exterior, posterior views. Figured specimen USNM 189533; USGS colln. 7066-CO. 

68, 69. Platyst1·ophia cf. P. colbiensis Foerste ( p. B9). 

Brachial exterior, posterior views. Figured specimen USNM 189534; USGS colln. 7079-CO. 

70, 71. Platystrophia elegantula McEwan (p. BlO). 

Brachial exterior, posterior views. Figured specimen USNM 189535; USGS colln. 4982-CO. 
GEOLOGICAL SURVEY 

5 10 

26 27 

37 

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16 

17 

18 

19 

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59 

64 

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68 

22 

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23 

25 

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30 

69 

PROFESSIONAL PAPER IO<i6-B PLATE 5 

31 

45 

46 

33 

48 

34 

35 49 

44 

51 

52 

65 

53 

70 71 

SPECIMENS OF PLATYSTROPHIA COLBIENSIS, PLATYSTROPHIA ANNIEANA, PLATYSTROPHIA CYPHA, 

PLATYSTROPHIA LATICOSTA, PLATYSTROPHIA CF. P. LATICOSTA, PLATYSTROPHIA ELEGANTULA, 

PLATYSTROPHIA CF. P . ANNIEANA, AND PLATYSTROPHIA CF. P. COLBIENSIS 
PLATE 6 

[Ali figures X 1.1 unless otherwise noted] 

FIGURES 1-5. Platystrophia laticosta (Meek) (p. B14). 

Brachial exterior, pedicle exterior, posterior, anterior, and lateral views. Figured specimen USNM 

189537; USGS colin. D1363-CO. 

6, 7. Platystrophia laticosta (Meek) (p. B14). 

Brachial exterior. Figured specimen USNM 189538. USGS colin. 6284-CO. 

8-10. Platystrophia laticosta (Meek) (p. B14). 

Brachial exterior, pedicle exterior, anterior view. Figured specimen USNM 189539; USGS colin. D1363-

CO. 

11-13. Platystrophia laticosta (Meek) (p. B14). 

Brachial exterior, pedicle exterior, anterior view of a small specimen. Figured specimen USNM 189540; 

USGS colin. D1363-CO. 

14-18. Platystrophia cypha (James) (p. B15). 

Brachial exterior, pedicle exterior, posterior, lateral, and anterior views. Figured specimen USNM 

189541. USGS colin. D1250-CO. 

19-21. Platystrophia laticosta (Meek) (p. B14). 

Brachial exterior, pedicle exterior, anterior view. This specimen is characterized by broad, low-angle 

plications and occurs in the same suite of specimens as figures 6, 7, 25, 26, 27, and 28. Figured 

specimen USNM 189542; USGS colin. 6284-CO. 

22-24. Platystrophia laticosta (Meek) (p. B14). 

Brachial exterior, pedicle exterior, anterior view. Figured specimen USNM 189543; USGS colin. 4545-

CO. 

25-28. Platystrophia laticosta (Meek) (p. B14). 

Brachial exterior, pedicle exterior, anterior, and lateral views. Figured specimen USNM 189544; USGS 

colin. 6284-CO. 

29, 30. Platystrophia cypha (James) (p. B15). 

View of brachial interior showing muscle scars; specimen tilted. View of brachial interior; photograph taken normal to plane of commissure. Figured spec-imen USNM 189545; USGS colin. 4067-CO. 

31. Platystrophia cypha (James) (p. B15). 

View of pedicle interior; photograph taken normal to plane of commissure. Figured specimen USNM 

189546; (X 1.) USGS colin. 4067-CO. 

32. Platystrophia cypha (James) (p. B15). 

Pedicle interior. Figured specimen USNM 189547; (X 1) USGS colin. 4067-CO. 

33-37. Platystrophia cf. P. foerstei McEwan (p. B18). 

Brachial exterior, pedicle exterior, posterior view, anterior view, and lateral view. Figured specimen 

USNM 189548; USGS colin. D1370-CO. 

38-41. Platystrophia cf. P. foerstei McEwan (p. B18). 

Brachial exterior, pedicle exterior, posterior view, lateral view. Figured specimen USNM 189549; USGS 

colin. D1370-CO. 

42-46. Platystrophia sp. (p. B18). 

Brachial exterior, pedicle exterior, posterior view, lateral view, and anterior view. Figured specimen 

USNM 189550; USGS colln. D1292-CO. 

47, 49. Platystrophia ponderosa Foerste (p. B16). 

Brachial interior; photograph taken normal to plane of commissure. Brachial interior; specimen tilted to 

show inward-sloping brachiophore bases and the formation of the cruralium-like structure. Figured 

specimen USNM 189551; USGS colin. 4195-CO. This specimen is a short-hinge-line form commonly 

designated P. ponderosa var. auburnensis Foerste. 

48. Platystrophia ponderosa Foerste (p. B16). 

Pedicle interior of a short-hinge-line form commonly referred to P. ponderosa var. auburnensis Foerste. 

Figured specimen USNM 189552; USGS colin. 4195-CO. 

50-54. Platystrophia acutilirata (Conrad) (p. Bll). 

Brachial exterior, pedicle exterior, posterior view, anterior view, and lateral view. Figured specimen 

USNM 189553; USGS colin. 5309-CO. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-B PLATE 6 

SPECIMENS OF PLATYSTROPHIA LATICOSTA, PLATYSTROPHIA CYPHA , PLATYSTROPHIA CF. P. 

FOERSTEI, PLATYSTROPHIA SP. , PLATYSTROPHIA PONDEROSA, AND PLATYSTROPHIA ACUTILIRATA 
FIGURES 

PLATE 7 

[All figures X 1.1 unless otherwise noted] 

1, 3. Platystrophia acutilirata (Conrad) (p. Bll). 

Brachial exterior, posterior view of a spec-imen studied by McEwan (1919) from the Whitewater 

Formation near Richmond, Ind. Figured specimen USNM 189554. 

2. Platystrophia acutilirata (Conrad) (p. Bll). 

Pedicle exterior of a specimen studied by McEwan (1919) from the Whitewater Formation near 

Richmond, Ind. Figured specimen USNM 189555. 

4-6. Platystrophia annieana Foerste (p. B12). 

Brachial exterior, anterior view, lateral view of a specimen studied by McEwan (1919) from the 

"Richmond Group" near Waynesville, Ohio. Figured specimen USNM 189556 (X 1.2). 

7, 8. Platystrophia annieana Foerste (p. B12). 

Lateral view, anterior view of a specimen studied by McEwan (1919) from the "Richmond Group" 

near Waynesville, Ohio. This specimen is not as thick as the one shown in figures 4-6. Figured 

specimen USNM 189557 (X 1.2). 

9-12. Platystrophia unicostata Cumings (p. B14). 

Pedicle exterior, anterior view, posterior view, lateral view of a specimen studied by McEwan (1919) 

from the "Maysville Group" 2.5 miles north of Lebanon, Ky. Figured specimen USNM 189558. 

13, 14. Platystrophia unicostata Cumings (p. B14). · 

Brachial exterior, anterior view of a specimen studied by McEwan (1919) from the "Maysville 

Group" near Madison, Ind. Figured specimen USNM 189559. Note the presence of only one plication in the sulcus. This is the single attribute that is supposed to distinguish this species from 

all others. 

15, 16. Platystrophia unicostata Cumings (p. B14). 

Brachial exterior, anterior view of a specimen studied by McEwan (1919) from the "Maysville 

Group" near Madison, Ind. Figured specimen USNM 189560. 

17-19. Platystrophia laticosta (Meek) (p. B14). 

Brachial exterior, anterior view, lateral view of a specimen studied by McEwan (1919) from the 

"Maysville Group" ("Bellevue Formation?") in Oldham County, Ky. Figured specimen USNM 

189561. 

20-21. Platystrophia laticosta (Meek) (p. B14). 

Anterior view, lateral view of a specimen studied by McEwan (1919) from the "Maysville Group" 

("Bellevue Formation?") in Oldham County, Ky. Figured specimen USNM 189562. 

22, 23, 27. Platystrophia cypha (James) (p. B15). 

Brachial view, lateral view, anterior view of a specimen studied by McEwan (1919) from the Arnheim Formation near Waynesville, Ohio. Figured specimen USNM 189563. 

24, 25. Platystrophia cypha (James) (p. B15). 

Brachial exterior, anterior view of a specimen studied by McEwan (1919) from the Arnheim Formation near Waynesville, Ohio. Figured specimen USNM 189564. 

26. Platystrophia cypha (James) (p. B15). 

Brachial exterior of a specimen studied by McEwan (1919) from the Arnheim Formation near 

Waynesville, Ohio. Figured specimen USNM 189565. 

28. Platystrophia cypha (James) (p. B15). 

Brachial exterior of a specimen studied by McEwan (1919) from the Arnheim Formation near 

Waynesville, Ohio. Figured specimen USNM 189566. 

29. Platystrophia cypha (James) (p. B15). 

Pedicle exterior of a specimen studied by McEwan (1919) from the "Arnheim" Formation 1 mile 

east of Seatonville, Ky. Figured specimen lJSNM 189567. 

30. Platystrophia clarksvillensis Foerste (p. B16). 

Brachial exterior of a specimen studied by McEwan (1919) from the Waynesville Shale near Oregonia, Ohio. Figured specimen USNM 189568. 

31. Platystrophia claTksvillensis Foerste (p. B16). 

Anterior view of a specimen studied by McEwan (1919) from the Waynesville Shale near Waynesville, Ohio. Figured specimen USNM 189569. 

32, 33. Platystrophia clarksvillensis Foerste (p. B16). 

Brachial exterior, anterior view of a specimen studied by McEwan (1919) from the Waynesville 

Shale near Waynesville, Ohio. Figured specimen USNM 189570. 
34, 35. Platystrophia cf. P. annieana Foerste (p. B14). 

Pedicle exterior, posterior :views. Figured specimen USNM 189571; USGS colin. 7066-CO. 

36, 38. Platystrophia colbiensis Foerste (p. B9). 

Brachial exterior, anterior views of rather large specimen of the species. Figured specimen USNM 

189572; USGS colin. 7319-CO. 

37. Platystrophia colbiensis Foerste (p. B9). 

Brachial exterior of a large specimen of this species occurring in the same suite as the specimen 

figured in 36 and 38. Compare these specimens with the figures of P. colbiensis studied by McEwan 

(1919) from the Catheys Limestone (Trentonian) of Tennessee. Figured specimen USNM 189573. 

USGS colin. 7319-CO. 

39. Platystrophia elegantula McEwan (p. B10). 

Posterior view of a specimen studied by McEwan (1919) from either the Bigby Limestone (Trentonian) of Tennessee or the Trenton Group at Ellisburg, N.Y. Figured specimen USNM 189574. 

40. Platystrophia colbiensis Foerste (p. B9). 

Pedicle exterior of a specimen studied by McEwan (1919) from the Catheys Limestone (Trentonian) 

in Nashville, Tenn. Figured specimen USNM 189575. 

41. Platystr-ophia colbiensis Foerste (p. B9). 

Anterior view of a specimen studied by McEwan (1919) from the Catheys Limestone (Trentonian) 

near Edgefield Junction, Tenn. Figured specimen USNM 189576. 
GEOLOGICAL SURVEY PROF ESSIONAL PAPER 1066-B PLATE 7 

2 

4 

6 

17 18 

21 

30' 

32 

41 

SPECIMENS OF PLATYSTROPHIA ACUTILIRATA, PLATYSTROPHIA ANNIEANA, PLATYSTROPHIA 

UNICOSTATA, PLATYSTROPHIA LATICOSTA, PLATYSTROPHIA CYPHA, PLATYSTROPHIA 

CLARKSVILLENSIS, PLATYSTROPHIA CF. P. ANNIEANA, PLATYSTROPHIA ELEGANTULA, 

AND PLATYSTROPHIA COLBIENSIS 
Middle and Late Ordovician Plectambonitacean, 

Rhynchonellacean, Syntrophiacean, 

Trimerellacean, and Atrypacean Brachiopods 

By HERBERT .J. HOvVE 

CONTR.IBUTIONS TO THE ORDOVICIAN PALEONTOLOG1' 

OF l(ENTUCK.Y AND NEARBY STATES 

GEOLOGICAL SURVEY P:ROFESSIONAL PAPER 1066--C 

Prepared in coojJeration with the 

Com.n1onwealth of [(entucky, 

University of [(entucky, 

[(entucky Geological Survey 

Descriptions and illustrations of 14 species· 

of Ordovician brachiopods 

UNITED STATES GOVERNlVIENT PRINTING OFFICE, WASHINGTON 1979 

CONTENTS 

l'age 

Abstract ----------------------------------------------------------------- C1 

Introduction ------------------------------------------------------------- 1 

Acknowledgments -------------------------------------------------------- 1 Systematic paleontology _ _ _ ____ _ _ __ _ __ _ _ _ _ _ _ _ _ _ _ __ _ _ _ _ _ _ _ _ _ _ __ _ _ _ _ _ _____ __ _ 1 

Superfamily Plectambonitacea _ _ _ __ __ ___ _ __ __ __ _ __ _ __ _ _ ___ _____ _ _ __ _ ___ 1 

Superfamily Rhynchonellacea ___________________________ ------------ __ 15 

Superfamily Syntrophiacea __________ ---------------------------------- 15 

Superfamily Trimerellacea ___ --· _ _ __ _ _ _ _ _ _ __ __ _ _ _ _ _ _ _ _ _ _____ _ _ _ ___ ___ _ _ 16 

Superfamily Atrypacea ----------------------------------------------- 17 

References cited _ _ _ __ _ _ __ _ _ __ _ _ _ _ _ __ _ __ __ _ __ _ _ _ __ _ _ ___ _ __ __ _ _ _ _ __ _ _ __ _ _ _ __ 17 

ILLUSTRATIONS 

PLATE 1. Sowet·byella. 

FIGURE 

2. Sowerbyella and Thaet·odonta. 

3. Rhynchotrema. 

4. Lepidocyclus? and Ot·thorhynchula. 

5. Orthorhynchula. 

6. Orthorhynchula. 

7. Orthorhynchula, E lliptoglossa?, Rostr-icellula, Zygospira?, 

Camerella, and Rhynchotrema. 

1. 

2. 

., 

0. 

4. 

5. 

6. 

7. 

8. 

9. 

10. 

11. 

12. 

13. 

14. 

Scatter diagram of length-width of Sowe·rbyella curdsvillensis and 

Thaerodonta clarksvillensis _______________________________ _ 

Scatter diagram of length-width of Sowet·byella sp. and Thaerodonta clarks1Jillensis _____________________________________ _ 

Sketches of variation in pedicle musculature of Rhynchotrema increbescens ----------------------------------------------- Scatter diagram of length-width of Rhynchotrema increbescens and 

R. wisconsinense ------------------------------------------

Scatter diagram of length-thickness of Rhynchott·ema inct·ebescens 

and R. wisconsinense -------------------------------------

Scatter diagram of width-fold width of Rhynchotrema increbescens 

and R. wiscons1~nense --------------------------------------

Scatter diagTam of thickness-height of fold of Rhynchotrema inct·ebescens and R. wisconsinense _____________________________ _ 

Variations in musculature of Orthorhynchula linneyi ------------

Scatter diagTam of length-width of Orthorhynchula linneyi and 0. 

sublinneyi ______________________________________________ _ 

Scatter diagram of length-thickness of Ot·thorhynchula linneyi and 

0. sublinneyi ____________________________________________ _ 

Scatter diagram of width-fold width of Orthorhynchula linneyi and 

0. sublinneyi ____________________________________________ _ 

Scatter diagram of thickness-height of fold of Orthorhynchula 

linneyi and 0. sublinneyi _________________________________ _ 

Variations in ventral musculature of Ortho1·hynchula sublinneyi __ 

Variations in dorsal musculature of Orthorhynchula sublinneyi __ 

Pag-1.' 

C2 

4 

4 

8 

8 

9 

9 

11 

12 

12 

13 

13 

14 

16 

III 
IV CONTENTS 

TABLES 

Pug•· 

TABLE 1. Measurements of length and width of species of Sowerbyella and 

Thaerodonta ----------------------------------------------- C5 

2. Number of costae (brachial valve) in species of Rhynchotrema ---- 7 

3. Number of costae (brachial valve) in species of Orthorhynchula -- 12 

SYSTEM OF MEASUREMENT UNITS 

The investigations underlying this series of reports were made over a period of 

years, and distances and stratigraphic measurements appear fairly uniformly in 

English units. Measurements of fossil specimens, on the other hand, follow the longstanding convention of appearing in metric units. Because of the dates of the investigations and the amount of resulting data, the English measurements have been retained. Conversions to metric units may be made by using the following conversion 

table. 

To convert 

English unit: 

Mile (mi) 

Foot (ft) 

To metric· unit: 

Kilometer (km) 

Meter (m) 

Multiply 

by: 

1.61 

.305 
CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

MIDDLE AND LATE ORDOVICIAN PLECTAMBONITACEAN., 

RHYNCHONELLACEAN., SYNTROPHIACEAN., TRIMERELLACEAN., 

AND ATRYPACEAN BRACHIOPODS 

By HERBERT J. HowE1 

ABSTRACT 

Middle and Upper Ordovician strata in Kentucky yielded 

a large silicified brachiopod fauna representing the superfamilies Plectambonitacea, Rhynchonellacea, Syntrophiacea, 

and Trimerellacea. Fourteen spedes from eight genera are 

described: Sowe·rbyella cttrdsvillensis ( Foerste), S. grierens·is 

Howe n. sp., Sowerbyella sp., S. rugosa (Meek), Thaerodonta 

cla?·ksvillensis (Foerste), Rhynchotrema dentatum (Hall), R. 

increbescens (Hall), Rost?·icellttla minuta Cooper, Lepidocycltts? capax (Conrad), Orthorhynchttla linneyi (James), 0. 

sttblinneyi Howe n. sp., Cam,e?·ella bella Fenton, C. sp. aff. C. 

immattt?'a Cooper, and Elliptoglossa? sp. An atrypid species, 

probably an aberrant Zygospira, is also described. 

INTRODUCTION 

The purpose of this paper is to describe the 

plectambonitacean, rhynchonellacean, syntrophiacean, and trimerellacean brachiopods from Middle 

and Upper Ordovician strata in Kentucky. The U.S. 

Geological Survey material at hand consists of more 

than 8,500 sp·ecimens representing 14 species and 8 

genera. 

All figured specimens have been deposited in the 

U.S. National Museum (USNM) in Washington, 

D.C. Photographed fossils were stained with india 

ink and then whitened with ammonium chloride. 

Statistics, tables, and scattergrams have been used 

in some sampl:es to show basic variations in diagnostic characters. In normally distributed samples, 

reduced major axes have been estimated from a 

method by Imbrie (1956). Measurements include 

length and width, thickness, height of fold (and 

corresponding depth of sulcus), and fold width. 

ACKNOWLEDGlVIENTS 

I am indebted to the U.S. Geological Survey for 

permission to ·study the Survey's large collection of 

1 Purdue University, Lafayette, Ind. 

Middle and Late Ordovician brachiopods from Kentucky; to G. Arthur Cooper for permission to examine pertinent specimens in the U.S. National 

Museum; and to Norman D. Newell for permission 

to examine Hall's type lot of Rhynchot?·ema increbescens, which is reposited in the American Museum 

of Natural History. I owe special thanks to John 

Pojeta of the U.S. Geological Survey for responding 

to numerous requests for assistance and information. 

SYSTEMATIC PALEONTOLOGY 

Superfamily PLECTAMBONITACEA Jones nom. trans!. 

Cooper and Williams .. Family SOWERBYELLIDAE Qpik 

Genus SOWERBYELLA Jones, 1928; emended Wang, 1949; Howe, 1972 

Sowerbyella curdsvillensis (Foerste) 1912 

Plate 1, figures 6-16 

Plecta?nbonites curdsvillensis Foerste, 1912; p. 122, pl. 10, 

figs. 15A, B. 

Plectambonites pttnctostriattts Mather, 1917; p. 38, pl. 1, figs. 

15-17. 

Sowerbyella punctostn'ata (Mather). Cooper, 1944, p. 335, pl. 

128, figs. 44-49. 

Sowerbyella cttrdsvillensis (Foerste). Cooper, 1956, p. 780, 

pl. 201A, figs. 1-13. 

Sowerbyella punctostriata (Mather). Cooper, 1956, p. 792, 

pl. 205C, figs. 9-25; pl. 206D, figs. 14, 15. 

Sowerbyella ctt'rdsvillensis (Foerste). Howe, 1972, p. 442, pl. 

1, fig. 9. 

Sowerbyella puncto8triata (Mather). Howe, 1972, p. 442, pl. 

1, fig. 12. 

Desc1·iption.-Shell large for the genus; width 

nearly twice the length; cardinal extremities acute 

to right-angular; anterior margin broadly rounded. 

Ornamentation unevenly costellate and faintly 

beaded; one to five finer costellae grouped between 

slightly larger ones. Region adjacent to posterior 

margin displaying weak oblique wrinkles in occasional specimens. 

Cl 
C2 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Pedicle valve moderat.ely convex in lateral profile; umbonal region gently inflated. Interior of 

pedicle valve finely papillose. Teeth small. Adjustordiductor muscle field wide, extending to about midlength; diductors strongly diverging in front of 

short median septum; paired adductor scars deeply 

incised into callus deposits of delthyrial floor. 

Brachial valve concave in lateral profile. Inner 

surface marked by fine papillose elevations. Adductor muscle field large, ·subcircular in outline, 

reaching beyond the middle of the valve; inner scars 

bordered by moderately elevated septa; occasional 

specimens displaying low median septum. Brachiophores large, strongly divergent, and ending in 

points; cardinal process strongly elevated ventrally. 

Interarea short, anacline. 

RemaTks.-S. curdsvillensis suggests the genus 

Thaerodonta in its large size and the deeply incised 

adductor scars on the delthyrial floor. However, it 

lacks the diagnostic dorsal lateral septa, accessory 

teeth, and hinge denticulations of that genus. Papillose ornamentation occasionally extends into the 

cardinal area of the brachial valve, but the papillae 

do not correspond with the dorsal denticles of 

Thaerodonta nor do any of the many specimens at 

hand show any fossettes along the ventral hinge. 

Comparison.-S. curdsvillensis is most like a form 

that has been widely recognized in the lower part 

of the Trenton Group of New York and Ontario and 

in the Midwest as S. punctostriata (Mather). According to Cooper (1956), S. curdsvillensis and S. 

punctost1·iata are sufficiently similar to be possible 

ecads of a single species, but he felt that larger collections than those available to him would be necessary to demonstrate this. He distinguished the two 

forms on the basis of S. punctostriata exhibiting 

(1) lesser concavity and generally thinner valves, 

(2) a shaUower brachial valve, (3) greater development of oblique wrinkling, ( 4) fairly late development of a thickened subperipheral rim, ( 5) lesser 

thickening of all internal features, and (6) a greater 

tendency to auriculate cardinal extremities. Mather 

(1917) emphasized the subperipheral rim and thickening of interior features in S. curdsvillensis as the 

major points of difference. Study of large suites of 

S. curdsvillensis in the USGS collections from Kentucky revealed wide variations in the amount of 

thickening of internal structures, the prominence 

of the subperipheral rim, shell thickness, acuteness 

of the cardinal extremities, and the concavity of the 

brachial valve. In view of these variations, the oblique wrinkling in S. punctostriata appears to be 

the only basis for distinguishing the two forms. 

1 Both show beaded costellae. 

I 

S. curdsvillenis is similar to Thaerodonta clar-ksvillensis in size and in growth pattern of length to 

width (fig. 1), but that form has accessory denticulations along the hinge, accessory teeth, and 

lateral septa dividing the dorsal muscle field. 

Distribution and material.-This species is one of 

the most common brachiopods in the Curdsville 

Limestone Member of the Lexington Limestone. Ap1 proximately 1,400 disarticulated valves, many of 

1 which are partially broken, were recovered from the 

j following USGS localities: 4122-CO, 4123-CO, 

I 4124-CO, 4125-CO, 4213-CO, 4940-CO, 5022-CO, 

5069-CO, 5084-CO, 6131~CO, and 6135-CO. 

Dimension.<;.-Measurements and growth patterns 

of length to width are given in figure 1 for comparison with respesentatives of Thaerodonta clarksvillensis. 

• 

0 

0 

15 

• 

• 

•• 

0 0 

0 

• 

0 

• • 

• 0 ~00 

oo • •o• oo 

0 

0 • 0 

oo• • 

• • 0 

0 • 

, .. • 0 

• 

10 

LENGTH' 

• 

• 

15 

FIGURE 1.-Scatter diagram of length-width in millimeters (brachial valve) of Sowerbyella curdsvillensis 

( Foerste) (open circles) from the Curdsville Limestone Member of the Lexington Limestone, USGS 

Iocs. 5101-CO and 7785-CO; and Thaerodonta clarksvillensis ( Foerste) (solid circles) from Richmond ian 

beds at Waynesville, Ohio, USNM 40460. 
MIDDLE AND LATE ORDOVICIAN BRACHIOPODS C3 

Sowerbyella grierensis Howe, n. sp. 

Plate 1, figures 1-5 

Description.-Shell of medium s,ize for the genus; 

adult ~specimens averaging about 12 mm in width; 

width nearly twice the length. Cardinal extremities 

acute to right angular; lateral margins sloping inward ; anterior margin broadly rounded to somewhat .truncate. Surface ornamented by costellae of 

nearly equal size; pedicle valve displaying finely 

beaded costellae; brachial valve occasionally bearing small oblique wrinkles adjacent to hinge. 

Pedicle valve moderately convex in lateral profile; 

umbo somewhat swollen; flanks gently convex to 

flat. Ventral interarea moderately long, pseudodeltidium absent or rudimentary. Interior of pedicle 

valve: teeth small; delthyrial floor thickened with 

callus deposits into which small adductor pits are 

incised. Adj ustor-diductor field large, subflabellate, 

reaching to about midlength, and diverging in front 

of a short median ridge. 

Brachial valve gently concave in lateral profile 

and having maximum concavity at about the middle. 

Dorsal interior displaying slightly diverging septa, 

which reach greatest elevation just anterior to middle; anterior slope of crest steep and papillose. 

Medial region marked by weak ridge. Adductor 

muscle field long, extending to midlength; impressions about equal in size and bordered laterally by 

nearly straight margins. Inner surface finely 

papillose. 

Dist1·ibution and mateTial.-This species is found 

in the Grier Limestone Member of the Lexington 

Limestone. Four USGS localities ( 4871-CO, 4872-

CO, 4876-CO, and 4956-CO) yielded 119 disarticulated valves. 

Types.-Holotype, USNM 208592, a pedicle valve 

from the Grier Limestone Member of the Lexington 

Limestone. USGS loc. 4956-CO; length 7.4 mm, 

width 13.0 mm. Paratype, USNM 208589, a dorsal 

valve, USGS Joe. 4956-CO; length 5.5 mm, width 

10.4 mm. Paratype, USNM 208590, a pedicle valve, 

USGS loc. 4956-CO, length 6.7 mm, width 12.2 mm. 

Paratype, USNM 208591, a dorsal valve, USGS loc. 

4956_.CQ, length 6.7 mm, width 12.3 mm. Paratype, 

USNM 208593, a dorsal valve, USGS loc. 4956-CO, 

length 7.4 mm, width 14.4 mm. 

Rema1·ks.-S. gTierensis is closely related to a 

group of Shermanian Sowe1·byella that includes S. 

cu1·dsvillensis (Foerste), S. eximia Cooper, and S. 

monilifeTa Cooper. All of thes,e forms display beaded 

ornamentation, incised adductor scars in the ventral 

valve, and with the exception of S. g1·ieTensis, all 

are large for the genus. S. gTierensis most closely 

suggests S. cwrdsvillensis, but it is much smaller and 

more delicate than the latter and the costellae are 

more equally developed. Also, the outer margins of 

the dorsal muscle field are nearly straight in contrast to the rounded borders of S. curdsvillensis. 

The trivial name, g1·ierensis, alludes to its occurrence in the Grier Limestone Member of the Lexington Limestone. 

Sowerbyella rugosa (Meek) 

Plate 1, figures 17-20 

Leptaena rugosa Meek, 1873, p. 72, pl. 5, figs. 3f, g, h. 

Sowerbyella ru,qosa (Meek). Cooper, 1944, p. 335, pl. 128, 

figs. 41-43. 

Sowerbyella ru,qosus (Meek). Caster and others, 1961, pl. 2, 

figs. 14-16. 

Sowerbyella rugosa (Meek). Howe, 1972, pl. 1, figs. 4-7. 

Remarks.-St.udy of large suites of S. rugosa in 

the collections at the U. S. National Museum shows 

a number of diagnostic features for this species, 

namely: rugose surface ,exteriors, oblique wrinkling 

along the posterior margins of both valves, acute 

cardinal extremities, and a well-defined dorsal 

median septum. The U.S. Geological Survey collections from the Kope Formation contain specimens 

that are smaller than most of those examined in the 

National Museum, but in other aspects they are 

characteristic of the species. Occasional specimens 

in both the National Mus•eum and the Kentucky material show slightly elevated dorsal lateral septa 

somewhat suggestive of Thaerodonta. 

Material.-The USGS collection consists of 37 

specimens from the Kope Formation, loc. 7978-CO. 

C01nparison.-S. rugosa suggests Tlwe1·odonta 

aspera Wang in its rugose exterior, but it lacks the 

accessory teeth, hinge denticulations, and elevated 

dorsal lateral septa of that species. 

Fig"r-o·ed specimens.-USNM 208596 and 208597, 

respectively, a pedicle valve and complete specimen, 

from Kope Formation, USGS loc. 7978-CO ; and 

USNM 170730, dorsal valve, from Kope Formation 

outcrop behind the Newport Shopping Center on 

U.S. Highway 27, Newport, Ky. 

Sowerbyella sp. 

Plate 2, figures 1-13 

Desc1·iption.-Outline semielliptical, wider than 

long; cardinal extremities acute to obtuse. Surface 

unevenly multicostellate, consisting of one to four 

finer costellae separated by somewhat larger ones. 

Pedicle valve moderately convex in lateral pr-ofile. Interarea long, apsacline. Ventral interior 

papillose. Muscle field elongate forming strongly 

bilobed outline anteriorly. Adductor scars deeply 

incised into adventitious deposits on delthyrial floor; 
C4 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

diductor scars large, separated posteriorly by short 

septum. Hinge showing incipient fossettes on occasional specimens. Pseudodeltidium absent or rudimentary. _, 

Brachial valve moderately concave at the umbo 

becoming gently concave laterally and anteriorly. 

Occasional specimens, including juveniles, show 

incipient dentides along cardinal margins. Dorsal 

muscle field transversely subelliptical, extending 

about two-thirds the length of the valve. Medial 

septa slightly divergent, merging anteriorly with an 

elevated platform that is thickened and spinose. 

Inner and outer adductor scars about equal in size. 

Median septum weak, occasionally well defined. 

Brachiophores long, bladelike, ending in sharp 

points. Inner surface finely papillose. 

Remarks.-A number of specimens of Sowerbyella sp. show incipient denticles on the brachial 

valve and corresponding fossettes on the pedicle. 

This morphology presages the much stronger accessory denticula,tions observed in the Late Ordovician genus Thaerodonta. None of the brachial valves 

show elevated lateral s~epta in the dorsal muscle field 

and only one of the ventral interiors develops accessory teeth such as in Thaerodonta. Sowerbyella 

sp. appears to be a connecting link between the late 

Shermanian species of the genus, which are large and 

have delthyrial thickening and incised ventral adductors, and the genus Thaerodonta, characterized 

by hinge denticulations, strong accessory teeth, and 

dor,sal lateral septa.. 

Comparison.-Sowerbyella sp. is most like S. 

rugosa, another Edenian species, but it differs in 

lacking the strongly lamellose exterior and oblique 

wrinkling of that form. Sowerbyella sp. is also 

similar to the Richmondian species, Thaerodonta 

clarksvillensis, but the latter is larger (fig. 2) and 

has hinge denticulations and elevated lateral septa. 

M aterial.-More than 200 disarticulated valves, 

the majority of which are brachial valve·s, were recovered from the Point Pleasant Tongue of the Clays 

Ferry Formation at USGS loc. 8068-CO. An additional 55 specimens came from Clays Ferry locs. 

4905-CO, 5058-CO, 7472""""'CO, and 7478-CO. Anumber of coquinoid limestone slabs display large number's of disarticulated valves and fragments. 

Dimensions.-Growth patterns of length to width 

are given in figure 2 for comparison with representatives of Thaerodonta clarksvillensis, the succeeding sowerbyellid sp·ecies in the stratigraphic S'ection. 

Figured specimens.-USNM 208600, 208601, two 

brachial valves, from Clays Ferry Formation, USGS 

loc. 5058-CO; USNM 208602, a complete ~specimen 

:::c 

1-

0 

~ 

24 

20 

15 

10 

0 

0 

0 

• ~ 0. oO 

0 •• 0 0 

0 8 

0 

0 

0 

• 0 

• 

• 

• 

•• 

• 

• • 

• • 

• • 

• • 

• • 

• 

, .. • 

a~~--~~--~~--~--~~-----

3 5 10 13 

LENGTH 

FIGURE 2.-Scatter diagram of length-width in millimeters (brachial valve) of Sowerbyella sp. (open circles) from the Point Pleasant Tongue of the Clays 

Ferry Formation, USGS loc. 8068-CO; and Thaerodonta clarksvillensis (solid circles) from Richmondian 

sedimentary rocks at Waynesville, Ohio, USNM 40460. 

from Clays Ferry Formation, USGS loc. 4905-CO; 

and USNM 208603-208608, from Point Pleasant 

Tongue of Clays Ferry Formation, USGS loc. 8068-

CO. 

Genus THAERODONTA Wang, 1949, amended 

Howe, 1972 

Thaerodonta darksvillensis (Foerste) 

Plate 2, figures 14-17 

Plectambonites rugosa-clarksvillensis Foerste, 1912, p. 127, 

pl. 1, figs. 7 A-C, pl. 10, figs. 7 A-D. 

Sowerbyella clarksvillensis (Foerste). Cooper, 1944, p. 335, 

pl. 128, figs. 39-40. 

Sowe,.,.byella rugosus clarksvillensis (Foerste). Caster and 

others, 1961, pl. 7, figs. 25 and 26?. 

Thaerodonta clarksvillensis (Foerste). Howe, 1972, pl. 1, 

figs. 1-3. 

Description.-Shell of medium size for the genus; 

length about sixth-tenths the width; hinge usually 
MIDDLE AND LATE ORDOVICIAN BRACHIOPODS C5 

forming the greatest width; cardinal extremities 

acute to obtuse; anterior margin rounded to slightly 

truncate. Surface unequally multicostellate; occasionally lamellos,e in anterior part of shell. 

Pedicle interior: apex of delthyrial floor filled with 

callus deposits into which small adductor scars are 

deeply incised; adjustor-diductor muscle field large, 

reaching beyond midlength and diverging in front 

of median septum; adjustors and diductors about 

equal in size. Teeth small, supported by advancing 

dental plates. Hinge fossettes large, ranging from 

four to eight in most specimens, and situated on 

cardinal flanks. 

Brachial interior: cardinalia displaying short 

brachiophores that end in points; cardinal process 

strongly elevated. Adductor musde field ma~ked by 

. two P'air,s of septa, the outer pair being weaker than 

the inner ones. Hinge flanks marked by denticles 

corresponding in position to the ventral fossettes. 

Comparison.-:-This species sugges;ts S. curdsvillensis in shape and in size (fig. 1 and table 1), but 

it differs from the Shermanian form in having dorsal lateral septa and hinge-like denticulations. 

ThaeTodonta cla1·ksvillensis is similar to Sowerbyella 1·ugosa· in many aspects but differs from the 

Edenian species in having a normally ,smooth exterior, hinge..;line denticulations, and somewhat less 

width relative to length. Also, posterior wrinkling is 

not as common or as pronounced as is found in 

Sowe1·byella 1.,ugosa. Thaerodonta claTksvillensis 

most closely resembles T. recedens (Sardeson) from 

the Maquoketa Shale of Iowa and Minnesota in 

size, shape, weakness of accessory teeth in the 

ventral valve, and weakness of lateral septa in the 

dorsal muscle field. The Ohio Valley form has fewer 

and distinctly weaker hinge-line denticulations. The 

differences may reflect geographic separation of 

populations of the same species. 

TABLE 1.-Measurements (in millimeters) of length and 

width of species of Sowerbyella and Thaerodonta 

Species -------------- II III IV 

Number (N) .,. ________ 24 26 23 24 

Length (L) (mean) 10.6 9.73 6.4 10.53 

Observed range, L ---- 8.2-11.7 7.7-12.2 4.3-8.5 8.2-12.2 

Width (W) (mean) 18.60 17.58 13.40 16.98 

Observed range, W ___ 15.7-22.1 13.6-23.3 10.8-17.6 14.2-20.0 

I. Sowcrbyclla cttrdsvillcnsis ( Foerste), from the Curdsville Limestone 

Member of the Lexington Limestone, USGS locs. 5101-CO and 7785-CO. 

H. 7'/t.ncrodonta clarksvillcnsis (Foerste), from Richmondian strata at 

Waynesville, Ohio, USNM 40460. 

III. Sowm·l>yclla sp., fl'Om Point Pleasant Tongue of Clays Ferry Formation, USGS Joe. 8068-CO. 

IV. Tlwcrodontct rcccdcns ( Sardeson) , from Maquoketa Shale, near 

Spring Valley, Minn., USNM collection. 

Superfamily RHYNCHONELLACEA Gray 

Family RHYNCHOTREMA TIDAE Schuchert nom. transl. Cooper 

Genus RHYNCHOTREMA Hall, 

1860; emended Wang, 1949; Cooper, 1956; 

Howe, 1965 

Rhynchotrema dentatum (Hall) 

Plate 7, figures 21, 22 

At·rypa dentata Hall, 1847, p. 148, pl. 33, figs. 14a-c. 

Rhynchonella, dentata (Hall). Meek, 1873, p. 121, pl. 11, figs. 

3a-d. 

Rhynchot·rema dentatum arnheimensis Foerste, 1909a, p. 227, 

pl. 4, fig. 12. 

Rhynchotrema clentatum arnheimensis Foerste 1910 p. 27, 

pl. 3, fig. 13. ' ' 

Rhynchotrema dentata (Hall). Foerste, 1910, p. 29, pl. 2, 

fig. 16, pl. 3, fig. 12. 

Rhynchot'rema dentatum arnheimensis Foerste. Bassler, 1932, 

pl. 24, figs. 5-8. 

Rhynchotrerna dentaturn (Hall). Cooper, 1944, p. 309, pl. 118, 

figs. 11-13 . 

Rhynchot·rema dentatmn (Hall). Wilson, 1948, pl. 19, figs. 

23-25. 

Rhynchot·rerna clentatwm, (Hall). Wilson, 1949, pl. 19, figs. 

23-25. 

Rhynchotr·ema dentaturn (Hall). Caster and others, 1961, pl. 

5, figs. 19-23. 

Rhynchotrerna clentaburn (Hall). Howe, 1965, pl. 134, figs. 4, 

13. 

Rhynchotrema dentaturn (Hall). Howe, 1969, pl. 155, figs. 

1-8; pl. 156, fig. 25. 

Remarks.-Three USGS localities (D1248-CO, 

D1247-·CO, and D1246-CO) in the Bull Fork Formation (Richmondian) yielded nine specimens, all 

of: which are partially exposed on bedding surfaces 

of lim·eg,tone samples. These specimens conform to 

the shape and size variation displayed in the large 

collections of R. dentatum from Ohio and Indiana. 

which are reposited in the U.S. National Museum: 

They al,so conform to the large numbers of specimens recovered by Howe (1969) from .the "Arnheim" Formation and basal calcarenites of the 

overlying Fernvale Formation in Tennessee. This 

species is a common and diagnostic faunal element 

of Richmondian beds in Ohio and Indiana (Caster 

and others, 1961). 

FiguTed specimens.-USNM 208689 (pl. 7, fig. 

21), from the Bull Fork Formation (Richmondian), 

USGS loc. D1247~CO; USNM 208690 (pl. 7, fig. 

22), from ,the Bull Fork Formation, USGS loc. 

D1246-CO. 

Rhynchotrema increbescens (Hall) 

Plate 3, figures 1-30 

Atrypa increbescens Hall, 1847, p. 146, pl. 33, figs. 13c-d 

(lectotype designated by Wang, 1949, p. 11). 

Rhynchonella (Rhynchotrema) increbescens (Hall). Hall, 

1860, p. 66. 

Trematospira ( ?) quadriplicata Miller, 1875, p. 60, figs. 6, 

7. 
C6 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Rhynchotrema inaequivalve ( Castelnau). Foerste, 1909b, p. 

314, pl. 7, figs. lOA-C. 

Rhynchotrema inaequivalve (Castelnau). Miller, 1913, pl. 6, 

fig. 3. 

Rhynchotrema kentuckiense Fenton and Fenton, 1924, p. 67, 

pl. 1, figs. 4, 5; 18-22. 

Rhynchotrema kentuckiense va.rians Fenton and Fenton 

1924, p. 68, pl. 1, figs. 1-3. ' 

Rhynchotrema mercerense Fenton and Fenton, 1924, p. 69, 

pl. 2, figs. 17-21. 

Rhynchotrema increbescens (Hall). Bassler, 1932, pl. 18, figs. 

7, 8. 

Rhynchotrema increbescens (Hall). Cooper, 1944, p. 309, pl. 

118, figs. 14-16. 

Rhynchotrema kentuckiense Fenton and Fenton. Cooper, 

1956, p. 629, pl. 130, A, figs. 1-5. 

Rhynchotrema increbescens (Hall). Cooper, 1956, pl. 138, A, 

figs. 1-5. 

Rhynchotrema increbescens (Hall). Wilson, 1949, pl. 9, figs. 

5-9. 

Rhynchotrema qu.adriplicata (Miller). Howe, 1965, pl. 134, 

figs. 3, 11, 12, 14. 

Rhynchotrema sp., Howe, 1965, pl. 134, figs. 2, 10. I 

Rhynchotrema increbescens (Hall). Alberstadt, 1973, p. 51, 

pl. 7, figs. 6, 7. 

1 

Rhyncho.trema increbescens (Hall). Schmidt, 1965, fig. 422, 

3a~. 

Description.-Shell of average size for the genus; I 

width and length about equal. Lateral profile unequally biconvex, the brachial valve having the I 

greater depth. Outline subtriangular to subelliptical; 1 

anterolateral margins rounded in outline; anterior 

commissure strongly uniplicate with the denth of 

the sulcus averaging more than one-half of th~ total 

thickness of the shell. Surface multicostate, numbering about 14 to 20 costae (table 2), of which 4 

occur on the fold and 3 in the sulcus. Surface crossed 

by closely spaced zig-zag lamellae, which become 

especially conspicuous near the anterior commissure. 

Pedicle valve moderately convex in lateral profile, 

having the gre-atest convexity at about the middle. 

Beak elevated and suberect; umbo swollen, merging 

anteriorly with a progressively widening sulcus that 

·occupies somewhat more than one-half the width 

of the valve at the front. Ventral flanks gently inflated. Interior of pedicle valve: delthyrium triangular and open or partially closed by rudimentary 

deltidial plates; beak occasionally resorbed to form 

a small apical foramen. Delthyrial floor large, occupied by scar of pedicle attachment. Teeth strong, 

supported by thin dental plates; umbonal cavities 

small and commonly reduced by shell thickening. 

Ventral muscle field large and flabellate in outline 

in mature specimens, occasionally subquadrate in 

juveniles; adductor scars small, incised, truncate 

at the back and tapering anteriorly; diductor scars 

large, expanding anteriorly to enclose the adductor 

impressions; adjustor scars situated at lateral margin of field, occasionally attaining the width of the 

diductors (fig. 3). 

Brachial valve strongly convex in lateral profile, 

the greatest depth occurring at about the middle. 

Umbo broadly swollen, merging anteriorly with a 

fold that becomes prominent at the front; flanks inflated. Interior of brachial valve: hinge plates divided, thick, gently concave and supporting short 

crura; cardinal process bladelike and dividing narrow notothyrial cavity; shaft low to strongly 

swollen and elevated. Adductor muscle field oval in 

outline, the posterior and anterior pair about equal 

in size. 

Dimensions.-Growth patterns of length to width, 

length to thickness, thickness to height of fold, and 

width to fold width are given in figures 4-7 for 

comparison with R. wisconsinense from the Decorah 

Formation in Minnesota. 

Distribution.-Rhynchotrema increbescens is one 

of the most abundant brachiopods in late Middle 

Ordovician rocks in Kentucky. USGS samples yield 

more than 5,000 specimens from the following 

stratigraphic members (arranged in order of decreasing age) : 240 specimens (about 90 percent 

disarticulated and partially broken) from the 

Curdsville Limestone Member of the Lexington 

Limestone; USGS locs. 4123-CO, 4213-CO, 5023-

CO, 5080-CO, 5100-CO, 5101-CO, 7782-CO, 7784-

CO, and 7785-CO. Approximately 500 specimens 

(about 65 percent disarticulated and partially 

broken) from the Grier Limestone Member of the 

Lexington Limestone; USGS locs. 4072-CO, 4073-

CO, 4075-CO, 4852--'CO, 487 4-CO, 4876-CO, 4879-

CO, and 4957-CO. Approximately 4,300 specimens 

(more than half articulated juveniles) from the 

upper part of the Grier Limestone and the Perryville Limestone Members of the Lexington Limestone. About 40 articulated specimens from the 

Brannon Member of the Lexington Limestone and 

245 specimens from the Tanglewood Limestone 

Member of the Lexington Limestone; USGS locs. 

D1119-CO, D1120-CO, D1121-CO, D1123-CO, 

4982-CO, 7790-CO, and 7809-CO. 

Discussion.-Considerable confusion has surrounded the genus Rhynchotrema Hall. Rhynchotrema increbescens (Hall) is the type species, although Hall (1860, p. 68) described the characters 

of the genus from three specimens now assigned to 

Lepidocyclus manniensis (Foerste). Wang (1949) 

designated a specimen that was figured by Hall 

(1847, pl. 33, fig. 13c-d) as lectotype of R. increbescens. Through the courtesy of Norman D. 

Newell, I was able to examine the type lot, which is 
MIDDLE AND LATE ORDOVICIAN BRACHIOPODS C7 

....... ______ , 

A B c 

D 

E F 

FIGURE 3.-Interior views of Rhynchot?·ema increbescens (Hall) showing variations in pedicle musculature, X 4, USNM 

208635A-F, respectively, from the Perryville Limestone Member of the Lexington Limestone, USGS loc. 5015-CO. 

reposited in the American Museau of Natural History. A total of sev,en specimens are in the type collection (instead of four as reported by Cooper, 

1956). Except for one specimen, which may be a different species, the Hall specimens conform to the 

size and shape exhibited by the Lexington members; 

thus, they appear to be conspecific (figs. 4 and 5). 

Com,paTison.-R. incTebescens is similar to R. 

wisconsinense Fenton and Fenton in size, and only 

slight differences in shape are noted. R. incr-ebescens 

is somewhat narrower and not as thick relative to 

length, and it has a somewhat larger fold and sulcus 

(figs. 4-7). Surface ornamentation is the major difference between the two species. R. wisconsinense is 

more costate (table 2), and its surface lamellae are 

much more conspicuous. 

TABLE 2.-Number of costae (brachial valve) in species of 

Rhynchotrema 

[,u-range of means; C.L.-confidence Ievell 

Species -------------------· 

Number (N) --------

Mean ---------------

Observed range _____ _ 

Standard deviation __ _ 

p, (95 percent C.L.) 

p, (99 percent C.L.) __ _ 

28 

17.37 

14-20 

1.486 

16.9-17.86 

16.69-18.07 

II 

45 

21.09 

17-24 

1.743 

20.65-21.53 

20.46-21.72 

I. Uhy11chotrcma increbesccns (Hall) from the Salvisa Bed of the Perryville Limestone Member of the Lexington Limestone, USGS Joe. 5015-CO. 

II. R. wisconsincnse Fenton and Fenton, from the Ion Dolomite Member 

of the Decorah Formation, roadcut exposure, 1% mi east of U.S. Highway 52, south edge of Cannon Falls, Minn., USNM 179571, collected by 

0. C. Cole. 
C8 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

15 13 

10 

:I: 

...... 

0 

~ 

5 

JL-~--~~--~--~~--~--.__. ___ 

5 10 15 

LENGTH 

FIGURE 4.-Scatter diagram and reduced major axes of 

length-width in millimeters of Rhynchotrema increbescens (solid circles) from the Perryville Limestone 

Member of the Lexington Limestone, USGS loc. 5015-

CO; R. wisconsinense Fenton and Fenton (open 

circles) from the Ion Dolomite Member of the Decorah 

Formation, county road exposure, 114 mi east of U.S. 

Highway 52, south edge of Cannon Falls, Minn., 

USNM 179571, collected by 0. C. Cole. R. increbescens from Trenton Group, Middleville, N. Y. (type 

lot AMNH 707/1 shown in solid triangles). + marks 

means of dimensions. 

Genus ROSTRICELLULA Ulrich and Cooper, 1942 

Rostricellula minuta Cooper, 1956 

Plate 7, figures 9-12 

Rostricellula ? minuta Cooper, 1956, Cooper, p. 640, pl. 

137, A, figs. 1-6. 

RemaTks.-This species, which Cooper tentatively assigned to the genus Rosttticellula, is found only 

sparingly in the Logana Member of the Lexington 

Limestone. The USGS collections include six dorsal 

valves from loc. D1196-CO and a small complete 

specimen from loc. 5073-CO. They show a more 

triangular outline than the types of the species from 

the Hermitage Formation in Tennessee, but the 

small size, high fold, and deep sulcus marked by a 

single costa are diagnostic features. The fold is 

strongly elevated at the front and bears two strong, 

angular costae. The flanks display seven to nine 

costae. The nonimbricate ornamentation and absence 

of a cardinal process indicate relationship to 

RostTicellula. 

10 

CJ) 

CJ) 

w 

z 

~ 

u 

:I: 

...... 5 

FIGURE 5.-Scatter diagram and reduced major axes of 

length-thickness in millimeters of Rhynchotrema increbescens (solid circles) from the Perryville Lime-

·stone Member of the Lexington Limestone, USGS loc. 

5015-CO; R. wisconsinense Fenton and Fenton (open 

circles) from the Ion Dolomite Member of the Decorah 

Formation, county road exposure, 114 mi east of U.S. 

Highway 52, south edge of Cannon Falls, Minn. Collected by 0. C. Cole. R. increbescens from Trenton 

Group, Middleville, N.Y. (type lot AMNH 707/1 shown 

in solid triangles). + marks means of dimensions. 

Figwred spec'imens.-USNM 208691 (pl. 7, fig. 9), 

from 0.5 ft from the top of the Logana Member of 

the Lexington Limestone, USGS loc. D1196-CO 

length 6.8 mm, width 7.2 mm, USNM 208692 (pl. 7, 

figs. 10-12), from the upper part of the Logana 

Member of the Lexington Limestone, USGS Joe. 

5073~Co; length 5.1 mm, width 5.1 mm. 

Family LEPIDOCYCLIDAE Cooper 

Genus LEPIDOCYCLUS Wang, 1949; emended Howe, 1965 

Lepidocyclus? capax (Conrad) 

Plate 4, figures 1-10 

Atrypa capax Conrad, 1842, p. 264, pl. 14, fig. 21. 

Atrypa increbescens Hall, 1847, p. 146, pl. 33, figs. 13t-y. 

Rhynchonella capax (Conrad). Meek, 1873, p. 123, pl. 11, 

figs. 2a-f. 

Rhynchonella perlamellosa Whitfield, 1882, Whitfield, p. 265, 

pl. 12, figs. 23-25. 

Rhynchotrema capax (Conrad). Hall and Clarke, 1894a, p. 

825, pl. 42, figs. 11, 12, 16 (not figs. 13, 14, 15). 
MIDDLE AND LATE ORDOVICIAN BRACHIOPODS C9 

I 

I0 

~ 

0 

...J 

0 

u. 

10 

5 

10 

WIDTH 

15 

FIGURE 6.-Scatter diagram and reduced major axes of 

width-fold width in millimeters of Rhynchotrema inc·rebescens (solid circles) from the Perryville Limestone Member of the Lexington Limestone, USGS loc. 

5015-CO and R. wisconsinense Fenton and Fenton 

(open circles) from the Ion Dolomite Member of the 

Decorah Formation, exposure on county road, 1 14 mi 

east of U.S. Highway 52, south edge of Cannon Falls, 

Minn.; USNM 179571, collected by 0. C. Cole. + 

marks means of dimensions. 

Rhynchotrema capax (Conrad). Hall and Clarke, 1894b, p. 

183, pl. 56, figs. 14, 15, 22, 23 (not figs. 16, 17, 18, 

20, 21). 

Rhynchotrema capax (Conrad). Winchell and Schuchert, 

1895, p. 462, pl. 34, figs. 30-33. 

Rhynchotrema capax (Conrad). Cooper, 1944, p. 309, pl. 

118, figs. 7-10. 

Rhynchotrema capax (Conrad). Caster and others, 1961, pl. 

5, figs. 7-10. 

Rhynchotrema perlamellosum (Whitfield). Cooper, 1944, p. 

309, pl. 118, figs. 29-30. 

Lepidocyclus pe?·lamellostts (Whitfield). Wang, 1949, p. 14, 

pl. 6A, figs. 1-5. 

Lepidocyclus? capax (Conrad). Howe, 1965, pl. 134, figs. 15, 

16, 20; 1966, p. 263, pl. 31, figs. 15-20; 1967b, p. 850, 

pl. 104, figs. 1-5, 11-14, 23; pl. 105, fig. 10; 1969, p. 

1341, pl. 156, figs. 1-14. 

Lepidocyclus? sp. Howe, 1965, pl. 134, fig. 20. 

Lepidocyclus capax (Conrad). Alberstadt, 1973, p. 53, pl. 

6, figs. 1-3. 

Remwrks.-This species is one of the most widespread and diagnostic brachiopods in Upper Ordovician rocks of North America. It is particularly common in Richmondian rocks of the Ohio Valley and 

in correlative strata in Texas, Oklahoma, Mis:souri, 

and Tennessee. It is less oommon in the Maquoketa 

Shale of Iowa and the Ely Springs Dolomi.te of 

Nevada. A larger form, identified as L. gigas by 

Macomber (1970), from the Bighorn Dolomite in 

0 

...J 

0 

u. 

u. 

0 

II 

(.!J 

w 

I 

10 

5 

0 5 

THICKNESS 

10 12 

FIGURE 7.-Scatter diagram and reduced major axes of 

thickness-height of fold in millimeters of Rhynchotrema increbescens (solid circles) from the Perryville 

Limestone~ember of the Lexington Limestone, USGS 

loc. 5015-C~nd R. wi .:;consinense Fenton and Fenton 

(open circles) ~'\om the Ion Dolomite Member of the 

Decorah Formation, exposure on county road, 114 mi 

east of U.S. Highway 52, south edge of Cannon Falls, 

Minn.; USNM 179571, collected by 0. C. Cole. + 

marks means of dimensions. 

Wyoming appears to differ from L. capax only in its 

much larger size. Specimens from the "Arnheim" 

Formation of Tennessee are smaller than those in 

the Ohio Valley and they average nearly three more 

costae per valve. The Oklahoma representatives of 

the species are larger and slightly less costate than 

the norm for the Ohio Valley. These differences 

probably reflect the geographic separation of the 

populations. 

Rhynchotrema increbescens suggests L. capax in 

many aspects, and it is pr.obably directly ancestral 

to .the Late Ordovician species. Internally, both 

fo-rms display a fiabellate muscle field in the ventral 

valve, a delthyrium which is open or only partially 

closed by rudimentary deltidial plates, and a large 

delthyrial cavity which is wholly occupied by the 

scar of the pedicle attachm·ent. Moreover, occasional 

specimens of L. capax exhibit Rhynchot?·ema-like 

dental plates that are not completely obscured by 

shell thickening. Externally, the two forms are very 

, similar except for the smaller size of R. increbescens 

and its moderately elevated ventral beak. L. capax 

occupies a position that is intermediate between 

Lepidocyclus and Rhynchotrema because of its open 

delthyrium and large pedicle callist. 

Material.-Three USGS localities (D1259-CO .. 

D1260-CO, and D1263-CO) in the Bull Fork For-
C10 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

mation yielded 11 specimens. An additional 7 4 specimens were recovered from six localities in the 

Dillsboro Formation of Indiana-6139-CO, 6140-

CO, 6141-CO, 4573-CO, 4574-CO, and 4575-CO. 

Figured specimens.-USNM 208649, from Bull 

F·ork Formation, USGS loc. D1259-CO; USNM 

208650-53, from Dillsboro Formation, USGS loc. 

6139-CO; and USNM 208654 and 208655, from 

Richmondian roadcut, U.S. Highway 50, 3.1 mi 

east of Versailles, Ind. 

Family ORTHORHYNCHULIDAE Cooper 

Genus.ORTHORHYNCHULA Hall and Clarke, 1893 

Orthorhynchula linneyi (James), 1881 

Plate 4, figures 11-18; plate 5, figure 7; plate 6, 

figures 1-15; plate 7, figures 1-4. 

Orthis? linneyi James, 1881, p. 41. 

Orthis linneyi James. N ettleroth, 1889, p. 41, pl. 34, figs. 

7-13. 

Orthorhynchula linneyi (James). Hall and Clarke, 1894a, p. 

181, pl. 56, figs. 10-13. 

Orthorhynchula linneyi (James). Foerste, 1910, p. 24, pl. 3, 

fig. 10. 

Orthorhynchula linneyi (James). Schuchert and Cooper, 

1932, pl. 16, figs. 12, 17, 28-30. 

Orthorhynchula linneyi (James). Cooper, 1944, p. 309, pl. 

117, figs. 41-47; (1956) pl. 128, F, figs. 32-36. 

Orthorhynchula linneyi (James). Wilson, 1949, pl. 18, figs. 

6-9. 

Orthorhynchula linneyi (James). Caster and others, 1961, 

pl. 3, figs. 32, 33. 

Orthorhynchula linneyi (James). Schmidt, 1965, fig. 425, 

3a-c. 

Description.-Shell .subtriangular to occasionally 

subelliptical in outline; apical angle slightly more 

than 90°; sides broadly rounded; valves subequal in 

depth, the brachial valve deeper and showing greatest width at the middl·e; width somewhat exceeding 

length; hinge line short, averaging somewhat less 

than half of the shell width.· Surface costate, ornamented with 3 costae in sulcus, 4 on the fold, and 

7 to 13 on the flanks. 

Pedicle valve gently to moderately convex in 

in lateral profile, displaying the greatest convexity 

between the umbo and the middle of the valve. Umbo 

swollen with moderately steep sides; flanks gently 

inflated. Sulcus originating in front of umbo and 

forming a mesial depression that increases in width 

to about one-half the shell width at the front. Interarea of pedicle valve short but well defined, averaging somewhat less than one-half the shell width; 

delthyrium large, open, with small apical foramen 

usually present through beak resorption. 

Brachial valve moderately to strongly convex in 

lateral profile, displaying the greatest curvature in 

the posteri·or half. Umbo inflated, merging anteriorly with a fold which bears four costae, the lateral 

pair of which are weaker and lower than the median 

costae; fold becoming moderately elevated at the 

front and occupying about one-half the valve width. 

Flanks moderately convex. Dorsal interarea smaller 

than the ventral one and varying from about fourtenths to one-half the valve width. 

Interior: Teeth large, supported by ·short dental 

plates that may become obscured by adventitious 

deposits in gerontic forms. Ventral muscle field 

typically quadrate in outline and occupying from 

one-third to one-half the valve length; adductor impressions gently forming a linear track in the anterior one-half to two-thirds of the muscle field; diduct.or scars moderately impressed, elongate; adjus tor scars commonly indistinguishable from diductors; when defined, adj us.tors occupy the sides of 

the muscle field and are shorter than the diductors. 

Dorsal muscle field extending to about the middle 

of the valve and divided medially by a low ridge extending from the notothryial platform; adductor 

scars unequal in sjze, the posterior pair the larger. 

Dorsal hinge plates deeply concave and bordered by 

long crura, which are extended anteriorly. Cardinal 

process directed posteriorly, supported by main 

shaft, which is most commonly bilobid on the myophore; accessory ridges commonly p"roduce a multilobate form to the myophore. Diductor impressions 

extending from the posterior face of the myophore 

and along the sides of the cardinal shaft. 

Dimensions.-Growth patterns of length to width, 

length to thickness, thickness to height of fold, and 

width to fold width are given in figures 9-12 for 

comparison with Orthorhynchula sublinneyi from 

the Devils Hollow Member of the Lexington Limestone. 

Dist?·ibution.-Orthorhynchula linneyi is one of 

the most common brachiopods found in the Calloway Creek Limestone (Maysvillian) of Kentucky. 

The Calloway Creek material at hand consists of 

approximately 1,250 specimens from USGS locs. 

€409-CO and 6413-CO. Nearly all of the specimens 

are disarticulated and partially to extensively fragmented. The overlying Ashlock F·ormation yielded 

only three pedicle valves from USGS loc. 6411-CO. 

Comparison.-The Maysvillian species is very 

similar to its ancestral form, 0. sublinneyi n. sp., 

in size and in growth patterns of length to width, 

length to thickness, thickness to height of fold, and 

width to fold width (figs. 9-12). The scattergrams 

suggest that 0. linneyi is somewhat narrower i:.1 

I outline, more globose in lateral profile, and slightly 

I 

narrower in its fold. Because the differences are 

small and sample preservation precluded normally 
MIDDLE AND LATE ORDOVICIAN BRACHIOPODS C11 

A 

B 

', ........ ________ ,--

c 

E 

D 

F 

' \ 

I 

I 

I 

FIGURE 8.-Interior views of 0Tthorhynchula linneyi showing variations in musculature, X 2; A, B, C, pedicle valves, 

USNM 208663, 208664, and 208696; D, E, F, brachial valves, USNM 208700, 208704, and 208703. From the Calloway 

Creek Limestone (Maysvillian), USGS loc. 6409-CO. 

distributed data for all of the parameters, it is not 

clear whether these differences are significant. 0. 

linneyi is significantly less costate than 0. sublinneyi 

(averaging only 22 costae compared to 28 in the 

latter, table 3), and it has a more consistently subtriangular outline instead of the common subelliptical form of the Lexington Limestone species. The 

fold is characterized by four costae, whereas in 0. 

sublinneyi fold costation is much more variable, 

ranging from three to as many as eight costae. Only 

rare specimens of 0. linneyi show three costae and 

none in the collections have more than four. In about 

four-fifths of the specimens examined the lateral 

costae on the fold are distinctly less elevated than 

the central pair. A similar pattern occurs in the 

majority of 0. s~~bl'inneyi bearing four costae on the 

fold. 

Discussion.-This species w·as first described by 

James (1881) from specimens collected by W. M. 

Linney from the "upper part of the Cincinnati 

Group" in Boyle County, Ky. Although James did 

not include any illustrations or precise stratigraphic 

and geographic data, his description conforms to the 

Maysvillian form, 0. linneyi, rather than to forms 

from the Lexington Limestone previously noted in 

the literature as 0. linneyi but described herein as 

0. sublinneyi. James' description is as follows: 

Shell sub-oval in outline, breadth and length about as 4 to 

3; cardinal line less than half the broadest part of the shell; 

regularly and evenly rounded margin from the terminations 

of the cardinal line to the front; cardinal area short and 

confined to the ventral valve. Umbone of the ventral valve 

prominent, shell curving sharply to the beak which projects 

beyond that of the other valve and is incurved; a mesial 

sinus commencing near the beak, narrow and shallow at 
C12 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

30 20 

25 

15 

10 

8 

8 

. 

0 

0 

0 

10 

0 0 

0 

0 

0 

0 

. ••·•· • eo 

0 

. . • • i 

oo o.o 

0. 

• 0 

15 

LENGTH 

0 

• 0 0 

• • 0 

.. 0 

•oe 0 

0 

20 

0 

. 

24 

FIGURE 9.-Scatter diagram of length-width in millimeters of Orthorhynchula linneyi (open circles) from 

the Calloway Creek Limestone, USGS loc. 6409-CO 

and 0. subl-inneyi Howe n. sp. (solid circles) from the 

Devils Hollow Member of the Lexington Limestone, 

USGS locs. 5036-CO and 5095-CO. 

first, but widening and deeping to the front margin; deltidium triagonal, and rather broad. Beak of the dorsal valve 

projecting very little, if any, beyond the cardinal line, and 

but slightly incurved; a mesial elevation commencing rather 

low at the umbone, but becoming prominent near and at the 

front; front margin quite sinuous, caused by the mesial 

sinus of the ventral valve, and the prominent mesial sinus 

on the dorsal valve. Each valve covered by about 23 rather 

coarse, simple plications, three of which are in the sinus, 

and the same number on the mesial elevation. 

Nettleroth (1889, pl. 34, figs. 7-13) illustrated additional specimens of 0. linneyi, which were collected 

by W. M. Linney from "shales of the Hudson River 

or Cincinnati Group, near Danville, Kentucky." His 

figures show the less costate Maysvillian species 

rather than the earlier form, 0. sublinneyi, from the 

Lexington Limestone. 

Members of Orthorhynchula are characterized by 

long crura, ·strongly concave hinge plates in the 

dorsal valve, an orthoid-Iike cardinal process, a 

ventral quadrate muscle field, and a small but welldefined pedicle interarea. Schuchert and Cooper 

15 

• 

(/) 

(/) 

w 

z 

~ 

~10 :I: 

• 

• 

1- 0 

0 

olb 

• 

5 0 

0 

00 

.o 

• • • 

•• 

• 

• 

• • • 

• 

0 

• 

• 

oo 0 

0 

• • 

2~~~~~~~~~--~~._~~~~ 

7 10 15 

LENGTH 

20 22 

FIGURE 10.-Scatter diagram of length-thickness in 

millimeters of Orthorhynchula linneyi (open circles) 

from the Calloway Creek Limestone, USGS loc. 

6409-CO; and 0. sublinneyi Howe (solid circles) 

from the Devils Hollow Member of the Lexington 

Limestone, USGS locs. 5036-CO and 5095-CO. 

(1932, p. 226) transferred Por-ambonites ottawaensis Billings, a Trentonian species from Ontario, to 

Orthorhynchula because it possessed an interarea on 

the pedicle valve and a divided hinge plate with 

concave crural supports. Later, Cooper (1956, p. 

627) rea.ssessed the types of P. ottawaensis and 

compared additional material with the interiors of 

0. linneyi. He concluded that the two forms have 

TABLE 3.-N umber of costae (brachial valve) in species of 

Orthor hynchula 

[t.t-range of means; C.L.-confidence level] 

Species --------------------

Number (N) --------

Mean --------------- 0 bserved range _____ _ 

Standard deviation 

~ (95 percent C.L.) __ 

~ (99 percent C.L.) __ 

20 

22.80 

19-31 

2.75 

21.52-24.08 

19.94-25.66 

II 

20 

28.25 

23-38 

3.36 

26.68-29.82 

26.10-30.40 

·I. Orthorhynchula linneyi (James), from upper 5 ft of Calloway Creek 

Limestone (Maysvillian), USGS loc. 6409-CO. 

II. 0. sublinneyi Howe, n. sp., from the Devils Hollow Member of the 

Lexington Limestone, USGS Jocs. 5036-CO and 5095-CO. 
MIDDLE AND LATE ORDOVICIAN BRACHIOPODS C13 

30 

25 

• 

15 0 

0 

0 

10 0 

0 

0 

o o o• 

• • .! 

• • • 0 

• 011 

• • 0 

• 

0 

• 

• 

• • •• • • 0 

• 

0 

oo 0 0 

• 0 0 

0 

0 

0 

0 

• 

a----------._--------~--------~ 0 5 10 15 

FOLD WIDTH 

FIGURE 11.-Scatter diagram of width-fold width in millimeters of Ortho'rhynchula linneyi (open circles) from 

the Calloway Creek Limestone, USGS loc. 6409-CO; 

and 0. sublinneyi (solid circles) from the Devils Hollow Member of the Lexington Limestone, USGS locs. 

5036-CO and 5095-CO. 

little in common except for their interareas and, as 

a consequence, he established a new genus, Drepanorhyncha, bas·ed on the Billings species. According 

to Cooper, the conc:ave hinge plates of Drepanorhyncha lie o'bliquely facing one another rather 

than directly outward as in Or·thorhynchula. Additionally, he attributed generic significance t;o the 

long dental plates and absence of a cardinal process 

in his genus. Further study is needed to determine 

the ventral muscle pattern in D'repanorhyncha. In 

0. linneyi, the type species of Orthorhynchula, the 

diductors show variations in outline ranging from 

the typical quadrate pattern with angular corners 

to lobate forms with rounded margins. (Contrast 

C with A and Bin fig. 8.) 

Orthorhynchula sublinneyi Howe, n. sp. 

Plate 4, figures 19-31; plate 5, figures 1-6, 8-15 

Desc'ription.-Large, transversely subelliptical to 

subtriangular in outline; posterolateral margins 

15 

00 

0 

• t-10 

:I: 0 

Q • 

w 

:I: • • 

0 .o 

_J • • 

0 • • u... 5 • 

0 • 

0 

• 0 

0 0 

10 15 19 

THICKNESS 

FIGURE 12.-Scatter diagram of thickness-height in millimeters of fold of Orthorhynchula linneyi (open circles) from the Calloway Creek Limestone, USGS loc. 

6409-CO; and 0. sublinneyi (solid circles) from the 

Devils Hollow Member of the Lexington Limestone, 

USGS locs. 5036-CO and 5095-CO. 

widely divergent, lateral margins rounded, front 

margin nearly straight. Lateral profile unequally 

biconvex, the brachial valve being deeper. Surface 

multic01state, from 19 to 38 costae; sulcus and fold 

oommonly bearing 3 and 4 costae, respe·ctively, but 

variations include 2 to 6 in the sulcus and 3 to 8 

on the fold. 

Pedicle valve broadly convex in lateral profile; 

sulcus originating at the umbo, and increasing in 

width and depth anteriorly, where it attains nearly 

one-half the valve width at the front. Flanks of 

ventral valve gently swollen. Pedicle interarea apsacline and curved in lateral profile; short but well 

defined, and varying from four-tenths to about onehalf the shell width. Interior of pedicle valve: 

delthryium large, triangular, open; beak occasionally resorbed, forming an apical foramen ; delthryial 

cavity deep; teeth stout, supported by short, receding dental plates; umbonal cavities small, shallow, 

and com.monly obscured by adventitious deposits in 

adult specimens. Muscle field quadrate in outline 

. occasionally lobate (fig. 13)' and occupying one~ third to one-half the length of the valve; adductor 

scars small, forming a linear track in the front half 

of the muscle field; adjustors small, typically shorter 

than the diductors, but occasionally reaching the 

front margin; diductor scars large, elongate, forming angular to rounded anterolateral margins. 
Cl4 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

A 

B 

D 

I 

I 

I 

I 

I 

c 

E 

FIGURE 13.-Interior views of Orthorhynchula sublinneyi showing variations in ventral musculature. A, X 4, USNM 208684, 

from USGS loc. 6916-CO; B-E, USNM 208683, 208680, 208682, 208681, respectively, from USGS loc. 5036-CO. Solid 

outline is the muscle field; stippled outline is the actual muscle scars. 

Brachial valve moderately convex in lateral profile; flanks broadly inflated; fold originating at the 

umbo and occupying nearly one-half the shell width 

at the anterior commissure. Dorsal interarea smaller 

than the ventral one, poorly defined in some specimens. Interior of brachial valve: cardinal process 

bladelike and serrated posteriorly on the myophore, 

shaft low to strongly elevated and thickened, commonly becoming bilobid or even trilobid posteriorly; 

accessory ridges to the main shaft effecting a multilobate appearance to the myophore when present. 

Hinge plates strongly concave, hearing long crura 

that taper to points at the ends. Dorsal muscle field 

ovate in outline, separated mesially by a well-detined ·septum; anterior scars much smaller than 

posterior pair. 

Dimensions.-Growth patterns of length to width, 

length to thickness, thickness to height of fold, and 

width to fold width are given in figures 9-12 for 

comparison with 0. linneyi, its descendent species, 

from the Calloway Creek Limestone ( Maysvillian) . 

DistTibution.-0. sublinneyi is an important 

brachiopod of the Perryville Limestone, Devils Hollow, and Millersburg Members of the Lexington 

Limestone. The Perryville collection consists of approximately 450 specimens, mostly disarticulated 

and partially broken, from USGS locs. 6915-CO and 

1 6916-CO. The Devils Hollow material contains 
MIDDLE AND LATE ORDOVICIAN BRACHIOPODS C15 

more than a thousand spe-cim·ens recovered from 

USGS locs. 5036""""'CO, 5087 -CO, 5095-CO, and 7789-

CO. Nearly all of these specimens are disarticulated 

and are partially to extensively br·oken. Three Millersburg specimens were collected from USGS loc. 

7051-CO. 

Types.-Holotype, USNM 208667 (pl. 4, figs. 24-

26), from the Devils Hollow Member of the Lexington Limestone, USGS loc. 5095-CO; length 20.7 mm; 

width 25.0 mm; and thickness 16.8 mm. Paratype, 

USNM 208668 (pl. 4, figs. 28-30), from USGS loc. 

5095-CO i length 22.0 mm; width 30.0 mm; and 

thickness 16.7 mm. Paratype, USNM 208666 (pl. 

4, figs. 21-23), from USGS. loc. 5095-CO; length 

15.0 mm; width 17.3 mm; and thickness 9.5 mm. 

Paratype, USNM 208665 (pl. 4, figs. 19, 20), from 

USGS loc. 5095-CO; length 10.0 mm; width 11.7 

mm ; and thickness 5.5 mm. 

Discussion.-Foerste (1910) extended the range 

of 0. linneyi to include forms that he observed in 

the "Cynthiana Formation" of Kentucky. However, 

these older specimens now assignable to the Perryville Limestone, Devils Hollow, and Millersburg 

Members of the Lexington Limestone show greater 

variation in shell outline, ranging from a predominantly transversely subelliptical outline to subtriangular. 0. linneyi displays a more consistent subtriangular shape. Also, 0. sublinneyi is significantly 

more costate (table 3), and costate ornamentation 

on the fold and sulcus is more variable, varying 

from three to as many as ·eight on the fold and two 

to six in the sulcus. 

The ventral muscle field is characterized by elongate diductors that typically form an angular outline in fr.ont of the adjustor scars (fig. 13). Variants display rounded anterolateral margins that 

are sometimes shorter than the front margin of the 

adductor track. Two adductor scars can be differentiated in some specimens-a longer rectangular impression situated posteriorly and a smaller, oval, 

rectangular, ·Or chordate scar in front. The adjustor 

scars are typically shorter than the diductor scars, 

but gradations to the· same length are noted in occasional specimens. (Contrast fig. 13, C and E.) In 

the dorsal muscle field the anterior adductor pair 

are much smaller than the posterior scars (fig. 14). 

The cardinal process of 0. sublinneyi is especially 

variable, ranging from a low nearly indistinct ridge 

to one that is strongly elevated and thickened until 

it nearly fills the notothryial cavity between the 

hinge pla.tes. (Contrast figs. 8 and 9 of pl. 5.) The 

myophore varies from a flattened and serrated shelf 

to a bilobid structure characterized by a deep fissure 

along the shaft. Occasionally, the shaft protrudes 

upward as a thin partition dividing the myophore 

surface into two parts. 

Superfamily SYNTROPHIACEA Schucbert and Cooper 

Fa·mily CAMERELLIDAE Hall and Clarke 

Genus CAMERELLA Billings, 1859 

Camerella bella Fenton 

Plate 7, figures 23-28 

Came1·ella. bella. Fenton, 1928, p. 136, pl. 3, figs. 1-12. 

Ca.merella bella. Fenton. Cooper, 1956, p. 563, pl. 112, C, figs. 

8-15. 

Rema'rks.-Approximately 150 disarticulated 

valves, nearly all of which are partially to extensively broken, were recovered from the Camp Nelson Limestone (USGS loc. 7836-CO). The coarsely 

silicified specimens show costation that is limited 

to the anterior half of the valves, a well-defined dorsal fold and corresponding ventral sulcus, and flanks 

marked by four coarse costae. The fold originates 

between the umbo and the middle of the valve and 

becomes moderately elevated at the front margin. 

The valves are unequally convex in lateral profile. 

The brachial valve has the greater depth. Internal 

features include a small cruralium that is narrow 

and supported by a short ·septum, and a large 

spondylium that is supported by a septum reaching 

to midlength or beyond. Overall, these features conform most closely to C. bella Fenton, a species having fairly large size for the genus and partial plicate 

surface ornamentation. 

Distribution.-Cooper (1956, p. 564) recorded 

and described this spe·cies from the Plattin Group 

(Macy Formation) in Missouri and the Carters 

Limestone in Tennessee. 

Fig'tttred specimens.-USNM 208692 (pl. 7, figs. 

23, 28), from the Camp Nelson Formation, USGS 

J.oc. 7836-CO ; USNM 208693 (pl. 7, figs. 24, 27), 

from USGS loc. 7836-CO; and USNM 208694 (pl. 7, 

figs. 25, 26) from USGS loc. 7836-CO. 

Camerella sp. aff. C. immatura Cooper 

Plate 7, figures 17-20 

Camerella immatura Cooper, 1956, p. 570, pl. 110, A, figs. 1-5. 

Remarks.-Two localities in the Curdsville Limestone Member of the Lexington Limestone (USGS 

7782-CO and 7784-CO) yielded 11 poorly preserved 

specimens for study. Their small size, noncos.tate exteri·or, and outline suggest the holotype of C. immatu?·a Cooper from the Chatham Hill Formation of 

Cooper (1956) in Virginia. Cooper's holotyp·e is somewhat different in that it shows a shallow f.old and 

sulcus anteriorly and a narrowly uniplicate anterior 

commissure. The noncostate ornamentation and 

small size of the Kentucky specimens also suggest 
C16 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

A 

c 

,•. .. . .. : .. 

· ...... · 

B 

FIGURE 14.-Interior views of Orthorhynchula sublinneyi showing variations in dorsal musculature. A, 

USNM 208678A, X 4; B, USNM 208678B, X 3; C, USNM 208678C, X 3; All from the Devils Hollow 

Member of the Lexington Limestone, USGS loc. 5036-CO. Stippled outline is the actual muscle scars. 

C. nuda Cooper, but a low fold and shallow sulcus 

in that species produces a moderately long uniplication along the anterior commissure; two or 

three faint costae are developed on its flanks and 

three in the sulcus. 

Figured specimens.-USNM 208697 (pl. 7, figs. 

17-20), from the lower part of the Curdsville Limestone Member of. the Lexington Limestone, USGS 

loc. 7784-CO. 

Superfamily TRIMERELLACEA Schuchert 

Genus ELLIPTOGLOSSA Cooper, 1956 

Elliptoglossa? sp. 

Plate 7, figures 5-8 

Remarks.-Two USGS localities (D1200-CO and 

7805-CO) from the Tanglewood Limestone Member 

of the Lexington Limestone yielded several fragments of an inarticulate brachiopod. According to 

G. A. Cooper (written commun., 1974) the inarticu-
MIDDLE AND LATE ORDOVICIAN BRACHIOPODS C17 

late appears to be his genus Elliptoglossa. The surface ornamentation and shape suggest species of that 

genus, but the assignment is only tentative because 

the muscle scar patterns are different. It does not 

have the muscle platforms of Lingulops but otherwise the interiors are similar. 

FiguTed specimens.-USNM 208686 (pl. 7, figs. 

5, 7) from the Tanglewood Limestone Member of 

the Lexington Limestone, USGS loc. D1200-CO and 

USNM 208687 and 208688 (pl. 7, figs. 6, 8) , two interior views, from the Lexington Limestone, USGS 

loc. 7805-CO. 

Superfamily ATRYPACEA Schuchert 

Family ATRYPIDAE Gill 

Genus ZYGOSPlRA Hall, 1862 

Zygospira 1 sp. 

Plate 7, figures 13-16 

Renw?·lcs.-A single well-preserved specimen of 

Zugosp1:1·a? sp. was found in a Lexington Limestone 

collection from USGS locality 5015-CO. Its small 

size, biconvex profile, costation, and rostrate pedicle 

beak are suggestive of the genus Zygospira, but its 

outline and shape cannot ·be compared with any 

known species of that genus. 

The flanks of both valves are moderately inflated. 

The outline is subovate with the length being greater 

than the width. The valves are moderately bioonvex 

in lateral profile displaying the maximum depth at 

midlength. Surface ornamentation consists of 13 

costae on both ventral and dorsal valves. 

Figu1·ed specimen.-USNM 208685 (pl. 7, figs. 

13-16), from the Perryville Limestone Me·mber of 

the Lexington Limestone, USGS loc. 5015-CO; length 

5.0 mm, width 6.4 mm, and thickness 4.7 mm. 

REFERENCES CITED 

Alberstadt, L. P., 1973, Articulate brachiopQds of the Viola 

Formation (Ordovician) in the Arbuckle Mountains, 

Oklahoma: Oklahoma Geol. Survey Bull. 117, 90 p. 

9 pls. 

Bassler, R. S., 1932, The stratigraphy of the Central Basin 

of Tennessee: Tennessee Div. Geology, Bull. 38, 268 p., 

49 pis. 

Caster, K. E., Dalve, E. A., and Pope, J. K., 1961, Elementary guide to the fossils of the Ordovician in the vicinity 

of Cincinnati, Ohio (a revision of the elementary guide 

to the fossils and strata in the vicinity of Cincinnati, by 

Bucher, Caste1·, and Jones, 1939, 1945, 1955): Cincinnati Mus. Nat. History, 47 p., 8 pls. 

Conrad, T. A., 1842, Descriptions of new species of organic 

remains belonging to the Silurian, Devonian, and Carboniferous Systems of the United States: Acad. Nat. 

Sci. Philadelphia Jour., v. 8, pt. 2, p. 235-279, pis. 12-17. 

Cooper, G. A., 1944, Phylum Brachiopoda, in Shimer, H. W., 

and Shrock, R. R., Index fossils of North America: 

New York, John Wiley and Sons, p. 277-365, pls. 105-

143. 

---1956, Chazyan and related brachiopods: Smithsonian 

Misc. Colin., v. 127 (2 parts), 1245 p., 269 pls. 

Fenton, C. L., 1928, The stratigraphy and larger fossils of 

the Plattin Formation in Ste. Genevieve County, Missouri: Am. Midland Naturalist, v. 11, p. 125-143. 

Fenton, C. L., and Fenton, M. L., 1924, Some Black River 

brachiopods from the Mississippi Valley: Iowa Acad. 

Sci. Proc. 1922, v. 29, p. 67-77, 2 pls. 

Foerste, A. F., 1909a, Preliminary notes on Cincinnatian 

fossils: Denison Univ. Sci. Lab. Bull., v. 14, p. 209-232, 

pl. 7. 

---1909b, Preliminary notes on Cinc·innatian and Lexington fossils: Denison Univ. Sci. Lab. Bull., v. 14, p. 

289-334, pls. 7-11. 

---1910, Preliminary notes on Cincinnatian and Lexing·-

ton fossils of Ohio, Indiana, Kentucky, and Tennessee: 

Dension Univ. Sci. Lab. Bull., v. 16, p. 17-100, pls. 1-6. 

---1912, Strophomena and other fossils from Cincinnatian and Mohawkian horizons, chiefly in Ohio, Indiana, 

and Kentucky: Denison Univ. Sci. Lab. Bull., v. 17, p. 

17-173, pls. 1-18. 

Hall, James, 1847, Descriptions of the organic remains of 

the lower division of the New York System: Paleontology of New York, v. 1, 338 p., 87 pls. 

---1860, Contributions to paleontology, 1858 and 1859, 

with additions in 1860: New York State Cabinet Nat. 

History Ann. Rept. 13, p. 55-128. 

---1862, Observations upon a new genus of Brachiopoda: 

New York State Cabinent Nat. Hitstory, Ann. Rept. 15, 

p. 154-155, figs. 1-2. 

Hall, James, and Clarke, J. M., 1894a, An introduction to 

the study of the Brachiopoda, intended as a handbook 

for the use of students, Pt. 2: New York State Geologist 

Ann. Rept. 13, p. 749-1015. 

---1893, 1894b, An introduction to the study of the 

genera of Paleozoic Brachiopoda: New York Geol. Survey, Paleontology of New York, v. 8, pt. 1 (1893), 367 

p.; pt. 2 (1894)' 394 p. 

Howe. H. J., 1965, Morphology of the brachiopod genera 

Rhynchotrcma, Hypsiptycha, and Lepidocyclus: Jour. 

Paleontology, v. 39, no. 6, p. 1125-1128, pl. 134. 

---1966, The brachiopod genus Lepidocyclus from the 

Cape (Fernvale) Limestone (Ordovician) of Oklahoma 

and Missouri: Jour. Paleontology, v. 40, no. 2, p. 258-

268, pl. 31. 

---1969, Rhynchonellacean brachiopods from the Richmondian of Tennessee: Jour. Paleontology, v. 43, no. 6, 

p. 1331-1350, pls. 155-156. 

---1972, Morphology of the brachiopod genus Thaerodonta: Jour. Paleontology, v. 46, p. 440-446, pls. 1-3. 

Imbrie, John, 1956, Biometrical methods in the study of 

invertebrate fossils: Am. Mus. Nat. History Bull., v. 

108. art. 2, p. 211-252, 10 text-figs. 

James, U. P., 1881, Contributions to paleontology-Fossils of 

the Lower Silurian formation, Ohio, Indiana, and Kentucky: Paleontologist, no. 5, p. 33-44. 

Jones, 0. T., 1928, Plectambonites and •some allied genera: 

Great Britain, Geol. Survey, Mem. Palaeont., v. 1, pt. 

5, p. 367-527, 5 pis. 

Macomber, R. W., 1970, Articulate brachiopods from the 

Upper Bighorn Formation (Late Ordovician) of Wyoming: Jour. Paleontology, v. 44, p. 416-450. 
C18 CONTRIBUTIONS TO ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Mather, K. F., 1917, The Trenton fauna of Wolfe Island, 

Ontario: Ottawa Naturalist, v. 31, p. 33-40, pl. 1. 

Meek, F. B., 1873, Descriptions of invertebrate fossils of the 

Silurian and Devonian System: Ohio Geol. Survey, 

Paleontology, v. 1, pt. 1, 245 p., pls. 1-23. 

Miller, A. M., 1913, Geology of the Georgetown quadrangle, 

Kentucky: Kentucky Geol. Survey, 4th ser., v. 1, p. 

317-351. 

Miller, S. A., 1875, Monograph of the Class Brachiopoda of 

the Cincinnati Group: Cincinnati Quart. Jour. Sci., v. 

2, no. 1, p. 6-62, figs. 6, 7. 

Nettleroth, Henry, 1889, Kentucky fossil shells: a monograph of the fossil shells of the Silurian and Devonian 

rocks of Kentucky: Kentucky Geol. Survey, 245 p., 36 

pis. · 

Schmidt, Herta, 1965, Rhynchotrematidae in Williams, 

Alwyn, and others, Treatise on invertebrate paleontology, part H, Brachiopoda: New York and Lawrence, 

Kans., Geol. Soc. America and Univ. Kansas Press, p. 

H552-H597. 

Schuchert, Charles, and Cooper, G. A., 1932, Brachiopod 

genera of the suborders Orthoidea and Pentameroidea: 

Peabody Mus. Nat. History Mem., v. 4, pt. 1, 270 p., 29 

pis. 

Ulrich, E. 0., and Cooper, G. A., 1942, New genera of Ordovician brachiopods: Jour. Paleontology, v. 16, p. 620-

626, pl. 90. 

Wang, Y., 1949, Maquoketa Brachiopoda of Iowa: Geol. Soc. 

America Mem. 42, 55 p., 12 pis. 

Whitfield, R. P., 1882, Species from the shales of the Hudson 

River Group: Wisconsin Geol. Survey, Geology of Wisconsin, v. 4, p. 248-266. 

Wilson, C. W., Jr., 1948, The geology of Nashville, Tennessee: Tennessee Div. Geology Bull. 53, 172 p., 29 pls. 

---1949, Pre-Chattanooga stratigraphy in central Tennessee: Tennessee Div. Geology Bull. 56, 28 pls. 

Winchell, N. H., and Schuchert, Charles, 1895, The lower 

Silurian Brachiopoda of Minnesota: Minnesota Geol. 

Survey, Final Rept., v. 3, pt. 1, p. 333-474, pis. 29-34. 
PLATES 1-7 

Contact photographs of the plates in this report are available, at cost, from U.S. 

Geological Survey Library, Federal Center, Denver, Colorado 80225 
PLATE 1 

[All figures X 3 except fig. 20, X 4] 

FIGURES 1-5. Sowerbyella grierensis Howe, n. sp. (p. C3). 

From the Grier Limestone Member of Lexington Limestone; USGS loc. 4956-CO. 

1. Interior of brachial valve, paratype, USNM 208589. 

2. Interior of pedicle valve, paratype, USNM 208590. 

3. Exterior view of brachial valve, paratype, USNM 208591. 

4. Exterior view of pedicle valve, holotype, USNM 208592. 

5. Interior of brachial valve, paratype, USNM 208593. 

6-16. Sowerbyella curdsvillensis (Foerste) (p. C1). 

From the Curdsville Limestone Member of the Lexington Limestone. 

6, 7. Exteriors of two brachial valves, USNM 208575, USNM 208576, respectively, from USGS loc. 

5081-CO. 

8. Exterior of pedicle valve USNM 208577; USGS loc. 4124-CO. 

9, 10. Two brachial valves, U~- _ 208578, 208579, respectively; USGS loc. 4124-CO. 

11. Interior of brachial valve, USNM 208580; USGS loc. 4124-CO. 

12. Interior of pedicle valve, showing deeply incised adductor scars; USNM 208581; USGS loc. 

4124-CO. 

13. Dorsal interior of juvenile, showing papillose ornamentation; USNM 208582; USGS loc. 4124-

CO. 

14. Ventral interior showing musculature; USNM 208583; USGS loc. 4124-CO. 

15. Interior of brachial valve, displaying cardinalia; USNM 208584; USGS loc. 4122-CO. 

16. Brachial interior, USNM 208585; USGS loc. 4124-CO. 

17-20. Sowerbyella rugosa (Meek) (p. C3). 

17. Dorsal interior, displaying slightly elevated lateral septa in muscle field; USNM 208596; from 

Kope Formation, USGS loc. 7978-CO. 

18, 19. Ventral and dorsal views, respectively, of complete specimen, showing lamellose ornamentation; 

from Kope Formation, USGS loc. 7978-CO. USNM 208597. 

20. Interior of brachial valve, showing papillose ornamentation on cardinal flanks; USNM 170730; 

from Kope Formation, Newport Shopping Center on U.S. Highway 27, Newport, Ky. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-C PLATE I 

1 

2 3 4 

5 6 

7 

8 9 10 11 

12 13 

14 

15 

16 17 

18 19 

20 

SOWERBYELLA 
PLATE 2 

FIGURES 1-13. Sowerbyella sp. (p. C3). 

From the Clays Ferry Formation. 

1. Interior of brachial valve, X 3, USNM 208600, USGS loc. 5058-CO. 

2, 3. Interior of brachial valve, X 3, X 6, USNM 208601, USGS loc. 5058-CO. 

4. Dorsal view of complete specimen, X 3, USNM 208602, USGS loc. 4905-CO. 

From Point Pleasant Tongue of Clays Ferry Formation, USGS loc. 8068-CO. 

5, 8. External and internal views of dorsal valve, X 3, X 6, respectively, USNM 208603. Note incipient denticles on cardinal flanks. 

6, 10. External and internal views of dorsal valve, X 3, USNM 208604. 

7, 9. External and internal views of brachial valve, X 3, USNM 208605. 

11. Pedicle interior, X 3, showing incipient fossettes along hinge, USNM 208606. 

12. Brachial interior of juvenile, displaying several incipient denticles along hinge, X 3, USNM 

208607. 

13. Pedicle interior, showing rudimentary accessory teeth, X 5, USNM 208608. 

14-17. Thaerodonta clarksvillensis (Foerste) (p. C4). 

From the Bull Fork Formation, USGS loc-. D1254-CO. 

l 4. Exterior of brachial valve, X 3, USNM 208616. 

15. Enlarged view of brachial interior, displaying hinge-line denticles, X 5, USNM 208617. 

16. Pedicle interior, displaying fossettes, X 4.5, USNM 208618. 

17. Interior· of brachial valve, X 4.5, USNM 208619. Note lateral septa dividing adductor muscle 

field. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066--C PLATE 2 

1 2 

4 5 

6 7 

9 

15 

14 

SOWERBYELLA AND THAERODONTA 
PLATE 3 

FIGURES 1-30. Rhynchotrema increbescens (Hall) (p. C5). 

All figures from the Perryville Limestone Member of the Lexington Limestone, USGS loc. 5015-CO, unless noted. 

1-4. Dorsal, ventral, side, and end views, X 2.5, of young adult, USNM 208623. 

5, 6, 11, 12. Dorsal view1s of early growth series, X 3, USNM 208624-208627, respectively. 

7-10. Dorsal, ventral, side, and end views, X 2.5, of young adult, USNM 208628. 

13-17. Dorsal, ventral, side, end, and top views, X 2.25, of subtriangular form, USNM 208629. 

18. Brachial view of subellipital member, X 2.25, USNM 208630. 

19. Brachial view, X 2.25, USNM 208631. 

20. Ventral interior of juvenile, showing dental plates, x 2.25, USNM 208632. 

21. Ventral interior of late juvenile, X 3, showing large open delthyrium and rudimentary interarea, USNM 208633. 

22. Ventral interior, displaying quadrate muscle field, X 3, USNM 208634. 

23. Ventral interior, showing flabellate muscle field, X 3, USNM 208635a. 

24. Ventral interior, displaying dental plates, X 3, USNM 208635c. 

25. Enlarged view of ventral interior, x 4.5, showing rudimentary deltidial plates, USNM 

208637. 

26. Enlarged view of ventral interior, X 4.5, showing dental plates supporting delthyrial 

opening, USNM 208638. 

27, 30. Two dorsal interiors, X 3, USNM 208639, 208640, from the Tanglewood Limestone Member of the Lexington Limestone, USGS loc. 5016-CO. 

28. Interior of brachial valve, showing cardinalia, X 4.5, USNM 208641. 

29. Brachial interior, X 3, USNM 208642. Contrast thin cardinal septum with swollen septum 

of figure 30. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-C PLATE 3 

1 3 2 

4 6 

7 8 

10 11 12 

13 14 15 16 17 

18 20 21 22 

23 24 

27 28 29 30 

RHYNCHOTREMA 
PLATE 4 

[All figures X 1.5] 

FIGURES 1-10. Lepidocyclus? capax (Conrad) (p. C8). 

1, 2, 5. Dorsal, ventral and side views, from the Bull Fork Formation, USNM 208649, USGS loc. 

D1259-CO. 

3, 4. Ventral and dorsal views of young adult, USNM 208650, from Dillsboro Formation, USGS 

loc. 6139-CO. 

6, 10. Pedicle interior and side view of globose specimen, USNM 208654, 208655, respectively, from 

Richmond ian outcrop along U.S. Highwy 50, 3.1 miles east of Versailles, Ind. 

7-9. Two dorsal interiors and a pedicle interior, USNM 208651, 208652, 208653, respectively, from 

Dillsboro Formation, USGS loc. 6139-CO. 

11-18. Orthorhynchula linneyi (James) (p. C10). 

From the Calloway Creek Limestone (Maysvillian), USGS loc. 6409-CO. 

11, 12. Dorsal and side views of juvenile, USNM 208657. 

13, 14. Dorsal and end views of young adult, USNM 208658. 

15. Side view of adult, USNM 208659. 

16-18. Dorsal, end, and ventral views, respectively, of adult, USNM 208660. 

19-31. Orthorhynchula sublinneyi Howe, n. sp. (p. C13). 

From the upper part of the Devils Hollow Member of the Lexington Limestone, USGS loc. 5095-CO 

unless noted. 

19, 20. Dorsal and side views of juvenile, USNM 208665. 

21-23. Dorsal, side, and ventral views, respectively, of young adult, USNM 208666. 

24-26. Dorsal, ventral, and side views, respectively, USNM 208667. 

28-30. Dorsal, ventral, and side views, respectively, showing elliptical outline, USNM 208668. 

27, 31. Pedicle exterior and dorsal view of complete specimen, USNM 208669, 208670, respectively, from 

the Devils Hollow Member of the Lexington Limestone, USGS loc. 5036-CO. 
GEOLOGICAL SURVEY 

1· 2 

7 

12 

19 20 

21 22 

24 

3 

8 

15 

14 

23 17 

25 26 

30 

LEPIDOCYCLUS? AND ORTHORHYNCHULA 

PROFESSIONAL PAPER 1066-C PLATE 4 

4 

5 

9 10 

16 

18 

27 
PLATE 5 

FIGURES 1-6, 8-15. Ortho'rhy·Ju;h:ula sublinney·i Howe, n. sp. (p. C13). 

1, 2. Interior of brachial valve, X 3, and X 

6, respectively, USNM 208671, from the Perryville Limestone Member of the Lexington Limestone, 

USGS loc. 6916-CO. 

3. Interior of brachial valve, X 3, USNM 208677, from the Devils Hollow Member of the Lexington Limestone, USGS loc. 5036-CO. 

4, 5. Interior of brachial valve, X 3 and X 6, respectively, USNM 208672, USGS loc·. 6916-CO. 

6, 8, 9. Interiors of three dorsal valves, showing variations in cardinal process, X 6, USNM 208673, 

208674, and 208675, re.spectively, USGS loc. 6916-CO. 

10. Enlarged view of pedicle interior, X 4, USNM 208679, USGS loc. 5036-CO. 

11. Brachial interior, displaying dorsal musculature, X 3, USNM 208678, USGS loc. 5036-CO. 

12. Pedicle interior, X 3, USNM 208680, USGS loc. 5036-CO. 

13. Enlarged view of pedicle interior, showing musculature, X 4, USNM 208681, USGS loc. 5036-

CO. 

14. Interior of pedicle valve, X 3, USNM 208676, USGS loc. 6916-CO. 

15. Interior of pedicle valve, X 3, USNM 208682, USGS loc. 5036-CO. 

7. Ort/W'rhynchula linneyi (James) (p. C10). 

7. Interior of pedicle valve, showing thick adventitious deposits obscuring dental plates, x 3, 

USNM 208661, from the Calloway Creek Limestone, USGS loc. 6409-CO. 
GEOLOGICAL S RVEY 

7 

13 

2 

5 

14 

ORTHORHYN CHULA 

PROFESSIONAL PAPER 1066-C PLATE 5 

3 

6 
PLATE 6 

FIGURES 1-15. Orthorhynchula linneyi (James) (p. C10). 

From the Calloway Creek Limestone (Maysvillian), USGS loc. 6409-CO. 

1, 2. Enlarged views of ventral musculature, X 3 and X 6, respectively, USNM 208663. 

3, 6. Enlarged views of ventral musculature, X 3 and X 4, respectively, USNM 208664. 

4. Interior of pedicle valve showing quadrate muscle field, X 3, USNM 208696. 

5, 8. Enlarged views of dorsal cardinalia, X 3 and X 6, respectively, USNM 208695. 

7. View of cardinalia and notothyrial platform, X 4, USNM 208697. Note diverging c-rural plates. 

9. Oblique view of cardinalia and notothyrial platform, X 4, USNM 208698. Crural plates obscured 

by shell thickening. 

10, 11. Interior of brachial valve displaying simple bladelike cardinal process, X 6 and X 3, respectively, 

USNM 208699. 

12, 15. Dorsal interior showing bilobid cardinal process and myophore, X 6 and X 3, respectively, USNM 

208700. 

13. Brachial interior showing trilobate process, X 6, USNM 208701. 

14. Interior of brachial valve, X 6, USNM 208702. Note accessory ridges forming a quadrilobate 

myophore. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-C PLATE 6 

ORTHORHYNCHULA 
FIGURES 

PLATE 7 

1-4. Orthorhynchula linney·i (James) (p. C10). 

1-4. Brachial, pedicle, side, and end views of juvenile, x 3, USNM 208662, from the Calloway Creek 

Limestone, USGS loc. 6409-CO. 

5-8. Elliptoglossa? sp. (p. C16). 

5, 7. Interior and exterior views, X 8, USNM 208686, USGS loc. D1200-CO, from the Tanglewood 

Limestone Member of the Lexington Limestone. 

6, 8. Interior views of two valves, X 8, USNM 208687 and 208688, respectively, from USGS loc. 7805-

CO. 

9-12. Rostricellula minutct Cooper ( p. C8). 

9. Pedicle view, X 4, USNM 208691, 0.5 ft from top of the Logana Member of the Lexington 

Limestone, USGS loc. Dl196-CO. 

10-12. Side, anterior, and brachial views, X 4, USNM 208692, from the Logana Member of the Lexington Limestone, USGS loc. 5073-CO. 

13-16. Zygospira? sp. (p. C17). 

13-16. Dorsal, ventral, side and top views, X 4, USNM 208685, from the Perryville Limestone Member 

of the Lexington Limestone, USGS loc. 5015-CO. 

17-20. Ca1nerella sp. aff. C. immatura Cooper ( p. C15). 

17-20. Ventral, dorsal, side, and anterior views, X 4, USNM 208697, from the lower part of the 

Curdsville Limestone Member of the Lexington Limestone, USGS loc. 7784-CO. 

21-22. Rhynchotrema dentatum (Hall) (p. C5). 

21. Brachial valve, x 3, USNM 208689, from the Bull Fork Formation (Richmondian), USGS loc. 

D1247-CO. 

22. Brachial view of complete specimen, X 3, from the Bull Fork Formation, USGS loc. D1246-CO, 

USNM 208690. 

23-28. Camerella bella Fenton (p. C15). 

From the Camp Nelson Limestone, USGS loc. 7836-CO. 

23, 28. Exterior and interior views of pedicle valve, X 3 and X 4, Respectively, USNM 208692. 

24, 27. Exterior and interior views of brachial valve, X 3 and X 4, respectively, USNM 208693. 

25, 26. Exterior and interior views of brachial valve, X 3 and X 4, respectively, USNM 208694. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-C PLATE 7 

1 

9 

13 

15 

4 

2 3 

11 12 

10 

14 17 18 

16 20 

21 

22 

23 24 25 

26 27 28 

ORTHORHYNCHULA, ELLIPTOGLOSSA ?, ROSTRICELLULA, ZYGOSPIRA ?, CAMERELLA, 

AND RHYNCHOTREMA 

6 
Additional Trilobites from 

the Ordovician of Kentucky 

By REUBEN JAMES ROSS, JR. 

CONTRIBUTIONS 

KEN'TUCKY AND 

TO THE 

NEARBY 

ORDOVICIAN 

STATES 

PALEONTOLOGY OF 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-D 

Prepared in cooperation with the 

Com.m.onwealth of /{entuck;' 

University of Kentuck;1, 

J(entucky Geological Survey 

Species of the trilobites Triarthus, 

Decorproetus, Isotelus, Gravicalymene, 

Platylichas, Prim.asjJis, and Acidaspis, are 

described from Orvodician strata of Kentucky 

UNITED STATES GOVERNl\1ENT PRINTING OFFICE, WASHINGTON 1979 

CONTENTS 

Page 

J\bstract ---------------------------------------------------------------- D1 

Introduction ------------------------------------------------------------- 1 

J\cknowledgments -------------------------------------------------------- 1 

Descriptions of trilobites -------------------------------------------------- 2 

Olenidae ------------------------------------------------------------- 2 

Tria'rthrus Green, 1832 -------------------------------------------- 2 

Pr6etidae ------------------------------------------------------------ 3 

Decoroproetus Pribyl, 1946 ---------------------------------------- 3 

J\saphidae ----------------------------------------------------------- 5 

lsotelus DeKay, 1824 --------------------------------------------- 5 

Megalaspid ( ?) --------------------------------------------------- 5 

Encrinuridae --------------------------------------------------------- 5 

Cybelinid ______ ------ _______________ ----------- _ --- _ -------- __ -- _ 5 

Calyminidae --------------------------------------------------------- 5 

Gravicalym,ene Shi1·ley, 1936 --------------------------------------- 5 

Flexicalymene Shirley, 1936 --------------------------------------- 6 

Lichidae ------------------------------------------------------------- 7 

Platylichas Gurich, 1901 ------------------------------------------ 7 

Odontopleuridae ------------------------------------------------------ 8 

P?·intaspis Richter and Richter, 1917 ------------------------------- 8 

Acidaspis Murchison, 1839 ---------------------------------------- 11 

References cited ---------------------------------------------------------- 12 

ILLUSTRATIONS 

PLATE 1. T1·iarthrus, Isotelus, and megalaspid ( ?) . 

2. Decorop1·octus, Gravicalymene, and cybelinid. 

3. G1·avicalymene and Flexicalymene. 

4. Platylichas and Primaspis. 

5. Primaspis. 

6. Primaspis and Acidaspis. 

SYSTEM OF MEASUREMENT UNITS 

The investigations underlying this series of reports were made over a period of 

years, and distances and stratigraphic measurements appear fairly uniformly in Engli:sh units. Measurements of fossil specimens, on the other hand, follow the longstanding convention of appearing in metric units. Because of the dates of the investigations and the amount of resulting data, the English measurements have been retained. Conversions to metric units may be made by using the following conversion 

table: 

To convert 

English unit: 

Mile (mi) 

Foot (ft) 

To metric unit: 

Kilometer (km) 

Meter (m) 

Multiply 

by: 

1.61 

.305 

III 
CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

ADDITIONAL TRILOBITES FROM THE ORDOVICIAN OF KENTUCKY 

By REUBEN JAMEs Ross, JR. 

ABSTRACT 

Trilobites collected from Ordovician limestones in Kentucky supplement earlier collections reported by Ross in 

1967. Included are olenids, proetids, asaphids, calymenids, 

lichids, and odontopleurids. A remarkable specimen of · 

P'ri?na.sp'is shows traces of the ventral appendages crudely 

silicified. 

INTRODUCTION 

Preparation of large samples of Ordovician limestones from Kentucky for silicified brachiopods and 

pelecypods has also provided a limited number of 

trilobites. These 'SUpplement the few trilobites previously reported (Ross, 1967). 

The generic as~semblage of trilobites from the 

Ordovician rocks of Kentucky res-emble those of the 

Caradocian of England, Scandinavia, and to a 

lesser extent Bohemia. The genera described and 

illustrated here include TTia1·thrus, Decoroproetus, 

lsotelus, GTavicaly1nene, Flexicalymene, Platylichas, 

P·rin~aspis, and Acidaspis. 

These genera do not all occur in the sam.e ~stratigraphic units. Care should be taken to ally each 

genus and species with the stra.tigraphic interval to 

which it belongs. CoUections and localities are indicated so that the reader may refer t<?· the stratigraphic summary. 

Most collections were made under the direction 

of John Pojeta. However, two collections not made 

by U.S. Geological Survey personnel hav-e yielded 

important ma:terial. S. M. Warshauer and J. M. 

Warn of the University of Cincinnati found exceptionally fine specimens of T'tiaTthTus that are not 

silicified. A new species, GTavicalymene tntncatus, 

is represented by unsilicified specim.ens collected by 

D. M. Lorenz, of the University of California, Los 

Angeles. 

The genus Oryptolithus was found in six collections, but because only fragments of fringes were 

p~esent, no effort was made to describe or illustrate 

the ~specimens. The six collections are: 

5073 ·CO-Logana Member, Lexington Limestone-Frankfort East quadrangle. 

5092 CO-Logana Membe-r, Lexington Limestone-Tyrone quadrangle. 

7791 CO-Logana Member, Lexington Limestone-Salvisa quadrangle. 

. 7793 CO-Tanglewood Limestone Member, Lexington Limestone-Ford quadrangle. 

6211 CO-Kope Formation, lowermost bedsMoscow quadrangle. 

7806 CO-Point Pleasant T·ongue of the Clays 

Ferry Formation-Moscow quadrangle. 

Six species are given letter designations rather 

than being named formally. The two species of 

Acidaspis are represented by one cranidium and one 

pygidium each-hardly an adequate sample on 

which to base a species. The species of Deco1·op1·oetus and P1·imaspis are represented by enough specimens to indicate that they belong to four different 

species but by too few to be sure that one or more 

previously desc·ribed !Species are not synonyms. 

Museum numbers are abbreviated as follows: 

AMNH-American Museum of Natural History 

NYSM-New York State Museum 

UCM-University of Cincinnati Museum 

USNM-U.S. National Museum 

ACKNOWLEDGMENTS 

Niles Eldredge of the American Museum of 

Natural History loaned specimens of T?·ia'ttlt'rus 

becki and Primaspis tTentonensis described and 

illus:trated by James Hall (1847). Specimens on the 

basis of which Ruedemann (1926) revised Tria1·-

thrus becki and T. eatoni were furnished by Donald 

W. Fisher of the New York State Museum at Albany, who also provided the loan of specimens of 

Primaspis eatoni from the Trenton Group. 

Dl 
D2 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

DESCRIPTIONS OF TRILOBITES 

Class TRILOBITA Walch, 1771 

Order PTYCHOP.\RIIDA Swinnerton, 1915 

Superfamily OLENACEA Burmeister, 1843 

Family OLENIDAE Burmeister, 1843 

Genus TRIARTHRUS Green, 1832 

Ruedemann (1926, p. 115-121) co·mpared and revised the two co·mmon North American species 

Triarthrus becki Green and Tria1·thrus eatoni Hall 

and emphasized the stratigraphic significance of 

their taxonomic differenc·es. Examination of the 

specimens illustrated by Ruedemann (1926, pl. 21, 

figs. 7, 8, 12) and by Hall (1847, pl. 64, figs. 2b, c) 

confirms these differences. 

The specimens described herein are assigned to 

Triarthrus eatoni rather than being assigned to a 

new species. All these Kentucky specimens from the 

Kope Formation are beautifully preserved, retaining their original convexity, whereas the specimens 

available to me from the Utica Shale are flattened. 

Such differences as exi,s.t between the Utica and the 

Kope specimens are probably caused more by preservati.on than by biology. 

In describing these olenid specimens I have 

tempered the terminology of Henningsmoen (1957, 

p. 12-14) with that of Harrington, Moore, and 

Stubblefield (1959, p. 0117-0126). 

Triarthrus eatoni (Hall) 

Plate 1, figures 1-13 

Trim·th-r·us eatoni (Hall) Ruedemann, 1926, New York State 

Mus. Bull., no. 272, part 2, p. 115-121, pl. 21, figs. 7-9. 

The beautiful little specimens of Triarthrus 

eatoni collected by S.M. Warshauer and J. M. Warn 

are all enr10lled and preserve the convexity that is 

usually lost by flattening in shale. The average 

sagittal length of cephala is a little more than 3 mm. 

Cephalon is 1.5 times as wide ·as long, without 

genal angles or spines. Except a.t occipital ring, 

border is continuously subtubular, of almost uniform width, and bounded by shallow furrow. Preglabellar field lacking. Cephalic axis constitutes 0.9 

sagittal length of cephalon; glabellar length (sag) 

exceeds 0.7 length of cephalon, and length (sag) 

of occipital ring is 0.2 sagittal length of cephalic 

axis. 

Glabellar outline is bluntly rounded in front; axial 

furrows only approximately parallel because glabella is widest at lateral lobe 2p. Sagittal length of 

ce,phalic ~xis 1.1 times greatest width of glabella. 

Length 6f glabella equals 0.86 its greatest width. 

Ant,erior width (tr) of occipital ring is 0.93 greatest width of glabella. 

Posterior courses of facial sutures divergent convex; length of cranidium mpre than 0.7 width (tr) 

at posterior margin. Width ( tr) of fixigena immediately behind palpebral lobe is 0.21 greatest 

width of glabella; width of fixigena at posterior 

border equals 0.36 greatest width of glabella. Anteriorly facial sutures cross border diagonally inward meeting at median suture. 

Thorax composed of 14 segments. Like occipital 

ring, each bears· median tubercle. Axis constitutes 

slightly more than one-third thoracic width. Pleurae 

slope steeply ventrolaterally. Tip of each pleura 

blunt, flattened, with lateral projection (pl. 1, figs. 

3, 13), which produces a tight fit against doublure 

of cephalon. Pleural furrows deep, terminating 

distally at .the lateral p·roj ection. 

Pygidium small; in every specimen, border is enrolled against cephalon so that its characters are 

partly hidden. However, it seems that at least the 

front three segments of the pygidium bear the same 

lateral projections as the tips of the thoracic segments. Axis composed of four rings and minute, 

transverse terminal piece. 

Illustrated specimens.-UCM 40633a-e. 

Occurrence.-Kope Formation, 23 ft above contact with unde,rlying Point Pleasant Tongue of 

Clays F·erry Formation. North side of 12 Mile 

Creek, 75 ft east of bridge (Twelve Mile Road) 

across creek, Laurel 71/:2-minute quadrangle, Kentucky. Collected by John M. Warn and Steven M. 

Warshauer. 

Discussion.-Triarthrus parchaensis Harrington 

and Leanza asnd T. rectifrons Harrington both possess a preglabellar field discrete from anterior 

border and in both the glabella is much broader 

than in T. eatoni. T. gachalensis Harrington and 

Leanza has a much wider glabella and narrower 

cephal on. None of the Early Ordovician species from 

Argentina (Harrington and Leanza, 1957, p. 115-

119) is very similar to Triarthnts eatoni from the 

Kope Formation. Triarthrus convergens Whittard 

(1961, p. 190-191, pl. XXIV, figs. 16-18) has a 

broader glabella and acute genal angles. According to Cooper (1953, p. 9, pl. 2, figs. 7-10), T?·iarthrus (Porterfieldia) caecigenus Raymond has 

only 11 thoracic segments and 7 axial rings on the 

pygidium as well as somewhat different features of 

the cephalon. 

A comparison of the specimens from the Kope 

with those collected by Hall from the Trenton at 

Middleville, N. Y., (Hall, 1847, p. 237, pl. LXIV, 

fig. 2; Ruedemann, 1926, p. 119-121) shows not only 

that the cephalic axis is wider and shorter in the 

Trenton species but also that it bears abbreviated 
ADDITIONAL TRILOBITES FROM THE ORDOVICIAN OF KENTUCKY D3 

glabellar furrows 3p that do not intersect the dorsal 

furrows; this anterior pair of furrows is virtually 

lacking in the Kentucky specimens. In the few specimens on which furrows 3p do appear they are 

visible o·nly as faint traces-but the traces extend 

to the dorsal furrow. 

Glabellar proportions of the Kope specimens agree 

exactly with those of specimens of comparable size 

in the Columbia University collections from the 

Utica Shale of Rome, N. Y. Those specimens are 

now considered to belong to T?·iarth/rus eatoni. Such 

seeming differences as exist in proportions o.f the 

cephalon are readily explained by mode of preservation. 

Superfamily PROET ACEA Salter, 1864 

Family PROETIDAE Salter, 1864 

Genus DECOROPROETUS Pribyl, 1946 

Deco?·op?·oetus Pribyl. Owens, 1973a, Norsk Geol. Tiddskr. v. 

53, p. 134. 

Deco?'op?·oetns Pribyl. Owens, 1973b, British Ordovician and 

Silurian Proetidae (Trilobita). Palaeontographical 

Soc., pub. no. 535, p. 41. 

P·roet·idellct Bancroft. Ross, 1967, U.S. Geol. Survey Prof. 

Paper 583-B, p. B6-B7. 

Species previously assigned to P1·oetidella (Ross, 

1967) must be redesignated Decorop1·oetus following the excellent revisions of Owens (1970, 1973a, 

1973b). 

Previously Decorop1·oetus (as PToetidella) has 

been repiOrted in the Grier and Tangle!wood Limestone Members of the Lexington Lim.estone and in 

the Clays Ferry Formation. Here it is recorded 

in the Perryville Lim·estone Member of the Lexington as well as at another locality in the Clays Ferry 

Formation. 

Decoroproetus sp. x 

Plate 2, figures 1-6 

In the collection (USGS colin. 6143 CO) from the 

Clays Ferry of the Cynthiana quadrangle are 22 

partly enrolled silicified specimens of Decm·oproetus. 

All are incomplete·. Most are composed of the hypostoma, glabella, thoracic axis, and pygidial axis. 

F;our .specimens retain m·o·st of one or both librigenae, but in three others only the silicified bo·rder 

and doublure of a librigena remains. No complete 

pygidi urn remains. 

Cephalon essentially semicircular in outline if the 

genal spine's are disregarded. The spines extend 

backward as far as. the third thoracic segment. 

Glabella widest between palpebral lobes and at occipital ring; width exceeds 0.9 sagittal glabella 

length including occipital ring. The width of glabella slightly more than one-third the width of 

cephalon. Glabellar outline constricted between 

fronts of palpebral lobes and rounded at ant·erior 

end. Occipital ring a flattened band set off by distinct occipital furrow. Occipital furrow curves forward sagittally and at junction with axial furrow. 

Occipital lobes are faint swellings adjacent to the 

axial furrowrs. Length (sag) of anterior border is 

less than 0.2 glabellar length. Length (exsag) of 

eyes is 0.45 glabellar length but length (exsag) of 

slender palpebral lobes is less than 0.3 glabella.r 

length. 

Hypostoma is strongly and narrowly convex, 

widest at anterior wings; width at wings only slightly less than sagittal length. Width of middle body 

two-thirds sagittal length. Middle body indistinctly 

divided into large anterior and short (sag) lobe by 

a pair of diagonal creases rather than maculae. Behind anterior wings, subtubular border surrounds 

hypostoma and is set off by a distinct border furrow. 

The anterior edge of the hypostoma lies beneath the 

rounded front of .the glabella. The rounded posterior 

margin of the hypostoma extends to the middle of 

the occipital ring. 

There are' 10 segments in the thorax and 6 rings 

in the pygidial axis, plus a narrowly rounded terminal piece. Pleural furrows on the thorax are 

straight and extend outward from the axial furrow 

at least a.s far as the pleural lobe is flat; all tips of 

pleurae are br10ken. 

The outlines of three pygidia are crudely indicated by partial silicification of border and doublure, 

but not a single specimen retains the pleural field. 

The outline s·eems to be broadly parabolic and about 

2.1/2 times as wide (tr) ·as long (sag). Length of 

axis is 0.85 length (sag) of pygidium. 

IllustTated specintens.-USNM 206836, 206837. 

Occu?Tence.-USGS collection 6143 CO, Upper 

tongue of Clays Ferry, 30-35 ft above base of section, roadcut on east side of Kentucky Highways 32 

and 36, Cynthiana quadrangle, Kentucky. 

Discussion.___.:Comparison with previously described species is hampered by the erratic nature of 

silicification. Such features as are preserved are 

similar to those of DecoTopToetus feaTnsidesi (Bancroft) from lower Caradocian of Shropshire, as described by Dean (1963, p·. 243-246) ; the glabellar 

outline, occipital lobes, dimensions of the preglabellar field, and outline of the pygidi urn are similar 

to those .of the English species, but definition of the 

anterior border is poorer than in D. fea?-nsidesi. 

D. subornatus (Cooper and Kindle, 1936, p. 364-

365, pl. 42, figs. 16, 24) is bas·ed on a pygidium and 
D4 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

fragmentary cranidium; reasonable comparison cannot be made with that species from Quebec. 

Decoroproetus marri Dean (1962, p. 124-126, pl. 

17, figs. 5, 8) possesses a more bluntly rounded 

glabellar outline, a longer (sag) pregl·abellar field, 

and a more prominent and narrower anterior borde'r 

than the Kentucky specimens. Owens (1973b, p. 44-

45) placed D. marri in synonymy with D. calvus 

(Whittard). Illustrations of the type and other 

specimens of D. calvus (Owens, 1973b, pl. 8, figs. 1a, 

1b, 7) show that the preglabellar field is more convex (sigmoidal) in sagittal profile than in the specimens from Kentucky. 

Owens ( 1973a., tahle 3) summarized the diagnostic features of Scandinavian sp·ecies of Decoroproetus. Inasmuch as D. sp. x possesses a constricted 

glabellar outline, lacks gl·abellar furrows, and has a 

straight longitudinal profile of the· preglabellar field, 

it is best c-ompared with D. gyratus Owens (1970, 

p. 316, 319-20, fig. 6A, B, D). The Scandinavian 

species has a longer ('sag) preglabellar field and a 

less well defined border. 

Decoroproetus sp. x differs from all British species (Owens, 1973b) with unfurrowed glabellae in 

having a flat rather than S'igmoidal (sag) preglabellar field, a distinct flat-topped border defined 

proximally by a break in slope, narrowly rounded 

frontal lohe :of glabella, and gentle constriction of 

the glabella. 

Decoroproetus has al1so been described from the 

"Confinis" Flags (Tripp, 1962, p. 13, pl. II, fig. 15) 

and from .the Upper Stinchar Limestone (Tripp, 

1967, p. 52-53, pl. II, figs. 13-17) of the Girvan 

District, southwest Scotland. The specimens from 

the "Confinis" Flags. are too incomplete· fo.r comparison; both of the two species from the Upper 

Stinchar Lim.estone have a much longer (sag) preglabellar field and one has a longer (~sag) pygidial 

axis than the species from the Clays Ferry. The two 

Scottish formations were correla,ted by Williams 

(1962, p. 58-62) with the Porterfieldian of Cooper. 

In Kentucky, a few specimens of Decoroproetus 

(under the name of Proetidella) were reported and 

illustrated (Ross, 1967, p. B6-B7) from the Lexingt.on Limestone and the Clays Ferry Formation. 

The cranidium from the Millersburg Member of the 

Lexington Limestone (P. sp. 3, Ross, 1967, pl. 2, 

fig. 15) may be conspecific with the species .described he·re, but none of the pygidia can be compared with the present incomplete material. 

Decoroproetus sp. 2 

Plate 2, figures 7-16 

Proetidella sp. 2. Ross, 1967, U.S. Geol. Survey Prof. Paper 

583-B, p. B7, pl. 2, fig. 14. 

Four fragments of cranidia included in sample, 

three of which are only the pregla.bellar field and 

border; the fourth is only the posterior third of a 

glabella. Nine librigenae are fairly well preserved. 

No hypos tom a is. confidently assigned to this species. 

Of the 1six pygidia only two are worthy of ill ustration. 

Librigenae bear long (ex sag) eyes above smooth 

surface that slopes gently to anterior border furrow. 

Narrow anterior border gently convex. Anterior and 

posterior border furrows intersect at acute angle 

·and continue as single furrow onto dorsal surface 

of genal spine. 

Pygidium broadly parabolic in outline, its length 

(sag) equaling 0.62 its width ( tr) . Axis robust, 

tapering, bluntly rounded at po,sterior end. Length 

of axis approximately 0.8 length (sag) of pygidium; 

anterior width (tr) of axis about 0.4 greatest pygidial width (tr). Axis composed of seven rings and 

terminal piece in largest specimen (pl. 2, figs. 7-9) 

but of six rings plus terminal piece in a slightly 

smaller pygidium (pl. 2, figs. 10-12). Axial furrow 

distinct but shallowing at confluence around end of 

axi1s. Three pairs of interpleural furrows almost 

reach margin, but only the anterior two pairs are 

readily discernible. Six pairs of pleural furrows 

traverse pleural fie·ld to approach margin but 

posterior two pairs. very faint. Discrete border and 

border furrow lacking; pleural regi.on distally concave im.mediately inside the margin. 

Occurrence.-USGS collection 5015 CO, Perryville 

Limestone Member of Lexington Limestone, 5 ft 

above base of Salvisa Bed. In quarry 0.4 mi .south 

of Perryville. Kentucky coo·rdinates, north zone: 

E. 2,232,250 ft, N. 478,400 ft. Perryville quadrangle, 

Kentucky. 

Illustrated specimens.-USNM 206838-206841 inclusive. 

Discussion.-The difference in number of axial 

rings on the two· illustrated pygidia might be considered the basis for distinguishing two species. 

Without a larger :sample, no measure of variability 

is practical. In other respects the pygidia seem most 

similar to that designat;ed as Prroetidella sp. 2 (Ross, 

1967, p. B7, pl. 2, fig. 14) fro'm the Tanglewood 

Limest.one Member o.f the Lexington Limestone in 

the Switzer quadrangle, Kentucky. It is unfortunately impossible to· make a meaningful comparison 

with the pygidia of Decoroproetus sp. x described 

here. 
ADDITIONAL TRILOBITES FROM THE ORDOVICIAN OF KENTUCKY D5 

Superfamily ASAPHACEA Burmeister, 1843 

Family ASAPHIDAE Burmeister, 1843 

Subfamily ISOTELINAE Angelin, 1854 

Genus ISOTELUS DeKay, 1824 

No genus is more widely represented in the collections from Kentucky than lsotelus. Unfortunately, only fragments remain in the great majority .. of 

the collec.tions, making identification as to species 

impossible. The genus is present in 22 collections. 

These are 6139 CO, 6145 CO, 6146 CO, 6412 CO, 

6414 co, 6418 co, 7458 co, 6909 co, 6916 co, 

6915 co, 7471 co, 7079 co, 7454 co, 7834 co, 

6136 CO, 5067 CO, 6417 CO, 7 456 CO, 7 457 CO, 

7 448 CO, 4852 CO, 7792 CO and 5015 CO. The best 

silicified preservation is in collection 5015 CO; this 

collection also sho·wed the best silicification of a 

group of collections treated in a previous study 

(Ross, 1967). 

lsotelus gigas DeKay 

Plate 1, figures 14, 15 

Isotelus gigas DeKay. Ross, 1967, U.S. Geol. Survey Prof. 

Paper 583-B, p. B3, B6, pl. 1. pl. 2, figs. 1-4. 

Henningsmoen (1975, p. 196, fig. 13) in a review 

of methods of trilobite ecdysis reported the dis~ 

co ve-ry of a specimen of I sotelus in which the· median 

suture between the librigenae was obsolete; his 

specimen was from the Trenton Group of New 

York. 

In the material from USGS collection 5015 CO 

prepared since 1966 are two e·xamples of lihrigenae 

yoked together (pl. 1, figs. 14, 15). In both, the 

median suture is merely a slit extending 5 mm back 

from the front margin; otherwise the doublure is 

continuous. Specimens &mailer than these two have 

librigenae separated by the median suture·. Probably, 

when the ·animal reached such a size that the cepha.-

lon was approximately 60 mm long, it was able to 

withdraw from its carapace without splitting the 

cheeks apart. 

1llust1·ated specimens.-USNM 206844, 206845. 

Megalaspid(?) pygidium 

Plate 1, figures 16-18 

A single pygidium without as,sociated cephalic 

parts ha:s been collec.ted from the Camp Nelson 

Limestone. Asaphid pygidi~a of this generalized 

type are almost impossible to identify as to genus 

wi.thout supporting information. This spedmen may 

belong to a megalaspid. Future collectors may discov-er the needed cephalic evidence. 

Illust1·ated specimen.-USNM 206846. 

Occun·ence.-Camp Nelson Limestone, USGS collection 7875 CO, Wilmore quadrangle, Kentucky. 

Order PHACOPIDA Salter, 1864 

Family ENCRINURIDAE Angelin, 1854 

Cybelinid cranidium 

Plate 2, figure 20 

A fragmentary cr,anidi urn, possibly belonging to· 

the genus PaTacybeloides, is illustrated as a matter 

of record. The specimen is a silicified cast of the 

ventral side of the carapace. No cybelinid pygidium 

was found associated. 

IllustTated specimen.-USNM 206842. 

OccurTence.-USGS collection 6419 CO, lower 

part of Logana Member of Lexington Limestone, 

Wilmore quadrangle, Kentucky. 

Family CALYMENIDAE Burmeister 

Genus GRA VI CAL YMENE Shirley 1936 

The importance of the genus G1·avicalymene in the 

Middle Ordovician of Kentucky has been reviewed 

by Ros;s (1967, p. B8-B9). Collection 7984 CO includes a sp·ecies assigned to Gravicalymene; however, it is so distinctive that it might be .the basis 

of a new genus or might be .assigned to· Diacalymene. 

The lateral glabellar lobes 3p are very small. The 

front of the glabella is transversely rectilinear; 

the width (,tr) at the front is at least as wide as 

the width of the glabella at lobes 3p. The preglabellar furrow is extremely deep and undercuts the 

front of the glabella. The anterior border is flat 

topped and has the kind of lateral profile associated 

by Shirley (1936, fig. 2; pl. XXIX, figs. 19-23 with 

Diacalymene. I have found no description of a species wi:th .the trunc;ated anterior glabella. 

The thickness of the carapace suggests that comparison with internal casts could be very difficult 

and misl,eading. 

A correction in my previous interpretation of 

pygidial segmentation (Ross, 1967, p. B9) is· in 

order. In all species of Gravicalymene described 

from Kentucky-including G. truncatus n. sp.-the 

first four ring:s of the pygidial axis are distinct. On 

the pleural regions there are five pairs. of pleural 

furrows but only four pairs of interpleural furro·ws. 

Because the fundamental segmentation of the 

pygidium is shown by the interpleural furrows 

(Harrington, 1959, p. 073), the front four rings 

should be considered axial rings. The terminal piece 

therefore bears two faint furrows and in some specimens an indistinct dimple. The fifth pleural furrow belongs to the front faint ring in the terminal 

piece. 

Gravicalymene hagani Ross 

Plate ~. figures 18, 19; plate 3, figures 1-9 

Gravicalymene hagani Ross, 1967, U.S. Geol. Survey Prof. 

Paper 583-B, p. B9-B10, pl. 3, figs. 1-12. 
D6 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

In the new material for USGS collection 5015 CO 

many beautifully silicified parts of Gravicalyn1-ene 

hagani are preserved. Four cranidia of different 

sizes, 'a hypos.toma, and the tip of a thoracic segment are illustrarted partly as a matter of record 

and partly to suppl,ement the previous description. 

· Hypostoma typical for the family Calymenidae. 

The specimen illustrated in plate 3, :figure 5 shows 

the anterior downward flexure to fit the rostral plate 

along the connective suture and the deep elongate 

pits on the ventral surface that correspond to the 

anterior wing processes on the inner dorsal side. 

The middle body is 1.5 times as long as wide. Length 

(sag) of anterior lobe about 0.70 length of middle 

body. 

Left side of a thoracic segment is illustrated to 

show the smooth facet on the outside and the vincular stop on the front ~edge near the tip. 

The insides of two cranidia show the fossular 

apodemes (pl. 3, figs. 4, 9). In larger, possibly 

gerontic, specimens the fossula seems to extend so 

dee.ply into the apodeme that ~a canal is present into 

the inner side of the integumen. Tliis feature may 

be the result of some vagary of silicification or 

maybe an o~riginal feature; if the latter, it would indicate a connection with the dorsal surface for purposes about which we can only speeulate. 

Illustrated specimens.-USNM 206847-206852 

inclusive. 

Occurrence.-Perryville Limestone Me m b e r , 

Lexington Limestone, USGS collection 5015 CO. 

Gravicalymene truncatus n. sp. 

Plate 3, figures 11-20 

This species is characterized by the transversely 

truncated anterior end of the glabella, small lateral 

lobes 3p, and deep preglabellar furrow. Outline of 

glabella would be bellshaped if anterior end were 

not truncated. 

The cephalon approximately semicircular in outline and its height only slightly less than its sagittal 

length. Length (sag) of glabella including occipital 

ring almost 0.75 }ength of cranidium. Length (sag) 

of occipital ring equals 0.2 length of glabella including ring. Width (tr) at frontal lobe equals width 

at lateral lobes 3p and 0.6 width (tr) at lobes 1p. 

Greates.t width of glabella at lobes 1p equals 1.0-

1.2 times glabellar length including occipital ring. 

· Palpebral lobes cenbered opposite glabellar lobes 

2p. Width ( tr) of fixed cheeks at palpebral lobes 

only 0.4 width of glabella at lobes 2p. 

Anterior border elevated, higher than 'wide (sag). 

Dorsal surface somewhat flattened and sloping 

1 backward. Anterior face of margin steeply inclined 

I 

downward and backward. Border furrow extremely deep; in one specimen undercutting front of 

glabella, in another vertically sided. Furrow widest 

sagittally. Combined width (sag) of border and 

border furrow equals 0.25 length of glabella including occipital ring. 

Length (exsag) of lateral lobes 3p only 0.09 length 

(sag) of glabella including occipital ring. 

Hypostoma not known. 

Thorax compos~ed of 13 segments of which the 

tips are flattened and rounded from front to back. 

The pygidium strongly convex of a generalized 

design common to all Kentucky species of Gravicalymene. Sagittal l1

ength -of pygidium equals 0.6 

its greatest width. Length of axis 0.9 pygidial length 

and 0.75 its own width (tr). Width of axis (tr) 

about 0.4 width of pygidium. Axis consists of four 

well-defined anterior rings and terminal piece; terminal piece takes up almost half the sagittal length 

of axis. T:erminal piece bears two faint transverse 

furrows delimiting two weak rings. A small median 

dimple may be present on some specimens in the 

back half of the terminal piece. Five pairs of pleural 

furrows but only four pairs of interpleural furrows 

pf'esent in pleural regions. 

Illustrated specimens.-USNM 206853-206855 inclusive. 

Occurrence.-USGS collection 7984 CO, Kope Formation, 57 ft 1 in. above Point Pleasant-Rope 

contact, Moffett Road s-ection, Demossville quadrangle, Kentucky. 

Discussion.-Although the glabella of a sp~ecies 

like Gravicalymene praecox (Bancroft) may be no 

wider (tr) at the frontal lobe than at lobes 3p, in 

no species described to date is the front of the glabella so abruptly tierminated. One is inclined to think 

the specimen deformed until he find others that are 

similar. The anterior truncation of the glabella, 

smallness of glabellar lobes 3p, enormously high anterior border, and deep border furrow distinguish 

this species. 

Genus FLEXICALYMENE Shirley, 1936 

Flexicalymene sp. 

Plate 3, figure 10 

A single fragmentary cranidium in the new collections is assignable to Flexicalymene. It is illustrated as a. matter of record. 

Illustrated specimen.-USNM 206856. 

Occurrence.-Gilbert Member of Ashlock Formation, USGS Collection 6129 CO. 
ADDITIONAL TRILOBITES FROM THE ORDOVICIAN OF KENTUCKY D7 

Order LICHIDA Moore 

Family LICHIDA[ Hawle and Corda, 1847 

Subfamily HOMOLICHINAE Phleger 

Genus PLATYLICHAS Gurich, 1901 

Because a pygidium is lacking, .the assignment of 

specimens described here to a genus is uncertain. 

However, the ass_ociation of a fragmentary hypostom.e with the middl1

e body wider than long and 

bounded posteriorly by a furrow rules out assignment to Lichas as shown by Tripp (1957, fig. 4). 

The posterior courses of longitudinal and axial fur~ 

rows are similar to those -of Platylichas halli 

( Foerste) from the Cincinnatian of Ohio and of 

Platylichas laxatus (McCoy) as illustrated by Warburg (1939, pl. 12, figs. 2, 3, 5, 6, 10), from the 

Chasnwps beds. The axial furrow runs almost 

straight from the front of the palpebral lobe to the 

inner end of the occipital lobe; the posterior 

"hooked" end of the longitudinal furrow is connected by a short, shallow furrow to the axial and 

occipital furrows also at the inner end of the occipital lobe. 

A case might be made for assigning this species 

to Metopolichas, but in all illustrations of M. hubnwri 

(Eichwald) (the type species) and M. ven·ucosus 

Eichwald the axial furrow is shown interse.cting the 

occipital furrow on the outer side of the occipital 

lobe, and no connecting furrow from the ~end of the 

longitudinal furrow is present. 

As noted by Tripp (1957, p. 116) a theoretical 

evolutionary sequence was. proposed for Platylichas 

by Opik (1937, p. 55-62) involving in particular 

migration of the posterior end of the axial furrow. 

The Kentucky sp1ecimens represent an early step in 

Opik's scheme. 

PlatyUchas is present in Caradocian deposits 

(Yugorskiy horizon) of southern Vaigach Island 

and northern Pay-Khoy peninsula north of the Urals 

(Bondarev and others, 1968). The genus is reported 

by Jaanusson (1964, p. 30) from the Caradocian 

(Viruan) Skagen Formation of Vastergotland, 

Sweden. Platylichas is also to be found in the Caradocian :strata of Lithuania (Modlinski, 1967). In 

Wales it is reported from Caradocian and Ashgillian 

strata (Whittington, 1962). Lesperance (1968) has 

recorded Platylichas at Perce, Quebec, from beds of 

either Caradocian or Ashgillian age. 

Platylichas halli (Foerste) 

Plate 4, figures 1-7 

Liclws halli Foerste, 1888, Denison Univ. Sci. Lab. Bull., v. 

3, p. 118-120, pl. XIII, fig. 4. 

This species is represented by six fragmentary 

cranidia and one p·artial hypostoma. 

I 

Greatest width of glabella positioned .slightly 

posterior to anterior pits, although width at the occipita1 ring is essentially its equal. Glabella is narrowest immediately in front of occioital furrow· 

there its width (tr) is less than hal:f the greatest 

width. At its intersection with the occipital furrow 

each axial furrow is essentially tangent to the inner 

end of the occipital lobe; each axial furrow runs 

forward and outward in a nearly straight course to 

the front of the palpebral furrow; it then curves 

inward and downward to the anterior pit. From the 

anterior pit each longitudinal furrow continues the 

course of the axial furrow, curves inward and backward. At a distance in front of the occipital furrow 

equal to one-eighth the sagittal glabellar length each 

longitudinal furrow curves abruptly outward to assume a "hooked" course. The length (ex sag) of 

composite lateral lobes thus defined is approximately six-tenths the sagittal glabellar length. Composite 

lobes moderately inflated. Frontal and median lobes 

less inflated than composite lobe·s. Frontal lobe slopes 

evenly forward to very narrow (sag) border. On a 

transverse line through the greatest width of glabella the width of median lobe is slightly more than 

half the width of each composite lobe. 

I 

The hooked posterior end of each longitudinal 

. furrow is connected by a short, shallow furrow to 

the intersection of axial and occipital furrows. Occipital lobes lie entirely outside this intersec.tion ; the 

distance (tr) between inner ends of occipital lobes 

is a little less than half the width ( tr) of the glabella at the occip-ital ring. The length (exsag) of 

arcuate palpebral lobe between one-fourth and onethird the length (sag) of glabella. The palpebral 

furrow is confluent with the axial furrow for a short 

distance posterior to the anterior pit; as a result 

each palpebral rim is connected by an eye ridge to 

the anterior pit. 

The single a~ssociated hypostoma lacks a posterior 

border and is incompletely silicified. The maculae 

serve to divide the subre·ctangular middle body, 

which is wider (tr) than long (sag) in a ratio of 

5.5 :4, into anterior and posterior lobes; the sagittal 

length of the anterior lobe is three times that of the 

posterior lobe. 

Librigenae, thorax, and pygidium not known. 

Illustrated specintens.-USNM 206857-206859. 

Occu?Tence.-USGS collection. 7343 CO (lithology 

of Millersburg Member of Lexington Limestone). At 

top ·Of tongue of Clays Ferry Formation, 0.9 mi 

south of Lair, Ky. Kentucky coordinates, North 

zone: E.1,983,700 ft; N.302,000 ft, Shawhan quadrangle, Kentucky. USGS collection 4959 CO. Upper 
D8 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

part of Grier Limestone Member of Lexington Limestone, 149-152 ft above Tyrone-Lexington contact. 

Central Kentucky Parkway. (Blue Grass Parkway),· 

north side at top of bluff. Kentucky coordinates, 

Nor:th zone: E. 1,835,050 ft; N. 173,600 ft, Salvisa 

quadrangle, Kentucky. 

Discussion.-In Platylichas bottniensis (Wiman) 

(Warburg, 1939, pl. 10) the posterior axial and 

longitudinal furrows intersect in front of the occipital furrow and in this regard differ from those 

of P. halli. The cranidium of P. laxatus (McCoy) 

(Warburg, 1939, pl. 12, figs. 2, 3, 5, 6, 9, 10; Dean, 

1963, p. 235-237, pl. 43, figs. 1, 2, 5, 8-12) is much 

wider ( tr) along the posterior border, has larger 

palpebral lobes, a narrower glabella, and shorter 

composite glabella lobes than the specimens from 

Kentucky. Whittington and Williams (1955, p. 424, 

pl. 40, figs. 113, 114, 117) described an indeterminate species from the Derfel Limestone of the 

Arenig District Wales, which is very sim.ilar in outline of glabella and proportions of frontal lobe but 

differs in the outline of composite glabellar lobes. 

Another Welsh s-pecies, P. nodulosus (McCoy) 

(Whi,ttington, 1962, pl. VII, figs. 1-8; 1968, p. 100-

101, pl. XXXI, figs. 5, 6, 8-11) is very similar to 

the Kentucky species in cranidial features, differing 

in having a narrower (tr) middle lobe of the glabella and a wider (.sag) anterior border. The median 

glabellar lobe of P. glenos Whittington (1962, p. 28, 

pl. VII, fig. 15; pl. VIII, figs. 3-5) is even narrower 

and its convexity in lateral view is greater than in 

the Kentucky species. 

A cranidium des·ignated P. cf. laxatus (McCoy) 

by De1an (1962, p·. 121, pl. 17, fig. 1) has a narrower 

glabella than P. halli; the 0omposite lobes of the glabella ar1e not terminated posteriorly by as. pronouncedly "hooked" longitudinal furrows and the 

median lobe of the glabella is narro·wer than in P. 

halli. 

Although the type specimen of Platylichas halli 

(Foerste) is not available for comparison, it is more 

than likely that we are dealing with this or a remarkably similar spe.cies. Foerste (1888, p. 120) 

oommented that the type specimen had come from 

the "Cincinnati Group" in Clermont County, Ohio. 

Bassler (1915, p. 35) interpreted this to mean 

"Maysville ( Corryville) ". The species range may 

easily include Edenian as well as Maysvillian 

equivalents .. 

Ancigin (1973, p. 106-107, pl. XV, fig.s. 11, 12, 

13, 15, 16) has described Platylichas micus from 

the uppermost Arenigian strata from the west side 

of the southern Urals. The widest part of the glabella is across the compound lobes, and the palpebral 

furruw is discrete from the axial furrow in this 

Rus.sian speeies; in both respects it diff;ers from P. 

halli. 

Order ODONTOPLEURIDA Whittington, 1959 

Family ODONTOPLEURIDAE Burmeister, 1843 

Subfamily ODONTOPLEURINAE Burmeister, 1843 

Genus PRIMASPIS Richter and Ri~hter, 1917 

Primaspis trentonensis (Hall) 

Plate 4, figures 8-14 

Acidaspis trentonensis Hall, 1847, p. 240, pl. 64, figs. 4a-f. 

Leonaspis trentonenwis? (Hall). Whittington, 1941, Jour. 

Paleontology, v. 15, p. 501-502, pl. 74, figs. 31-34. 

Primaspis trentonensis (Hall). Whittington, 1956b, Harvard 

Coli. Bull. Mus. Comp. Zoology, v. 114, no. 5, p. 203. 

The concept of PTimaspis tTentonensis as revised 

by Whittington (1941, p. 502-503, pl. 74, figs. 31-

37; 1956b, p. 203) included three specimens from 

two different localities. The present examination of 

specimens from Kentucky suggests that Whittington's hypodigm includes two different species. 

The holotype (AMNH 853/2), an enrolled specimen from ·exposures on the Bay of Quinte, near 

Belleville, Ontario, is illustrated in plate 4, figures 

8-11. The specimen has been somewhat abraded. 

The posterior margin of the occipital ring has been 

damaged and may have borne a median tubercle, 

which is now missing. Behind the occipital furrow 

a transverse row of five coarse tubercles decorates 

the axial part of the occipital ring. Each lateral lobe 

of the occip·ital ring is low and bounded proximally 

by a furrow, which may be deep mor:e because of 

zeolous preparation than from its natural state. The 

occipital furrow between the lateral occipital lobe 

and the posterior of the genal region is very shallow. 

The pygidium has only two pairs of sp·ines anterior to the major spines and two posterior pairs 

between the major ·spines. One of these posterior 

pairs is rooted in the bases of the major spines. 

The two sp:ecim.ens ( NYSM 9773, 977 4) of 

Primaspis (pl. 4, figs. 12-14) from the Trenton 

I

, Group at Trenton Falls, N. Y. (Whittington, 1941, 

pl. 74, figs. 35, 36, 37) have a different ornamentaj tion of the oc-cipital ring. A large median tube·rcle 

1 is present; other tubercles are :evenly distributed 

I behind the occipital furrow but increase in size to 

a transverse row behind the large median tubercle 

along the margin of the occipital ring. There are 

two· pairs of pygidial border spines in front of the 

ma.j or pair and two posterior pairs, both of which 

are discrete from the major spines. 

Three specimens, to be sure, can hardly be a suf..; 

ficient sample on which to base two species, but we 

· are faced with the fact that PTimaspis t1·entonensis 
ADDITIONAL TRILOBITES FROM THE ORDOVICIAN OF KENTUCKY D9 

(Hall) is based on one of them. The other two specimens differ in features that are of species rank. Additional collections should be made and studied. 

Primaspis sp. x 

Plate 5, figures 1-14; plate 6, figures 1, 2 

This species is represented in three collectionsUSGS collections 6143 CO, 6990 CO, and 7343 CO. 

An unfortunate amount of variation occurs between 

specimens, even between those from the same collection, in regard to details of ornament. These differences are caused almost entirely by different degrees 

of silicification. It is paradoxical that a single partial trilobite. (pl. 5, figs. 1, 2) whose dorsal surface 

preserves almost no fine ornament is the only known 

specimen to retain silicified casts of usually 

evanescent appendages. 

In general, cranidial features, including the tuberculate surface ornamentation, are similar to those 

of P. evoluta (Tornquist) as described and illustrated by Bruton ( 1966), p. 4-7, pl. 1, figs. 3, 5, 6), 

although slight differences in proportions do exist. 

Excluding genal spines the width (tr) of cephalon 

is approximately 2.5 times its length (sag). Similarly, the width (tr) of the cranidium at the posterior border is 2.0 times the cranidiallength (sag). 

At the palpebral lobes, the width (tr) is about 1.3 

times the sagittal length of the cranidium. The anterior width ( tr) between antenna! notches is almost 1.1 times the cranidiallength (sag). 

The width (tr) of the glabella at lateral lobe 1p 

is essentially equal to the glabellar length (sag) including occipital ring. At lobe 2p, it is almost 0.9 

and at lobe 3p, almost 0.6 of the glabellar length 

(sag). Lobe 1p semiovoid, pointed anterolaterally; 

lobe 2p about half as long ( exsag), semiovoid, but 

pointed posteroproximally. Lobe 3p very small, almost rectangular, narrow, directed anterolaterally. 

Anterior lobe of glabella slightly expanded. Occipital 

furrow deepest behind lateral glabellar lobe 1p. 

Occipital ring occupies almost one-third sagittal 

length of glabella; width (tr) of occipital ring at 

posterior border equals 0.8 glabellar length including occipital ring. Axial furrows poorly de·fined anteriorly but become deeply entrenched at distal end 

of glabellar furrow 3p, then run backward and outward around front third of lobes 1p and converge 

sharply to intersect occipital furrow, then diverge 

markedly around occipital lobes to cross posterior 

border. Lateral furrows 1p and 2p are deepest close 

to the longitudinal furrow. Longitudinal furrows 

arise faintly from proximal ends of 3p running almost straight backward to the occipital furrow, 

which they join in diverging downward into a deep 

pit behind lobe 1p; they then run almost straight upward and backward halfway across the occipital ring 

to delimit the proximal sides of occipital lobes. 

The occipital ring is divided into an anterior 

tuberculate half and a raised, smooth, bordering 

posterior half. A median tubercle is present on the 

posterior half. Laterally the tuberculate surface extends to the longitudinal furrows; the swollen 

occipital lobes are a part of the posterior portion of 

the occipital ring. 

On a line through the eye centers, each fixed cheek 

is a little lower than lateral glabellar lobes 1p; 

the width (tr) on that line is slightly less than the 

greatest width of lobe 1p. 

Facial sutures follow raised sutural ridges. Anteriorly the sutures converge slightly in dorsal view 

and cross the dorsal side of the border above the 

antenna! notch to the outer margin; from there the 

sutures converge sharply in a curving course downward and backward across the narrowly rolled 

doublure inside the antenna! notch. As a result, the 

notch is entirely on the free cheek. In ventral view 

a connective suture runs almost straight between 

facial sutures and separates an extremely narrow 

(sag) rostral plate from the remainder of the 

doublure; in anterior view the connective suture appears somewhat sinuous. The posterior edge of the 

rostral plate is concave in outline to fit the curved 

front of the hypostoma. The posterior facial sutures 

diverge at about 160° to the border furrow, then 

curve sharply to cross the posterior border immediately within the base of the genal spine. 

Each librigena bears a small bulbous eye above 

a genal platform which slopes approximately 45°. 

The prominent rolled border, set off by a deep furrow, bears 14 small tubercles along its ventral surface. The length of genal spine is about equal to the 

distance from axial furrow to facial suture at the 

posterior border. 

The hypostoma is of low convexity; its length 

about three-fourths its width. Anterior wings flexed 

dorsally to fit contour of antenna} notch on doublure. 

Lateral notch shallow. Shoulder angular, moderately swollen. Border furrow shallow. Maculae not 

evident, perhaps because of poor preservation. 

Thorax composed of 10 segments, each bearing a 

strong axial ring, principal pleural ridge, and prin-

-cipal pleural spine. The anterior ridge bears a neat 

row of tubercles, commonly six, and extends into 

an anterior pleural s.pine. Tubercles are also sparsely 

present on the axial ring. 
D10 CONTRIBFTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Exclusive of marginal spines the width ( tr) of 

the pygidium is twice its length (sag). The axis is 

composed of two rings and terminal piece. The anterior axial ring is confluent with a large pair of 

diverging, essentially horizontal major spines. From 

the thickened border four pairs of smaller spines 

protrude, two pairs ahead of the large pair and two 

pairs behind. The bases of all spines are discrete. 

Appendages.-On the ventral side of a single 

specimen (pl. 5, fig. 2) crude silicified casts of appendages are preserved. Silicification is too coarse to 

show the number of segments in each appendage. 

The specimen does show a pair of slender legs ( ?) 

for each segment of the thorax. Although one cannot determine any details of appendages under the 

cephalon it seems probable that they were different 

from thoracic appendages. With a modicum of 

imagination, one can visualize an anterior pair of 

mitten-shaped appendages (pl. 5, fig. 2, beneath the 

hypostoma. These modified appendages may have 

aided in the food-gathering process. 

Michael E. Taylor (oral a·nd written commun., 

1973) has called my attention to a somewhat similar 

arrangement of appendages on the modern isopod 

crustacean SeTolis. 

Illustrated specimens.-USNM 206860-206864 

inclusive. 

OccuTTence.-Clays Ferry Formation, USGS collection 6143 CO, Cynthiana quadrangle; USGS collections 6990 CO, 7343 CO, and 7812 CO Shawhan 

quadrangle, Kentucky. 

Discussion.-! have tentatively assigned to 

Primaspis sp. x the only specimen found in collection 6990 CO; this is a delicate, almost complete 

trilobite, but silicification of the pygidium is incomplete (pl. 5, figs. 10-14). The major spines of the 

pygidium are not differentially enlarged and the anterior and posterior spines are little more than 

tubercles around the margin. Whether the underdevelopment of the pygidial spines is an artifact of 

poor silicification or an original feature cannot be 

known until additional specimens are available from 

the same locality. 

PTimaspis sp. x bears a strong resemblance to P. 

evoluta Tornquist (Bruton, 1966, p. 4-7, pl. 1, figs. 

1-9) from the Boda Limestone of Sweden. The 

cranidium of the Kentucky species tends to be wider, 

but this might be related to the smaller size of specimens. The major spines of the pygidium are discrete from minor spines between them; in P. 

evoluta there are three pairs of spines between the 

major ones and one of these is rooted in the major 

spines. P. bestoTpensis Bruton possesses three more 

pairs of pygidial spines than P. sp. x and P. multispinosa Bruton has at least five mo·re pairs. 

PT'imaspis p?·irnoTdialis (Barrande) differs in having paired occipital spines on the glabella. In P. 

ascitus Whittington (1956b, p. 199-205, pl. 1, 2) 

the surface ornamentation is more densely tuberculate, the posterior border of the cranidium including the back of the occipital ring is tuberculate 

rather than smooth, and the pygidial spines number six pairs of which one is based on the major 

spines. 

All of the species of Pri1naspis described by 

Whittard (1961, p. 199-204, pl. XXVII) differ from 

P. sp. x either in number of pygidial spines or proportions of the cranidial features. In P. whitei there 

are 17 spines on the ventral border of the free 

cheeks, wider fixed cheeks, and 2 more pairs of 

pygidial spines. Primaspis simulatrix has more 

elongate glabellar lobes 1p, and a pygidium with 

many more sp-ines. P. rorringtonensis differs in it.s 

very densely spaced tubercles on the surface. 

Pri1naspis sen1ievoluta Reed (Dean, 1962, p. 122, 

pl. 17, figs. 3, 13) has· narrower fixed cheeks, but 

like P. halh has a total of five pairs of pygidial 

spines. 

Primaspis harnagensis (Bancroft) (Dean, 1963, 

p. 237-238, pl. 44, figs.1, 4, 6, 8) has longer (exsag) 

glabellar lobes 1p, and narrower (tr) fixed cheeks 

than P. sp. x; there are four pairs of pygidial spines 

in front of the major pair. P. caractaci (Salter) 

possesses one more posterior pair of pygidial spines 

(Dean, 1963,p. 240). 

Bruton (1968a, p. 13-14, pl. 2, fig. 5) noted that 

P. peregrina (Barrande) "has a smooth posterior 

margin of the occipital ring" and may be the only 

previously described species to share this feature 

with the specimens from Kentucky. 

Primaspis sp. y 

Plate 6, figures 3-16 

This species is represented by 3 fragmentary 

cranidia, 2 librigenae, 10 incomplete pygidia, and 2 

fragments of thoracic segments from collection 5015 

CO, and 2 fragmentary cranidia, 4 librigenae, 5 incomplete pygidia, and numerous fragments of 

thoracic segments from collection 6915 CO. 

The proportions of the cranidia of this species are 

almost identical to those of Pn:maspis sp. x, but a 

few significant differences exist, even though none 

of the cranidia is fully mature. The surface of the 

occipital ring in PTimaspis sp. y is tuberculate over 

its entire surface; the large median tubercle is posi1 tioned high on the posterior part. 
ADDITIONAL TRILOBITES FROM THE ORDOVICIAN OF KENTUCKY D11 

On the librigenae, 13 large tubercles or short 

spines ornament the ventral side of the border. 

Six pairs of marginal spines ornament the 

pygidium. The major spines diverge initially at an 

angle of 30 o ; a very short distance behind the 

pygidial margin they curve inward so that their 

tips converge at an angle less than 15° without meet~ 

ing. Three pairs of anterior spines decrease in size 

forward. Of the two pairs of posterior spines the 

median pair is the larger; the second smaller pair 

is rooted in the base of the major pa.ir of spines. 

Illu.st?·ated specin~ens.-USNM 206865-206870 

inclusive. 

Occu?Tence.-Salvisa Bed of Perryville Limestone 

Member of Lexington Limestone, USGS collection 

6915 CO, USGS collection 5015 CO. 

D'iSC'USS'ion.-PTin~asp?:s sp. y differs from P. sp. 

x in lacking a smooth posterior borde-r of the occipital ring. But the most striking difference is in the 

pygidium. In P. sp. y the major spines diverge. at 

60 o, and they maintain that angle throughout their 

length ; there are only two ra the·r than three pairs 

of anterior border spines and both posterior pairs 

of spines are discrete from the major spines. 

P1·in~aspi.s sp. y differs significantly from P. 

ascitus Whittington only in the direction of recurving of the major pygidial spines and in the size of 

the pos,terior spines that arise from the bases of the 

major spines. Whittington (1956b, p. 205) noted 

that the number of anterior border spines in P. 

ascUus is reduced with an increa,se in pygidial size 

fr.om a sagittal length of 0.9 to 1.35 mm. In PTimasp'iS sp. y a series of pygidia shows no change in 

number of border spines. although the sagittal 

length, exclusive of the articulating half ring, ranges 

from 0.75 to 1.5 mm. The close resemblance to P. 

asdtus suggests that the Salvisa Bed may be correlative with the lower part of the Martinsburg 

Shale north of Harrisonburg, Va. 

P?"i?nasm:s sen~ievoluta has one fewer pair of 

pygidial spines than does P. sp. y and P. haTnagens·is; there are four rather than three pairs in 

front of the major sp.ines. P. evoluta has two pairs 

of anterior and three pairs of posterior spines. 

Associated with the small specimens assigned to 

P1"in~aspis sp. y in collection 5015 CO are a large 

cranidium and pygidium (pl. 6, figs. 17-19, 21-23), 

which may be mature specimens of the same species. 

They are tentatively designated as Acidaspis sp. a, 

however. 

Genus ACIDASPIS Murchison, 1839 

Acidaspis? sp. a 

Plate 6, figures 17-19, 21-23 

A large cranidi urn and part of a large pygidi urn 

are associated with PTimaspis sp. y in USGS collection 5015 CO. Because of the number of border 

spines it is unlikely that the pygidium could belong 

to P1·imaspis sp. y; it resembles more closely pygidia 

of Acidaspis. The cranidium lacks the enormous occipital spine of Acidaspis, although the obtusely 

pointed extension of the occipital ring can be interpret·ed as such a spine. This cranidium may be 

a large mature specimen belonging to Pri1nasp1:s sp. 

y. Until additional material is discovered, the correct generic and specific assignment of these two 

specimens is uncertain. 

Sagittal length of cranidium is 6 mm, more than 

twice that of any cranidium here assigned to 

PTi?naspis sp. y. Cranidial length (sag) equals 0.6 

width (tr) at posterior margin and 0.7 width at 

palpebral lobes. Length (sag) of glabella including 

occipital ring is 0.94 sagittal length of cranidium 

but length of glabella excluding occipital ring only 

0.6 cranidial length. Length (sag) of occipital ring 

about 0.6 length of glabella in front of ring. Longitudinal furrows and occipital furrow shallow and 

broad, devoid of tuberculation. Middle lobe of glabella narrower (tr) than lateral lobe 1p and only 

slightly wider than greatest width (tr) of fixed 

I 

cheek. Width (tr) of glabella at lobes 1p equals 1.5 

sagittal length of glabella excluding occipital ring 

i and 0.7 transverse widt.h of cranidium between 

palp·ebral lobes. 

Narrow distinct dorsal furrows curve inward 

around lobes 1p to join occipital furro·w. A very 

short, shallow crescentic furrow branches from 

longitudinal furrow to indent the inner side of lobes 

1p; this f .J.Yxure previously described only fo·r 

Acidaspis aviensis Bruton (1968b, p. 300, fig. 12). 

Lateral furrows 1p and 2p subparallel and deep, 

clearly defining 2p. Furrow 3p very faint so that 3p 

is poorly defined and barely separated from frontal 

lobe. Three pairs of posterior border spines, of 

which the outer pair is rooted in the inner side of 

the major spines. 

Jllust1·ated speci1nens.-USNM 206871, 206872. 

Occu?Tence.-Salvisa Bed of Perryville Limestone 

Member of Lexington Limestone, USGS collection 

5015 co. 

Discussion.-The sagittal length of the occipital 

ring is longer (relative to the width of the ring) 

than in known species of P1·i1naspis. The peculiar 

indenting of the inner side of glabellar lobe 1p is 

shared by Acidaspis sp. b described here. However, 

in A. sp. b, the indenting furrow seems to be a continuation adaxially of furrow 1p, whereas in sp. a 
D12 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

it may be a minute indistinct anterolateral branch 

of the longitudinal furrow. Other species of Acidaspis may exhibit this feature, although it seems to 

have gone unnoticed in 'previous descriptions; it 

appears to be present in A. gTayi Barrande (Bruton, 

1968a, pl. 5, figs. 4, 6) . 

Acidaspis sp. b 

Plate 6, figures 20, 24-26 

The following description is based on a damaged 

silicified cranidium and a fragm~entary silicified 

pygidium. 

As in other species of Acidaspis, the axial l~obe of 

the cranidium is composed of a short wide glabella 

and an occipital ring dominated by a huge median 

spine. The occipital furrow is shallow medially; it 

curves hack across the longitudinal furrows and 

around the posterior ends of lateral glabellar lobe~ 

lp to reach the axial furrows .. Axial furrows are 

shallow but distinct in bounding the glabella; from 

their junction with the occipital furrow behind the 

lateral lobes lp, they diverge to, bound the occipital 

ring, turni,ng straight back at the border furrow to 

cross the margin. At the posterior margin the width 

(:tr) of thre occipital ring is 1.3 times the sagittal 

length of the glabella. 

The glabella is widest at lateral lobes lp. The 

sagiUJal glabellar length is 0.7 width (tr) at lobes 

lp, 0.9 width (tr) at lobes 2p, and 1.22 times width 

(tr) at lobes 3p. Each lateral lobe 1p is broadly 

elliptical and only moderately inflated; length 

(exsag) is half the sagitt1al length of glabella. The 

length ( exs·ag) of lobe 2p slightly overlaps lobe lp 

and is one-third the glabellar length. 

Lobe 3p is minute; its width (tr) exc:eeds its 

length ( exsag), which is only 0.13 the sagittal glabellar length. The longi1tudinal furrow does not alter 

lobe 3p, but originates in the proxim:al end of furrow 2p, from whence it runs back shallowly to meet 

th:e occipital furrow; from the junction a short 

sharply incised furrow curves inward and backward 

about halfway across the occipital ring. This short 

furrow might be considered the terminus of the 

longitudinal furrow. It partially defines a small occipital lobe. 

Palpebrallobe:S are short (ex:Sag), semierect, and 

positioned opposite the occipital furrow. The palpebral rims and furrows are confluent forward with 

the eye ridges~, which converge to the anterior border 

furrow, where they terminate aga•inst the frontal 

lobe of the glabella. Anteriorly the facial sutures 

converge to the border furrow (but not as much as 

the eye ridges), and cross the border to· the front 

margin where a conne~ctive suture parallels the margin. The course on the doublure is not known. Posteriorly the suture runs downward almost to the 

border furrow, turns la:te~rally parallel to the furrow, and then crosses furrow and border at an angle; 

the width (tr) of cranidium at the border is 1.6 

,tim:es the sagittal length of the glabella. 

The fragmentary pygidium excluding spines 

seems to have been about four tim:es. as. wide as long. 

The axis must have been composed of two rings and 

a terminal piece, all crudely defined. The anterior 

ring is linked by a raised ridge with a pair of coarse 

marginal spines. Six s.maller pairs are: arranged 

three in front of and three between the major 

spin:es; the inner pair adjacent to the major spines 

is based indis1tinctly on the larger spines. 

IllustTated specimens.-VSNM 206873, 20687 4. 

OccuTTence.-USGS collection 7343 CO. Top of 

tongue of Clays, Ferry Formation 0.9 mi south o.f 

Lair; Kentucky coordinate1s: E. 1,983,700 ft, N. 302,-

000 ft, Shawhan quadrangle, Kentucky. 

Discussion.-The single silicifi.ed cranidium described here is almost identical in proportions to 

that illustrated by Ross (1967, pl. 5, fig. 20); the 

only difference is the seeming absence of lateral 

glabellar lob:e 3p in the previously illustrated specimen. Whether the contrast between limestone and 

silicified preservat~on could account for this difference is, doubtful, but possible.· 

The peculiar indenting of glabellar lobe 1p adj acent to the longitudinal furrow has be·en previously 

discussed, under Acidaspis sp. a. 

REFERENCES CITED 

Ancigin, N. A., 1973, Trilobiti, in Stratigrafiia i fauna ordovika srednigo Urala [Trilobita, in Ordovician stratigraphy and fauna of the central Urals]: Moscow Ministry of Geology of USSR, Geol. Dept. Ural. Terr., p. 

62-111, pls. 1-19. 

Bassler, R. S., 1915, Bibliographic index of American Ordovician and Silurian fossils: U.S. Nat. Mus. Bull. 92, v. 

1, 718 p. 

Bondarev, V. I., Burskyi, A. Z., and Nekhorosheva, L. V., 

1968, A stratigraphical classification of the Ordovician 

of the arctic regions of the Ural-Novaya Zemlya fold 

area and its correlation with Ordovician standards of 

North Europe, in Stratigraphy of central European 

lower Paleozoic: Internat. Geol. Cong., 23d, Prague, 

1968, Proc., sec. 9, p. 85-95. 

Bruton, D. L., 1965, The Middle Ordovician of the Oslo 

region., Norway-19, The trilobite family Odontopleuridae: N orsk Geol. Tidsskr., v. 45, pt. 3, p. 339-356, pls. 

1-3. 

--1966, A revision of the Swedish Ordovician Odontopleuridae (Trilobita) : Uppsala Univ., Palaeont. Inst., 
ADDITIONAL TRILOBITES FROM THE ORDOVICIAN OF KENTUCKY D13 

pub. 67, 40 p., 6 pis.; also pub. as Uppsala Univ. Geol. 

Inst. Bull., v. 43, no. 8, 37 p., 1967. 

---1968a, A revision of the Odontopleuridae (Trilobita) 

from the Palaeozoic of Bohemia: Norske Vidensk.-Akad. 

Oslo. Skr., Mat.-Naturv. Kl., new ser., no. 25, 73 p. 

11 pl. 

---1968b, Ordovician odontopleurid trilobites from Estonia and Latvia: Lethaia, v. 1, no. 3, p. 288-302, 13 figs. 

Cooper, B. N.; 1953, Trilobites from the lower Champlainian 

formations of the Appalachian Valley: Geol. Soc. America Mem. 55, 69 p., 19 pis. 

Cooper, G. A., and Kindle, C. H., 1936, New brachiopods and 

trilobites from the Upper Ordovician of Perce, Quebec: 

Jour. Paleontology, v. 10, no. 5, p. 348-372, pls. 51-53. 

Dean, W. T., 1962, The trilobites of the Caradoc Series in 

the Cross Fell inlier of Northern England: British Mus. 

(Nat. History) Bull., Geolog'Y, v. 7, no. 3, p. 65-134, 

pis. 6-18. 

---1963, The Ordovician trilobite faunas of South Shropshire, III: British Mus. (Nat. History) Bull., Geology, 

v. 7, no. 8, p. 213-254, pls. 37-46. 

Foerste, A. F., 1888, Notes on Paleozoic fossils from Australia, Ohio, and New Brunswick: Denison Univ. Sci. 

Lab. Bull. 3, p. 117-133, pl. XIII. 

Hall, James 1847, Descriptions of the organic remains of the 

lower division of the New York System: Paleontology 

of New York, v. 1, 338 p., 87 pls. 

Harrington, H. J., 1959, General description of Trilobita, in 

Moore, R. C., ed., Treatise on invertebrate paleontology, 

Part 0, Arthropoda 1: New York and Lawrence, Kans., 

Geol. Soc. America and Univ. Kansas Press, p. 038-0117. 

Harrington, H. J., and Leanza, A. F., 1957, Ordovician trilobites of Argentina. Kansas Univ. Dept. Geology Spec. 

Pub. 1, 276 p., 140 figs. 

Harrington, H. J., Moore, R. C., and Stubblefield, C. J., 1959, 

Morphological terms applied to trilobita, in Moor·e, R. C., 

·ed. Treatise on invertebrate paleontology, Part 0, Arthropoda 1: New York and Lawrence, Kans., Geol. Soc. 

America and Univ. Kansas Press, p. 0117-0126. 

Henningsmoen, Gunnar, 1957, The trilobite family Olenidae, 

with description of Norwegian material and remarks on 

the Olenid and Tremadocian sedes: N orsk Videns.-

Akad., Oslo, Mat.-Naturv. Kl., Skr. 1, 303 p., 31 pls. 

---1975, Moulting ·in trilobites: Fossils and strata, no. 4, 

NATO Advanced Study Inst., Oslo, Proc., p. 179-200. 

Jaanusson, V., 1964, The Viruan (Middle Ordovician} of 

Kinnehulle and northern Billingen Voster-gotland: Uppsala Univ. Geol. Inst. Bull. no. 1, p. 1-73, 30 figs. 

Lesperance, P. J., 1968, Ordovician and Silurian trilobite 

faunas of the White Head Formation, Perce Region, 

Quebec: Jour. Pal,eontology, v. 42, p. 811-826, pl. 106. 

Modlinski, Zdzislaw, 1967, Stratigrafia ordowiku W obnizeniu 

litewskim (polska cz~sc syneklizy perybattyckiej) [Stratigraphy of the Ordovician deposits occurring in the 

Lithuanian depression]: Kwart. Geol. v. 11, no. 1, p. 

68-75, 2 figs. [English summ., p. 75] 

Opik, A., 1937, Trilobiten aus Estland: Tartu Univ., Geol. 

Inst., Pub. 52, 163 p., 26 pls. 

Owens, R. M., 1970, The Middl.e Ordovician of the Oslo 

region, N orway-23, The trilobite family Proetidae: 

Norsk Geol. Tiddskr., v. 50, no. 4, p. 309-332, figs. 1-8. 

---1973a, Ordovician proetidae (Trilobita) from Scandinavia: N orsk Geol. Tidsskr., v. 53, no. 2, p. 117-181, 

figs. 1-15. 

---1973b, British Ordovician and Silurian Proetidae 

(Trilobita) : Paleont. Soc. Mon. 98 p., 15 pls. 

Ross, R. J., Jr., 1967, Calymenid and other Ordovician trilobites from Kentucky and Ohio: U.S. Geol. Surv.ey Prof. 

Paper 583-B, 18 p., 5 pis. 

Ruedemann, Rudolf, 1926, The Utica and Lorraine Formations of New York, Part 2, Systematic paleontology, 

Number 2, Mollusks, crustaceans, and eurypterids: New 

York State Mus. Bull. 272, 227 p., 28 pis. 

Shirley, Jack, 1936, Some British trilobites of the Family 

Calymenidae: Geol. Soc. London Quart. Jour., v. 92, pt. 

4, p. 384-421, pl. XXIX-XXXI. 

Tripp, R. P., 1957, The classification and evolution of the 

superfamily Lichacea (Trilobita) : Geol. Mag., v. 94, 

no. 2, p. 104-122. 

---1962, Trilobites from the confinis flags (Ordovician) 

of the Girvan District, Ayrshire: Royal Soc. Edinburgh 

Trans., v. 65, no. 1, 36 p., 4 pls. 

---1967, Trilobites from the Upper Stinchar Limestone 

(Ordovician) of the Girvan District, Ayrshire: Royal 

Soc. Edinburgh Trans., v. 67, no. 3, p .. 43-93, 6 pls. 

Warburg, Elsa, 1939, The Swedish Ordovician and lower 

Silurian Lichidae: Svenska Vetensk Akad. Hand!., v. 

17, no. 4, p. 1-162. 

Whittard, W. F., 1955-1967, The Ordovician trilobites of the 

Shelve inlier, West Shropshire: London, Palaeontog. Soc. 

Mon. 352 p., 50 pls. 

Whittington, H. B., 1941, Silicified Trenton trilobites: Jour. 

Paleontology, v. 15, no. 5, p. 492-522, pis. 72-75. 

---1956a, Type and other species of Odontopleuridae 

(Trilobita): Jour. Paleontology, v. 30, no. 3, p. 504-520, 

pls. 57-60. 

---1956b, Silicified Middle Ordovician trilobites: The 

Odontopleuridae: Harvard College, Mus. Comp. Zoology 

Bull., v. 114, no. 5, 288 p., 24 pis. 

---1962-1968, Monograph of the Ordovician trilobites 

of the Bala area, Merioneth: Lqndon Palaeontographical 

Soc., pt. 1, p. 1-32, pls. 1-8, v. 116 (1962); pt. 4, p. 

93-138, pis. 29-32, v. 122 (1968). 

Whittington, H. B., and Williams, A., 1955, The fauna of 

the Derfel Limestone of the. Arenig District, North 

Wales: Royal Soc. London Philos. Trans., Ser. B, no. 

658, v. 238, p. 397-430. 

Williams, Alwyn, 1962, The Barr and lower Ardmillan series 

(Caradoc) of the Girvan District, south-west Ayrshire, 

with descriptions of the brachiopoda: Geol. Soc. London 

Mem. 3, p. 5-267, pl. 1-25. 
PLATES 1-6 

Contact photographs of the plates in this report are available, at cost from U.S. 

Geological Survey Library, Federal Center, Denver, Colorado 80225 
PLATE 1 

[All il!ustra tions are stereophotographs except figures 14 and 15] 

FIGURES 1-13. Triarthrus eatoni (Hall) (p. D2). 

Kope Formation, Laurel 7%-minute quadrangle, Kentucky, All 

figures X 5. 

1-3. Complete individual, enrolled. Relative to cephalon, 

dorsal, anterior, and lateral views. UCM 40633a. 

4-6. Complete individual, enrolled. Relative to cephalon, 

dorsal, anterior, and lateral views. UCM 40633b. 

7-9. Complete individual, enrolled. Relative to cephalon, 

dorsal, anterior, and lateral views. UCM 40633d. 

10-12. Complete individual, enrolled. Relative to C€phalon, 

dorsal, anterior, and lateral views. UCM 40633e. 

13. Partly enrolled individual on pleural tips showing 

lateral projections that fit snugly against doublure of 

cephalon. UCM 40633c. 

14, 15. Isotelus gigas DeKay (p. D5). 

USGS colin. 5015 CO, Perryvill€, Ky. Dorsal views of yoked 

doublure of free cheeks. Median suture no longer functional. 

USNM 206844, 206845 (X 1). 

16, 17, 18. Megalaspid(?) pygidium (p. D5). 

Posterior, lateral, and dorsal views, (X 3). 

USNM 206846. Camp Nelson Limes~one, USGS colin. 7875 CO. 
GEOLOG ICAL SURVEY PROFESSIONAL PAPER 1066-D PLATE 1 

TRIARTHR US, ISOTELUS, MEGALASPID(?) 
PLATE 2 

[All figures are stereopbotographs] 

FIGURES 1-6. Decoroproetus sp. x (p. D3). 

Two partly enrolled individuals, only partly silicified. USGS colln. 

6143 CO, Clays Ferry Formation, Cynthiana quadrangle, Kentucky. 

1-3. Specimen preserving preglabellar field anterior border,thoracic and pygidial axis (X 5), USNM 206836. 

4-6. Specimen preserving part of genal spine; hypostoma in place 

(X 4), USNM 206837. 

7-16. Decoroproetus sp. 2 (p. D4). 

USGS colin. 5015, Perryville Limestone Member of Lexington 

Limestone Perryville quadrangle, Kentucky. All figures (X 4). 

7-9. Pygidium, dorsal, posterior, and lateral views, USNM 

206838. 

10-12. Pygidium, lateral, dorsal, and posterior views, USNM 

206839. 

13, 14. Librigena, dorsal and ventral views, USNM 206840. 

15, 16. Librigena, ventral and dorsal views, USNM 206841. 

17. Pygidium undetermined, not described. 

USGS colin. 6419 CO, Logana Member of Lexington Limestone, 

Wilmore quadrangle, Kentucky. USNM 206843. 

18, 19. Gravicalymenc hagani Ross (p. D5); 

Thoracic segment showing construction of pleural tip (X 3), USGS 

colin. 5015 CO. USNM 206849. Note smooth facet and vincular stop. 

20. Cybelinid cranidium ( p. D5). 

Dorsal view (X 2). USNM 206842. USGS colin. 6419 CO, Logana 

Member of Lexington Limestone, Wilmore quadrangle, Kentucky. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-D PLATE 2 

DECOROPROETUS, GRAVICALYMENE, CYBELINID 
FIGURES 

PLATE 3 

[All figures are stereophotographs] 

1-9. Gravicalymene hagani Ross (p. D5). 

USGS colln. 5015 CO. Perryville Limestone Member of Lexington 

Limestone. 

1-3. Cranidium, inmatur,e, dorsal, anterior, and lateral views 

(X 4). USNM 206847. 

4. Cranidium, large (possibly gerontic), showing apodemes for 

attachment of hypostoma. Ventral view (X 2). USNM 

206850. 

5. Hypostoma, ventral view (X 5). USNM 206852. 

6-8. Cranidium, mature, lateral, dorsal; and anterior views (X 2). 

USNM 206848. 

9. Cranidium, ventral view (X 2), showing apodemes for attachment of hypostoma. USNM 206851. 

10. Flexicalymene sp. (p. D6). 

Partial cranidium, dorsal view (X 5). USNM 206856. USGS colin. 

6129 CO., Ashlock Formation. 

11-20. Gravicalymene truncatus n. sp. (p. D6). 

USGS colin. 7984 CO, Kope Formation, Moffett Road section, 

Demossville quadrangle, Kentucky. 

11. Large associated pygidium, para type, dorsal view (X 3). 

USNM 206853. 

12-14. Partial cephalon, paratype, dorsal, lateral, and anterior 

views (X 4). USNM 206855. 

15, 20. Pygidium, dorsal and posterior views (X 3). Same pygidium 

shown on left in figure 19. USNM 206854 (same no. as 

figs. 16 and 19). 

16-18. Cephalon and anterior part of thorax (same shown in fig. 

19), holotype, dorsal, anterior, and lateral views (X 3). 

USNM 206854. 

19. Thorax, lateral view of holotype, same specimen as in 

figures 15-18, 20. USNM 206854. 
GRAVICALYMENE, FLEXICALYMENE 
FIGURES 

PLATE 4 

[All figures are stereophotographs] 

1-7. Platylichas halli (Foerste) (p. D7). 

USGS colln. 7343 CO. Tongue of Clays Ferry Formation, Shawhan 

quadrangle, Kentucky. 

1. Hypostoma, ventral view (X 5), of a partially silicified 

specimen. USNM 206857. 

2-4. Cranidium, dorsal, lateral,• and anterior views (X 3). USNM 

206858. 

5-7. Cranidium, dorsal, anterior, and lateral views (X 2). USNM 

206859. 

8-11. Primaspis trentonensis (Hall) (p. D8). 

Holotype, illustrated by Hall (1847, pl. 64, fig. 4) and by Whittington (1941, pl. 74, figs. 31-34). Enrolled individual, views 

relative to cephalon are dorsal, ventral, anterior and lateral 

(X 6). AMNH 853~. Bay of Quinte, Ontario. 

12-14. Primaspis "trentonensis" (p. D8). 

Trenton Group near Trenton Falls, N.Y., (X 5). Previously illustrated by Whittington (1941, pl. 74, figs. 35-37) but not same 

species as Hall's holotype. 

12, 13. Individual showing ornament of occipital ring and arrangement of pygidial spines. NYSM 9774. 

14. Individual demonstrating cephalic features. NYSM 9773. 
GEOLOGICAL URVEY PROFESSIONAL PAPER 1066-D PLATE 4 

PLATYLICHAS, PRIMASPIS 
PLATE 5 

[All figures are stereophotographs] 

FIGURES 1-14. Primaspis sp. x (p. D9). 

Clays Ferry Formation, Cynthiana and Shawhan quadrangles, Kentucky. 

1, 2. Cephalon and partial thorax with silicified casts of appendages crudely preserved on ventral side (X 7). 

USNM 206860. USGS colin. 6143 CO. 

:), 4. Nearly complete individual. Dorsal and anterior views 

(X 7). USNM 206861. USGS colin. 6143 CO. 

5-9. Partial specimen, lacking posterior thorax and pygidium. 

Views of dorsal cephalon, thorax, ventral cephalon and 

hypostoma, anterior c·ephalon, and lateral (X 5). 

USNM 206863. USGS colin. 7343 CO. 

10-14. Complete individual (X 5). USNM 206862. USGS colin. 

6990 CO. Stumps of appendages may be partly preserved on ventral side in figure 11. Compare pygidium in 

figure 12 with that in plate 6, figure 1. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 106&--D PLATE 5 

PRIMASPIS 
FIGURES 

PLATE 6 

[All figures are stereophotographs] 

1-2. Primaspis sp. x (p. D9). . 

Thorax and pygidium showing fine ornament. Dorsaf and 

lateral views ( x 5). USNM 206864. USGS colin. 7343 CO. 

3-16. Primaspis sp. y (p. D10). 

Salvisa Bed of Perryville Limeston(; Member of ·Le-xington 

Limest,one, USGS colin. 6915 CO, except figs. 13, '14. 

3. Posterior part of cranidium, dorsal view showing 

full width (tr) at posterior border and occipital 

lobes (X 6). USN'~, ~06865.' 

4-6. Cranidium lacking po:sterior part of fixed cheeks. 

Dorsal~ anterior,_ and ·lateral views (X 7). USNM 

206866. 

7-9 .. Pygidium, dorsal, lateral, and posterior views (X 

7). USNM 206868. 

10-12. Pygidium, dorsal, lateral, and posterior views (X 

7). USNM 206869. 

13, 14. Hypostoma, ventral and dorsal views (X 7). USNM 

206870. USGS colin. 5015 CO. 

15, 16. Librigena, dorsal and lateral views (X 7). USNM 

206867. 

17-19, 21-23. Acidasp·is? sp. a (p. D11). 

USGS colin. 5015 CO, Salvisa Bed of Perryville Limestone 

Member of Lexington Limestone. 

17-19. Cranidium; dorsal, anterior, and lateral views (X 

4). USNM 206871. 

21-23. Pygidium, lacking left pleural region and tips of 

all spines. Dorsal, posterior, and lateral views 

(X 4). USNM 206872. 

20, 24-26. Acidaspis sp. b. (p. D12). 

USGS colin. 7343 CO. Tongue of Clays Ferry Formation. 

20. Pygidium, poorly preserved; dorsal view (X 3). 

USNM 206874. 

24-26. Cranidium, dorsal, anterior, and lateral views (X 

3). USNM 206873. 
GEOLOG ICAL SURVEY PROFESSIONAL PAPER 106&--D PLATE 6 

PRIMASPIS, ACIDASPIS 
Edrioasteroids (Echinodermata) 

By BRUCE M. BELL 

CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF 

KENTUCKY AND NEARBY STATES 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-E 

PTepaTed in cooperation with the 

Comuwnwealth of Kentucky, 

University of Kentucky, 

Kentucky Geological Suroey 

DesC'riptions and illustrations of six species, 

with com'Jnents on their morphology and distribution 

CONTENTS 

Page 

Abstract --------------------------------------------------------------------------------------------------------------------------- E 1 

In trod u cti on ---------------------------------------------------------------------------------------------------------------------- 1 

S y sterna tic pal eon to I o gy ------------------------------------------------------------------------------------------------------ 1 

References cited ---------------------------------------------------------------------------------------------------------------- 6 

ILLUSTRATIONS 

PLATE 1. Carneyella, Streptaster, and Cystaster. 

2. lsorophus and Edri.oaster. 

Page 

FIGURE 1. Carneyella pilea (Hall) based on USNM 170362-----------------------------------------~------------ E 1 

2. Cystaste1· stellatus (Hall) based on USNM 206294 --------------------------------------------------- 2 

3. lsorophus cf.l. cincinnatiensis (Roemer), based on USNM 206296 and USNM 206297 ----- 4 

4. Edri.oaster priscu.s (Miller and Gurley), oral surface (based on USNM 206299) and lower 

side of theca with attachment structure (based on USNM 206299)-------------------------- 6 

CONVERSION FACTORS 

The investigations underlying this series of reports were made over a period of years, and distances 

and stratigraphic measurements appear fairly uniformly in English units. Measurements of fossil 

specimens, on the other hand, follow the longstanding convention of appearing in metric units. 

Because of the dates of the investigations and the amount of resulting data, the English measurements have been retained. Conversions to metric units may be made by using the following conversion 

table: 

To convert English unit: 

Mile (mi) 

Foot (ft) 

To metric unit: 

Kilometer (km) 

Meter (m) 

Multiply by: 

1.61 

.305 

III 
CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

EDRIOASTEROIDS (ECHINODERMATA) 

By BRUCE M. BELL I 

ABSTRACT 

Seven edrioasteroids that belong to six species are described. The 

new matel"ial revises the known geographic and stratigraphic ranges 

of the species and provides the first known specimen on which the 

entire attachment structure of Ed1·ioaste1· is preserved. No new taxa 

are described. 

INTRODUCTION 

Seven edrioasteroids were found during this investigation of the Ordovician of Kentucky and nearby States. 

Five are silicified through replacement of the calcareous 

plates by beekite; they were recovered from acid residues. Silicification has obliterated most sutures but has 

preserved the thecal shape. The other two specimens 

retain the primary calcareous composition of the plates. 

They were isolated from the bulk samples in the field 

and were not acidized. 

The seven specimens represent six known specjes. The 

specimens extend the range of their respective taxa. 

Moreover, one specimen shows a rare intraspecific variation, and another preserves an attachment structure 

previously quite poorly known. 

SYSTEMATIC PALEONTOLOGY 

Phylum ECHINODERMATA Bruguiere 

Class EDRIOASTEROIDEA Billings, 1858 

Order ISOROPHIDA Bell, 1976 

Suborder LEBETODISCINA Bell, 1976 

Family CARNEYELLIDAE Bell, 1976 

Genus CARNEYELLA Foerste, 1917 

Carneyella pilea (Hall, 1866) 

Figure I; plate I, figures 1-3 

Carneyella pilea has a domal theca averaging 16 mm 

in diameter in adults; it has three central primary oral 

plates and one large hydropore oral; the hydropore slit 

is in the right-posterior part of the oral area formed by 

the two proximal coverplates of the posterior side of ambulacrum V, the large hydropore oral, and the right edge 

of the large posterior primary oral; the ambulacra form 

'New York Stale Museum and Science Service. Published by permission of the Director. 

New York Slnle Museum and Science Service, Joumal Series No. 155. 

low rounded ridges and are curved (I-IV, contrasolarly; 

V, solarly); ambulacral terminations are confined to interambulacral areas; the ambulacral tunnel is low and 

wide; the ambulacral floorplates are uniserial and imbricate proximally; ambulacral coverplates are biserial and 

of moderate thickness; a coverplate passageway system 

connects the thecal cavity directly to the exterior of the 

theca; the passageways are oblique and their external 

foramina elliptical; the interambulacrals are squamose 

and imbricate; the anal structure is a periproct; the peripheral rim plates are geniculate; theca prosopon includes small nodes sparsely scattered over the interambulacrals and rim plates, and small perradial ridges on 

the ambulacral coverplates. 

Discussion.-Figure 1 shows USNM specimen 170362 

from USGS locality 6699-CO, Point Pleasant Tongue of 

the Clays Ferry Formation. 

This specimen retains the calcareous composition of its 

plates. It appears to have been attached directly to a 

FIGURE 1.-Carneyella pilea (Hall, 1866). USNM 170362. Oral surface, X 3.5. 

El 
E2 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

hardground substrate. The theca is nearly complete except for the interambulacral area, in which most plates 

are disrupted or missing. Many of the distal plates of the 

peripheral rim are hidden or absent. The exterior surface 

of the theca has been deeply etched, which has removed 

the surface detail and in some areas obscured plate boundaries. 

USNM 170362 seems to be a typical adult Carneyella 

pilea except for ambulacrum V, which is reversed and 

curves. contrasolarly. It appears that ambulacrum V has 

a small aborted branch which extends from the posterior 

side adjacent to the anal area. It is possible that this 

represents the primary axis of ambulacrum V, which 

stopped growing, whereas the secondary branch continued to lengthen and curve contrasolarly. It is also possible that this specimen is one of the extremely rare variants in which a primary ambulacrum has a reverse 

curvature. 

The direction of ambulacral curvature is generally constant at the generic level in edrioasteroids, and thus it 

is employed as a primary taxobasis. However, it is not 

a sole determinant, for a suite of characters comprise the 

taxobases of a species. The anomalous ambulacrum found 

in USNM 170362 does not exclude the specimen from 

Carneyella pilea; all other features bespeak C. pilea. 

This specimen is among the oldest known representatives of this species, which is most common in the later 

Ordovician. 

Family LEBETODISCIDAE Bell, 1976 

Genus CYST ASTER Hall, 1871 

Cystaster stellatus (Hall, 1866) 

Figure 2; plate l , figures 5, 6 

Cystaster stellatus has a small discoidal theca; adult 

thecal diameters are commonly 7 to 8 mm; three large 

primary orals are flanked laterally only by two pairs of 

shared coverplates; the hydropore is along the proximal 

part of the posterior side of ambulacrum V and is encompassed by the two proximal coverplates of the posterior 

side of ambulacrum V and two large interambulacrals, 

one interambulacral being larger than the other and having a prominent sickle-shaped ridge; the straight ambulacra are relatively broad; the ambulacral tunnel is high 

and narrow; the uniserial floorplates imbricate proximally; the thick, wide ambulacral coverplates form a hiseries; a coverplate passageway system connects the thecal cavity directly to the exterior of the theca; the 

passageways are nearly vertical, and their external foramina are elongate; the interambulacral plates are squamose and imbricate; the anal structure is a periproct; the 

peripheral rim plates are squamose; large, rounded, irregular nodes cover the interambulacral and rim plates. 

Discussion.-Figure 2 shows USNM specimen 206294 

from USGS locality 6699-CO, Pt. Pleasant Tongue of 

FIGURE 2.-Cystaster stellatus (Hall, 1866). USNM 206294. Oral surface, X 6. 

the Clays Ferry Formation (7.4 mm axial by 6.8 mm 

transverse diameter). 

This specimen is preserved retaining the primary calcareous composition of its plates. The theca is nearly 

complete. The interambulacrals are collapsed and partially disrupted, as is the periproct. The central sector 

of ambulacrum III is displaced somewhat to the left. The 

larger, posterior interambulacral plate of the hydro pore 

structure is displaced toward the anus. This displacement exposes the stone canal passageway. The theca has 

been extensively etched, which exposes subsurficial 

views of the plates, particularly the ambulacral cover- · 

plates. 

USNM 206294 is a typical Cystaster stellatus. It is one 

of oldest known specimens of the species, which is most 

common in the Cincinnatian Series. 

Family LEBETODISCIDAE Bell, 1976 

Genus STREPT ASTER Hall, 1872 

Streptaster vorticellatus (Hall, 1866) 

Plate l , figure 4 

Streptaster vorticellatus has a domal theca that averages 15 mm in diamc~er and is totally dominated by the 

exceptionally high ambulacra. Three large primary orals 

are flanked by two pairs of lateral shared coverplates 

and several secondary oral plates; the hydropore opens 

along the proximal part of the posterior side of ambulacrum V; the hydropore structure comprises the second 
EDRIOASTEROIDS (ECHINODERMATA) E3 

and third proximal coverplates of the posterior side of 

ambulacrum V and one large bulbous interambulacral. 

The ambulacra are all curved contrasolarly and dominate 

the theca; and the ambulacral tunnel is extremely high 

and narrow. The uniserial floorplates imbricate proximally; the coverplates are massive and so high that they 

are columnar; movable spines are mounted in basins atop 

the coverplates. The coverplate passageway system connects the thecal cavity directly to the thecal exterior 

through the vertical passageways. The external foramina are unusually elongate; the interambulacrals are 

squamose and imbricate; the anal structure is a periproct; the peripheral rim plates are geniculate; the rim 

and interambulacral plates are covered with large, 

rounded, irregular nodes. 

Discussion.-Plate 1, figure 4, shows USNM specimen 206295, from USGS locality 7790-CO, Millersburg 

Member of the Lexington Limestone (11.2 mm axial by 

10.4 mm transverse diameter). 

The specimen is silicified and preserves only the peripheral rim, the ambulacra, and the oral area. It is clear 

that the ambulacra are all curved in a contrasolar direction, but it is difficult to identify individual ambulacra; 

therefore, the specimen may be improperly oriented in 

the plate. 

Ambulacral disposition and the columnar coverplates 

favor placement of this individual in the genus Streptaster. That genus is believed to be monotypic, and thus the 

specimen apparently belongs to the type species Streptaster vorticellatus. This is the oldest known specimen 

of Streptaster; all other specimens come from the Cincinnatian Series. 

Suborder ISOROPHINA Bell, 1976 

Family ISOROPHIDAE Bell, 1976 

Genus ISOROPHUS Foerste, 1917 

Isorophus cincinnatiensis (Roemer, 1851) 

Figure 3; plate 2, figures 1-3 

I sorophus cincinnatiensis has a do mal theca that is 

commonly 20 to 25 mm in diameter; the four large central 

primary orals are flanked by two pairs of lateral shared 

coverplates, one large hydropore oral, and five or more 

secondary oral plates; the slitlike hydropore is in the 

right-posterior part of the oral area. Five plates constitute the hydropore structure--~he hydropore oral, the 

right edge of the large right-posterior primary oral, the 

right-posterior shared coverplate, and the first two primary posterior coverplates of ambulacrum V. The structure is integrated with the central oral rise. Ambulacra 

are curved (I-IV, contrasolarly; V, solarly); they are of 

moderate width and taper gradually distally. The floorplates are uniserial, and contiguous floorplates abut one 

another along vertical sutures; the ambulacral coverplates form a double alternating biseries of pairs-large 

primary and distinctly smaller secondary plates. Secondary coverplates rarely reach the external adradial suture 

line; interambulacrals are squamose and imbricate, interambulacral areas are of moderate size in proportion 

to thecal diameter. The valvular anal structure is formed 

by an inner and outer circlet of alternating large triangular plates; the plates of the peripheral rim are geniculate; the thecal plates are smooth. 

Discussion.-Figure 3A and plate 2, figures 1-2, 

show USNM specimen 206296 from USGS locality 4929-

CO, Grier Limestone Member of the Lexington Limestone, 8ft below the base of the Brannon Member of the 

Lexington Limestone (6.6 mm axial by 6.5 mm transverse diameter). 

This silicified edrioasteroid is attached to a brachiopod 

(Rafinesquina sp.) in which silicification has produced 

large beekite rings. The edrioasteroid is nearly complete; 

only interambulacral 1 and part of 3 have missing plates. 

The specimen is only partially depressed. Most sutures 

have been obliterated. 

Figure 3B and plate 2,. figure 3, show USNM specimen 

206297 from USGS locality 7454-CO, Millersburg Member·ofthe Lexington Limestone (5.1 mm axial by5.4.mm 

transverse diameter). 

Silicification of this specimen has obscured detail. The 

individual has been separated from its attachment site 

and the theca has been depressed, thereby accentuating 

the relative elevation of the ambulacral-oral structures. 

USNM 206296 and 206297 are both poorly preserved 

and cannot be assigned with assurance to any species. 

However, those features that can be recpgnized ~ll suggest I sorophus, and it is likely that both specimens belong to the type species, I. cincinnatiensis, in that it is 

the most common species of the genus and is also the 

only one reported from equivalent horizons. Features 

suggesting this assignment include the curvature, length, 

width, and elevation of the ambulacra, the proportionally 

large size of the oral area, the valvular anal structure, 

and the apparent shape and position of the hydropore 

structure. 

Order EDRIOASTERIDA Bell, 1976 

Family EDRIOASTERIDAE Billings, 1858 

Genus EDRIOASTER Billings, 1858 

Edrioaster bigsbyi (Billings, 1857) 

Plate 2, figures 4, 5 

E drioaster bigsbyi has a subgloboid theca with an invaginated base; adults are commonly 40 to 45 mm in 

diameter; the oral covering plates are similar to the ambulacral coverplates; the hydropore is in the posterior 

part of the oral area; the slitlike opening is elongate normal to the suture line between the two oral plates, which 

it penetrates. The ambulacra are curved (I-IV, contrasolarly; V, solarly); curvature is initiated above the am-
E4 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

A 

FIGURE 3.-/sorophus cf. /. cincinnatiensis (Roemer, 1851). A, USNM 206296, oral surface, X 6. 

B, USNM 206297, oral surface, X 7. Dashed lines represent likely sutures. 

bitus. The biserial ambulacral floorplates house a sutural 

passageway system that connects the thecal cavity to 

the ambulacral tunnel. The ambulacral coverplates are 

biserial and sit on top of the floorplates without intrathecal extensions. Interambulacral plates are large, polygonal, and tessellate; the anal structure is a periproct; the 

margin of the oral surface is a flexible polyplated membrane that extends from the distal edge of the basal invagination of the theca down to the substrate; the exterior surfaces of the theca plates are nodose. 

Discussion. -Plate 2, figures 4-5, shows USNM 

specimen 206298 from USGS locality 5022-CO, Curdsville Limestone Member of the Lexington Limestone 

(34.9 mm axial by 35.5 mm transverse diameter by 14 

mm high). 

This specimen is fragmentary. Most of the plates of 

the upper oral surface are gone, and those of the lower 

side of the theca are hidden by matrix. However, the 

distal parts of all the ambulacra are preserved near or 

just below the ambitus. Moreover, most of the upper 

oral surface parts of ambulacra I and V and interambulacra 4 and 5 are preserved. The theca apparently remained inflated after burial, and the thecal cavity is filled 

with crystalline calcite. This filling demonstrates the size 

and shape of the specimen even though most of the upper 

oral surface is missing. 

The ambulacral structure and disposition clearly establish that this specimen is an Edrioaster. Its large size 

and lack of any unusual features suggest it is a member 

of the type species, E. bigsbyi. This individual extends 

the geographic range of the species, which previously 

was known only in Ontario and Michigan. 

Edrioaster priscus (Miller and Gurley, 1894) 

Figure 4; plate 2, figures 6-9 

Edrioaster priscus is very similar to E. bigsbyi but is 

thought to be smaller (commonly 15 to 19 mm in diameter), to have smooth exterior surfaces on its plates, and 
EDRIOASTEROIDS (ECHINODERMATA) E5 

B 

FIGURE 3.-Continued. 

to have ambulacral curvature initiated below the ambitus 

of the theca. 

Discussion.-Figur~ 4 and plate 2, figures 6-9, show 

USNM specimen 206299, from USGS locality 5072-CO, 

basal Curdsville Limestone Member of the Lexington 

Limestone (18.8 mm axial by 17.6 mm transverse diameter). 

Silification of this specimen has obliterated most sutures. However, the theca remains inflated and preserves the shapes of individual structures. The right 

quarter of the theca is missing, as are all of the oral and 

ambulacral coverplates. Oth~r structures are intact. 

USNM 206299 clearly is an E drioaster priscus. (E. 

priscus is recognized only with question. Specimens assigned to this species may be young E. bigsbyi. A complete discussion of this problem may be found in Bell 

(1974). The specimen reveals not only the thecal shape, 

ambulacral disposition, anal periproct, and hydropore 

structure, but also preserves some of the ambulacral passageway structures of the biserial floorplates. 

This specimen provides the only clear look at the attachment structure of Edrioaster (fig. 4B). Other specimens have demonstrated the existence of a polyplated, 

flexible membrane that extended downward from the 

distal plates of the oral surface; these plates form the 

inner edge of the invaginated base of the theca. Until 

now, only small segments of this membrane have been 

observed. In this specimen the flexible collar is triangular in shape. This may reflect the shape of the object 

to which the animal was attached, or perhaps it is due 

to a slight constriction of the ring after it was pulled 

from its attachment area. The distal edge of the membrane appears to be slightly curled under. Silification has 

obliterated the boundaries between the tiny platelets 

that constitute the structure. The specimen also suggests the presence of a sole acrdss the base of the triangular collar. This membrane probably was not plated 

and may have acted as a sucker. If so, attachment may 

have been by suction rather than by fleshy connection 

·between the polyplated membrane and the substrate. An 

Edrioaster might have been able to release itself from 

its resting site, in contrast with all Isorophida, which are 

thought to have been permanently anchored to the substrate. 
E6 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

A 

FIGURE 4.-Edrioaster priscus (Miller and Gurley,· 1894). USNM 206299. A, Upper oral surface, X 4. B, Lower 

side of theca with attachment structure, X 4. 

REFERENCES CITED 

Bell, B. M., 1974, A study of North American Edrioasteroidea: New 

York State Mus. and Sci. Service Mem. 21,447 p., 65 text-figs., 

63 pls. [1976]. 

Billings, Elkanah, 1857, Report for the year 1856 [Fossils from Anticosti, and new species of fossils from the Lower Silurian rocks 

of Canada]: Canada Geol. Survey Rept. Prog. 1853-1856, p. 

247-345. 

__ 1858, On the Asteriadae of the Lower Silurian rocks of Canada: 

Canada Geol. Survey, Can. Organic Remains, decade 3, p. 9-

74, 2 text-figs., pls. 8-10. 

Foerste, A. F., 1916, Notes on Cincinnatian fossil types: Denison 

Univ., Sci. Lab. Bull., v. 18, no. 4, p. 285-355 [1917]. 

Hall, James, 1866, Descriptions of some new species of Crinoidea and 

other fossils from the Lower Silurian strata of the age of the 

Hudson River Group and Trenton Limestone: New York State 

Cabinet Rept. for 1866, advance print, 17 p. [for final publication, see Hall, 1872, below]. 

___ 1871, Descriptions of some new species of fossils, from the 

shales of the Hudson River Group, in the vicinity of Cincinnati, 

Ohio: New York State Mus. Ann. Rept. 24 (advance print) 8 p., 

4 pls. [final publication: New York State Mus. Ann. Rept. 24, 

p. 225-232, 1872]. 

__ 1872, Descriptions of new species of Crinoidea and other fossils 

from the strata of the age of the Hudson River Group and Trenton Limestone: New York State Mus. Ann. Rept. 24, p. 205-

224, pls. 5--8. 
EDRIOASTEROIDS (ECHINODERMATA) E7 

J 

.· -.. : .. . · .. ---.,.,., 

B 

FIGURE 4.-Continued. 

Miller, S. A., and Gurley, W. F. E., 1894, New genera and species of 

Echinodermata: Illinois State Mus. Nat. History Bull. 5, 53 p. ,. 

5 pls: 

Roemer, F. (C. F. von), 1851, Beitrage zur Kenntniss der fossilen 

Fauna des devonischen Gebirges am Rein: Decheniana (V erhandlungen des N aturhistorischen vereins Reinlande und Westfalens), v. 8, p. 357-376, pls. 7-8. 
PLATES 1 and 2 

Contact photographs of the plates in this report are available, 

at cost, from U.S. Geological Survey Library, Federal Center, 

Denver, Colorado 80225 
PLATE 1 

FIGURES 1--3. Carneyella pilea (Hall). (p. E 1). 

USNM 170362. 

1. Oral surface, whitened with ammonium chloride, X 6. 

2. Oral surface, in xylene, X 6. 

3. Ambulacrum V and adjacent areas, in xylene, X 12. 

4. Streptaster cf. S. vorticellatus (Hall). (p. E 2 ). 

USNM 206295. Oral surface whitened with ammonium chloride, X 5. 

5, 6. Cystaster stellatus (Hall). (p. E 2). 

USNM 206294. 

5. Crinoid base and edrioasteroid attached to hardground substrate; ambulacrum III of the edrioasteroid points toward 

the crinoid base; whitened with ammonium chloride, X 3. 

6. Oral surface, whitened with ammonium chloride, X 10. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 106&-E-PLATE I 

5 

CARNEYELLA, STREPTASTER, AND CYSTASTER 
PLATE 2 

FIGURES 1, 2. Isorophus cf. /. cincinnatiensis (Roemer). (p. E3). 

USNM 206296. 

1. The specimen attached to a brachiopod, Rajinesquina sp., the anterior of the edrioasteroid pointed west-northwest, 

whitened with ammonium chloride, X 3. 

2. Oral surface, whitened with ammonium chloride, X 7. 

3. Isorophus cf. /. cincinnatiensis (Roemer) (p. E 3). 

USNM 206297. Oral surface whitened with ammonium chloride, X 8. 

4, 5. Edrioaster bigsbyi (Billings) (p. E 3) 

USNM 206298. 

4. Oral surface, whitened with ammonium chloride, X 2. 

5. Lateral view, whitened with ammonium chloride, X 2. 

6-9. Edrioaster priscus (Miller and Gurley) (p. E4). 

USNM 206299. 

6. Oral surface, whitened with ammonium chloride, X 3. 

7. Lower side of theca, whitened with ammonium chloride, X 3. 

8. Lateral view, whitened with ammonium chloride, X 3". 

9. Flexible attachment ring, whitened with ammonium chloride, X 6. 
GEOLOG ICAL SU RVEY PROFESSIONAL PAPER 106&--E -PLATE 2 

2 

8 

6 

ISOROPHUS AND EDRIOASTER 
Asteroidea (Echinodermata) 

By .J. W. BRANSTRATOR 

CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY 

OF KENTUCKY AND NEARBY STATES 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-F 

Prepared in cooperation with the 

C01nn~onwealth of Kentucky, 

University of Kentucky, 

/{entucky Geological Survey 

Systematics and paleoecology of four species, with 

comments on two species of uncertain systematic position 

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON 1979 
j 
CONTENTS 

Page 

Albstract ----------------------------------------------------------------- F1 

Introduction ------------------------------------------------------------- 1 Alcknowledgments _____ ---------- __ _ _ __ __ __ __ _ _ __ __ ____ ___ _ ________ ___ ____ 1 

Terminology ------------------------------------------------------------- 2 

Systematic paleontology ___________________ -------------------- __ ___ ___ ____ 2 

Pron1opalaeasteridae -------------------------------------------------- 2 

Prontopalaeaster ------------------------------------------------- 2 

P1·omopalaeastcr .. speciosus _________________________ ----------- 2 

Promopalaeaste1· finei ____________ ------------ ____ --------- ____ 4 

Schuchertiidae _______________ : _____________ ---------------------- __ __ 4 

Lanthanaster ---------------------------------------------------- 4 

Lanthanaster intermedius ------------------------------------- 4 

Stenasteridae -------------------------------------------------------- 5 

Stenaster -------------------------------------------------------- 5 

Stenaster obtusus --------------------------------------------- 5 

Species inquirenda ---------------------------------------------------- 6 

References cited ---------------------------------------------------------- 6 

PLATE 1. 

2. 

3. 

ILLUSTRATIONS 

Pro1nopalaeaste1·. 

P-romopalaeaste'r, Stenaster. 

Lanthanaster, M esopalaeaster, Species Inquire-nda. 

SYSTEM OF MEASUREMENT UNITS 

The investigations underlying this series of reports were made over a period of 

years, and distances and stratigraphic measurements appear fairly uniformly in 

English units. Measurements of fossil specimens, on the other hand, follow the longstanding convention of appearing in metric units. Because of the dates of the investigations and the amount of resulting data, the English measurements have been retained. Conversions to metric units may be made by using the following conversion 

table: 

To convert 

English unit: 

Mile (mi) 

Foot (ft) 

To metric unit: 

Kilomete-r (km) 

Meter (m) 

Multiply 

by: 

1.61 

.305 

III 
CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

ASTEROIDEA (ECHINODERMATA) 

By J. w. BRANSTR~TOR 1 

ABSTRACT 

Specimens belonging to the stelleroid genera Promopalaeaster, Lanthanaster, and Stenaster have been obtained from 

Kentucky's Middle and Upper Ordovician rocks. Promopalaea::~te?· speciosus (Meek) is a subjective senior synonym of P. 

prenuntius Schuchert. Lectotype and paralectotype specimens 

are designated from the syntypes of Palaeaster finei Ulrich 

and Mesopalaeaster proavitus Schuchert; both type suites 

are composed of immature specimens of Promopalaeaster 

finei (Ulrich) n. comb. By subjective synonomy, Mesopalaeaste?· 1:nterm,edius ( Schuchert) n. comb. replaces Lanthanaster cnwifonnis as the type species of Lanthanaster Branstrator. The generic affinities of "Hudsonaster milleri" 

Schuchert and "Mesopalaeaster? dubius" (Miller and Dyer) 

Schuchert cannot be determined from available materials. 

INTRODUCTION 

Verrill (1914, p. 17) noted that a particular difficulty in the determination of genera and species of 

starfishes is that many do not attain their adult or 

diagnostic characteristics until of· considerable size. 

Thus, young individuals of a species may appear to 

belong to different species, or even different genera, 

unless they can be compared with individuals in a 

growth series. I have attempted to piece together 

growth series for the fossil starfish species known 

from North America. This report deals with the results as applied to specimens from Kentucky. 

Most asteroid specimens from the later Ordovician strata in Kentucky belong to species, des·cribed 

previously, from Cincinnati and southwestern Ohio. 

Geographic and lithostratigraphic data accompanying the type and supplementary specimen material 

from Ohio are usually poor, however. Kentucky's 

ea;rlier Ordovician rocks have no time-equivalent 

strata exposed in the classic collecting sites in adjacent states. Some specimens from these earlier 

rocks belong to species described from ostensibly 

time-equivalent and lithologically similar strata in 

1 Earlham College, Richmond, Ind. 

southeastern Canada and the British Isles. Although 

c.ommonly coarsely recrystallized or disarranged 

during preservation, new specimens of Promopalaeaster finei, Lanthanaster intermedius, and Stenaster obtusus from Kentucky are most valuable because of the fine lithostratigraphic control with 

which they were collected. These specimens shed 

light on the succession and paleoecology of species 

originally described from elsewhere. 

Museum's from which specimens were borrowed 

have their names abbreviated as follows: U.S. National Museum of Natural History-USNM; Museum of Comparative Zoology, Harvard University-MCZ; University of Kentucky-UK; Yale 

University Peabody Museum-YPM; American 

Museum of Natural History-AMNH; Field Museum of Natural History-FM; University of Michigan, Museum of Paleontology-UM; and University of Cincinnati, Geology Museum-UC. 

ACKNOWLEDGMENTS 

John Poj eta provided silicified and nonsilicified 

specimens collected as part of the U.S. Geological 

Survey-Kentucky Geological Survey Cooperative 

mapping program. F. J. Collier lent type and supplementary specimens from the National Museum of 

Natural History. Porter M. Kier and Thomas 

Phalan, also of USNM, provided assistance and advice in utilizing the collections of that institution. 

Norman D. Newell and Roger Batten supplied spedmens from the American Museum of Natural History. Eugene S. Richardson, Jr., and Matthew H. 

Nitecki provided specimens and collection data from 

the Field Museum of Natural History. John K. Pope 

of Miami University and Lois Campbell of the University of Kentucky lent important specimens. Robert Kesling arranged for a loan of a specimen from 

the University of Michigan Museum of PaleontolFl 
F2 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

ogy. Richard A. Davis allowed the author to borrow 

and curate many specimens from the University of 

Cincinnati Geology Museum. Kenneth E. Caster 

provided consultation and invaluable library resources. Frederic Hotchkiss and John Poj eta offered 

additional data and helpful criticism. The Joseph 

Moore Museum at Earlham College provided research facilities for the completion of this project. 

TERMINOLOGY 

Spencer and Wright (1966, p. 28-30) provided a 

useful glossary of morphological terms applied to 

asterozoans. Their terminology is used herein, with 

exceptions and additions as follows: Brachium is 

used interchangeably with arm. Odontophore refers 

only to one of the ossicles functionally involved in 

the operation of the mouth frame. This particular 

ossicle is seldom visible on the external skeletal surface of fossil specimens, and many authors incorrectly refer to any unpaired, exposed axillary inferomarginal as an odontophore. Perradial indicates 

a feature on or near a vertical plane that would 

longitudinally bisect each brachium. Abradial indicates a position relatively away from this plane. 

Brachial length ( R) is oommonly used to denote 

size in stelleroids. It is the mean distance between 

the geometric center of the disc and each arm tip. 

Only an approximate value for this parameter is 

possible for most fossil specimens because they are 

commonly fragmental or distorted from their living 

pr.opor.tions. 

Systematic Paleontology 

Family PROMOPALAEASTERIDAE Scbuchert, 1914 

Genus PROMOP ALAEASTER Schuchert, 1914 

Palaeaster [part], 1868-1914. 

Mesopalaeaster Schuchert [part], 1914, p. 24-25; [part], 

1915, p. 74-77. 

Promopalaeaster Schuchert [part], 1914, p. 5-6, 33-34; 

[part], 1915, p. 102-106. 

Spencer [part], 1916, p. 91-92. 

Spencer and Wright [part], 1966, p. 53. 

Anorthaster Schuchert, 1914, p. 5-6, 11-12; 1915, p. 125-126. 

Spencer and Wright, 1966, p. 53. 

Diagnosis.-Asteroids with all external ossicle 

surfaces having numerous, prominent spine-base 

pustules, each pustule carrying or having carried, a 

single articulating spine; paxillae never present. All 

primary columns of ossicles prominent throughout 

life. Intermarginal and adradial ossicles arranged 

in longitudinal columns as well as transverse rows. 

More prominent transverse rows of intermarginals 

alternate with less prominent ones. Podia! pores 

abradial to ambulaeral ossicle· bodies at junctions 

of ambulacral and adambulacral ossicle columns. 

Proximal podial cupules quadriserial; distal podial 

cupules biserial. 

Type species.-Palaeaster speciosus Meek (1872) ; 

by original .designation of Schuchert (1914) as 

"Palaeaster granulosus Meek" [ =Palaeaster speciosus Meek]. 

Promopalaeaster speciosus (Meek, 1872) 

Plate 1, figures 1-.3 

Palaeaster granulosus? Hall. Meek, 1872, p. 227; 1873, p. 

60-61, pl. 4, figs. 3a-c. 

Palaeaster speciosus? Meek, 1872, p. 227; 1873, p. 60-61, pl. 

4, figs. 3a-c. 

P'romopalaeaster prenuntius Schuchert, 1915, p. 107-108, pl. 

13, fig. 3; pl. 15, fig. 5. 

P1·omopalaeaster speciosus (Meek). Schuchert, 1914, p. 34; 

1915, p. 109-112, pl. 14, figs. 3-4; pl. 15, figs. 1-4. 

Spencer and Wright, 1966, p. 53. 

Diagnosis.-Promopalaeaster with intermarginal, 

but not adradial accessory ossicles arranged in alternately prominent transverse rows. Intermarginals and adradials tumid and nearly as massive 

as adjacent ossicles of primary ·columns; not substantially excavated on ossicle margins. 

Materials and occurrence.-The holotype MCZ 

22, Dyer Colin.) is from Cincinnati, Ohio. No additional stratigraphic or locality data accompany the 

specimen or are included in Meek's description. 

Schuchert (1915, p. ll0-111) states unequivocally 

that the specimen was ·collected "in the Maysvillian 

at Cincinnati, Ohio." Although no specific reason 

exists to doubt this information, its authenticity 

cannot be documented, and it must be regarded as 

an inference on Schuchert's part. 

Promopalaeaster prenuntius Schuchert (1915, 

107-108) is a subjective synonym of P. speciosus. It 

was described from its holotype (UK 403), which 

was found in a coarse calcarenite in the Lexington 

Limestone (Middle Ordovician part) near Frankfort, Ky. A brachial fra.gment of another individual 

(YPM 3405) came from the same area and is similarly preserved. Natural molds of eight poorly preserved individuals in a calcarenitic slab (AMNH 

1100) labeled "Hudson River Group [Upper Ordovician], near Rome, New York" considerably extend 

the geographic range of P. speciosus. 

Description.-Known specimens of P. speciosus 

range in size from R~20 mm (Rome, N.Y. specimen) ·to R = 44 mm (the holotype) . Both Kentucky 

specimens have brachial lengths near 35 mm. 

Dorsal and ventral aspects are available from the 

P. speciosus holotype (pL 1, figs. lA-C). The specimen is ·composed of two, nearly complete, adjacent 

brachia, which meet at their bases in an acute angle. 

Each arm tapers slowly to a broadly acuminate tip. 
ASTEROIDEA (ECHINODERMATA) F3 

One open ambulacral groove· is clear of matrix and 

shows details of ambulacral ossicle structure and 

arrangement. 

Each ambulacral ossicle possesses a prominent 

ventral carina. Perradial nodes (pl. 1, fig. lC) on 

the ventral carina are also prominent, and form deep 

ambulacral channels for the lengths of the brachia. 

The ventral carinae on the distal half of each 

brachium are straight and define two columns of 

podial cupules in the a.mbulacral groove. On the 

proximal portion of each brachi urn the ventral 

ambula.cral carinae lie alternately diagonally on the 

ambulacral ossicles and form. four longitudinal 

columns of cupules. Dentition, or hinge structure, 

marks abutting surfaces between opposite ambulacral ossicles of adjacent columns. Contact with the 

adjacent adambulacral ossicle is by means of a 

prominent abradial flange on the ventral carina of 

each ambulacral ossicle. Most of the ossicle body of 

each ambulacral ossicle overlies the proximal portion of the next more distal ossicle. 

The intermarginal ossicles of P. speciosus are arranged in longitudinal columns as well as diagonally 

transverse rows. Close examination reveals that 

these rows are co·mposed of ossicles in two size 

groups. A row of small ossicles intercalates between 

each row of larger ossicles (pl. 1, fig. lA), and one 

of these paired series occurs for each inferomarginal and corresponding superomarginal on the 

lateral surface of an arm. This biserial intermarginal condition is common to all promopalaeasterids, 

but the intermarginals of P. speciosus are relatively 

more massive and carried many more spines than 

those of other promopalaeasterid species. 

Like the intermarginals, the adradial ossicles of 

this species are relatively massive and carried many 

more spines than similar ossicles of other promopalaeasterids. Abradial adradials of P. speciosus are 

at least as prominent as adj 3!cent superomarginals 

(pl. 1, figs. lA-B). The adradials are excavated only 

slightly at their margins for the accommodation of 

dermal papulae. Furtherm~ore, the paired subseries 

arrangement common to the adradials of other 

promopalaeasterids and the intermarginals of all 

promopalaeasterids does not occur in this species. 

Discussion.-The Kentucky specimens of P. 

speciosus, from the Lexington Limestone, are probably older than the holotype and New York specimens, as much of the Lexington Limestone is Middle Ordovician and the New York specimens are 

Late Ordovician in age. Schuchert (1915, p·. 107) 

assumed the holotype of his P. prenuntius to be disstinct from P. speciosus because of its "smaller size, 

less pustulose ornamentation of the plates, and lower 

position in the geological column." These are not 

tenable criteria for species differentiation among 

asteroids. 

Overall size, arm length, disc width, number of 

ossicles in a particular brachial column, number of 

intercalating ossicles in a brachial column, and 

number of intercalating columns-all increase with 

maturity in asteroids. The "pustulose ornamentation" referred to by Schuchert in distinguishing P. 

prenuntius from P. speciosus is simply an indication of overall spinosity of an individual. Spinosity 

varies intraspecifically in asteroids and, in fact, increases with size in some genera (Rasmussen, 

196.5) . Hence, the morphological characteristics 

used by Schuchert to distinguish P. prenuntius from 

P. speciosus may be useful in describing individuals, 

but they should be avoided in species characterization, unless the maturity of the examined specimens 

can be determined by comparison with other individuals in a growth series. Without substantiating 

morphological evidence, the stratigraphic occurrence criterion Schuchert used to distinguish his 

new species is meaningless. 

The holotype, UK 403, presents a ventral aspect 

that reveals details of ambulacral ossicle structure. 

Quadriserial podia! cupules occupy less of the arm 

lengths in this less mature sp·ecimen than they do 

in the larger P. speciosus holotype. An overturned 

arm tip (pl. 1, fig. 2) reveals that the specimen 

possesses the adradial ossicle condition unique to 

this species of Promopalaeaster. 

The Lexington Limestone specimens show the 

fenestrate nature of the ossicles. The coarse calcarenitic matrix imposed some distortion to the 

ossicle surfaces, but has allowed differential 

weathering of replaced stereom and stromal canal 

filling. Spines (pl. 1, fig. 3) and ossicles of these 

early asteroids had internal microstructures similar 

to those of modern echinoderms. 

Paleoecology.-Where matrix is available with 

specimens of P. speciosus (ail but the holotype), it 

is calcarenite, rather than the fossiliferous calcilutite found with the other species of the genus. The 

internal ampullae, the primary organs of respiration in modern asteroids, were connected remotely 

to the external podia in the promopalaeasterids. 

This imposed a respiratory inefficiency on this system in thes·e early forms (Branstrator, 1975). 

Furthermore, the alternate organs of respiration in 

asteroids, dermal papulae, were not well developed 

in this species. P. speciosus probably inhabited relatively high energy, oxygen-rich areas. 
F4 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Promopalaeaster finei (Ulrich, 1879) n. comb. 

Plate 1, figures 4-9; plate 2, figures 1-6 

Palaeaster finei Ulrich, 1879, p. 19, pl. 7, figs. 15a-b. 

Mesopalaeaster finei (Ulrich). Schuchert, 1914, p. 25; 1915, 

p. 81-82, pl. 7, fig. 5; pl. 9, fig. 5. 

Mesopalaeaste1· proavitus Schuchert, 1915, p. 83-84. 

Diagnosis.-Promopalaeaster with intermarginal 

and adradial accessory ossicles arranged in alternately prominent transverse rows. Interma.rginal 

and adradial ossicles less massive than adjacent 

ossicles in primary columns; substantially excavated 

on ossicle margins. 

Materials and occurrence.-The syntype material 

of Palaeaster finei Ulrich, 1879 (USNM 60604) is 

from the Upper Ordovician "Eden Shale" ( = Kope 

Formation) in ·eastern Cincinnati, Ohio. The lectotype is herein designated as the specimen figured on 

plate 2, figure 1 of this report; it has been circled 

on its slab by this author to distinguish it from other 

syntypes, which becom·e paralectotypes. Ulrich's 

original suite may have included YPM 14779, but 

because this is uncertain I am excluding these latter 

specimens from paralectotype designation. 

William H. White, Jr., of Milford, Ohio, found a 

number of small specimens eve 40371-40383) in the 

Kope Formation at the junction of Beechmont and 

Elstun Avenues in eastern Cincinnati. USNM 

236052 is from USGS locality 6419-CO (Logana 

Member of the Lexington Limestone). The syntypes 

of Mesopalaeaster proavitus Schuchert (1915) 

( FM 54069, Walker Colin.) are from the "Eden 

Shale" ( = Kope Formation) at Covington, Ky. The 

largest specimen (pl. 1, fig. 4) in the suite is herein 

designated as the lectotype of Schuchert's M. proavitus; the remainder of the syntype specimens become paralectotypes (pl. 1, fig. 5). M. proavitus 

material has not been figured previously. UM 6230 

cam·e from Cincinnati, but its stratigraphic occurrence is unknown. UC 40758, Winnes Colin. (pl. 1, 

fig. 9), is from an undetermined stratum near 

Augusta, Ky. Two coarsely silicified specimens, 

USNM 236051 and 236050 {pl. 2, fig. 5), are known 

from USGS locality 6134_.CO (Clays Ferry Formation). AMNH 1196 and USNM 92613 are from undetermined strata in Cincinnati, Ohio, and Covington, Ky., respectively. Finally, USNM 236049 is 

from USGS locality 6803-CO (Grier Limestone 

Member of the Lexington Limestone) . 

Description.-The specimens listed after the type 

material above are in order of increasing size. They 

range from R=2 mm (UC 40378), through the 

juvenile P. finei lectotyp'e with R = 9 mm, to USNM 

236049 with a brachial l·ength greater than 40 mm. 

The generic and specific diagnoses serve to distinguish P. finei from other Kentucky asteroids. 

The numerous specimens of various sizes make 

available som·e important information on skeletal 

ontogeny in this promopalaeas~terid. The nonadaxial 

relationship between the axial and extraxial skelton 

is apparent frnm the smallest of juvenile growth 

stages; there are always more adambulacral 

ossicles than inferomarginal ossicles in adjacent 

columns (pl. 1, figs. 5, 7; pl. 2, figs. 1, 2B, 3B, 4, 

6A) -this characteristic is useful in distinguishing 

all growth stages of this genus from those of Mesopalaeaster, which always has 1-to-1 ratio of ossicles 

in adjacent adambulacral and inferomarginal columns. Adoral carinae are absent in small individuals 

(pl. 2, fig. 6A), but develop in specimens over 20 

mm (pl. 2, fig. 2B). Unpaired axillaries become isolated from the ambitus by radial length 6 mm (pl. 2, 

fig. 6A), and become progressively mor'e isolated 

throughout growth (pl. 2, fig. 2B, lower axil). The 

youngest specimens (less than 3 mm) do· not hav·e 

adradial or intermarginal accessory ossicles, but 

both kinds of ossicles are present by R = 5 mm and 

increase in number throughout growth (pl. 2, figs. 

6B-D, 2A, 3A; pl. 1, figs. 4, 6, 8, 9). Mature specimens of M esopalaeaster developed no more than 

two or three columns of intermarginal ossicles {pl. 

3, fig. 4) ; juvenile Promopalaeaster are difficult to 

distinguish from this latter genus when only dorsal 

aspects are available. 

Paleoecology.-This species appears to have been 

adapted to a less oxygenated habitat than P. speciosus. Quadriserial podia occupied more of the 

brachial lengths in P. finei. Individuals of all sizes 

possessed numerous large papulae protruding 

through pores in the dorsal and lateral wall; these 

were necessary to supplement podial respiration. 

All specim,ens of P. finei are in, or appear to have 

come from, a calcilutite or mi~ed calcilutite-calcarenite matrix suggestive of quieter waters than 

the calcarenite matrix of P. speciosus. 

Family SCHUCHERTIIDAE Schuchert, 1915 

Genus LANTHANASTER Branstrator. 1972 

Lanthanaster Intermedius (Schuchert, 1915) n. comb. 

Plate 3, figures 1-3 

Mesopalaeaster intermedius Schuchert, 1915, p. 79-81, pl. 9, 

fig. 4. 

Lanthanaster cruciformis Branstrator, 1972, p. 66-69, pl. 1. 

Diagnosis.-Stelleroid possessing only ambulacral, 

adambulacral, and inferomarginal primary ossicles 

in the brachia. Dorsal skeleton of small cruciform 

·Ossicles, each surmounted by a single articulating 

spine. Ambulacral ossicles dorsoventrally flattened 

except for a high ventral carina. Ampullar pores at 
ASTEROIDEA (ECHINODERMATA) F5 

junctions of ambulacral and adambulacral columns. 

Few short, broad spines on low spine-base pustules 

on inferomarginals and large, deltoid ventral interbrachials. Madreporite on ventral surface. 

Materials and occurrence.-The holotype (FM 

9575, Faber Colin.) is from rocks of Maysvillian 

Age at Cincinnati, Ohio. The holotype of the synonymous species Lanthanaster cruciformis Branstrator (1972), UC 6433, is also from MaysvillianAge rocks in Cincinnati. Another Cincinnati specimen (USNM 92608) came from the Kope Formation. Silicified fragments of at least five small individuals (USNM 236053) have been etched from the 

upper part of the Clays Ferry Formation at USGS 

locality 6143....:co. 

Desc'ript?:on.-The holotype (pl. 3, fig. 1) is fragmental and shows portions of the ventral surfaces 

of two brachia. Its brachial length is nearly 14 mm. 

The more mature University of Cincinnati specimen 

possesses all five brachia, shows both dorsal and 

ventral surfaces, and is more ·than twice the size of 

the holotype. The other known specimens are smaller 

and less well preserved than either of these. 

The University of Cincinnati specimen best shows 

the cruciform dorsal ossicles and dorsal (pl. 3, fig. 

2B) and ventral (pl. 3, fig. 2A) spines. No spines 

are preserved with the holotype, nor are any cruciform dorsal ossicles apparent. The Kentucky specimens (pl. 3, figs. 3A-C) are too coarsely recrystallized to pres·erve well either of these characteristics. 

The madreporites of the Kentucky specimens (pl. 

3, fig. 3B) are more tumid than that of the University of Cincinnati specimen (pl. 3, fig. 2A), but 

this may be an ontogenetic diff·erence. Other than 

this difference, the newly recognized Ohio and 

Kentucky specim·ens confirm my earlier description 

of this species (Branstrator, 1972, p. 66-68). 

Schuchert's supposition (1915, p. 81) that the hidden dorsal surface of his specimen, was similar to 

that of MesopalaeasteT was an error. 

Discussion.-Schuchert (1915, p. 80) believed his 

species to be an interm·ediate form between the species he included in Hudsonaste1· and M esopalaeaster. 

The single, large, marginal, ventral interbrachial 

ossicle (characteristic of H udsonaster) , the wide 

ambulacral groove (a feature he believed common 

to P1·omopalaeaste1· species) , and the ambulacral 

ossicles of a form "known in M esopalaeaster" make 

a paradoxical combination best reconciled (to Schuchert's thinking) by the supposition that his new 

spec'ies was an evolutionarily intermediate form. The 

axillary intermarginals, while single as in Hudsonaster, are not otherwise similar to those of that 

genus. Lanthanaster axillary intermarginals are deltoid, possess few, scattered spine-base pustules, 

and are widest orad of their midlength; Hudsonaste1· 

axillaries are sagittate, have many, crowded spinebas'e pustules, and are widest distal to their midlength. Had Schuchert known of the distinctive 

dorsal ossicles and of the ventral madreporite in the 

species that his specimen represented, he would not 

have placed it in M esopalaeaster. 

I did not recognize Sch uchert' s error in placing 

his specim,en among the M esopalaeaster prior to my 

description of Lanthanaster cruciformis. I have 

subsequently examined Schuchert's holotype and 

found that it must be included in the same species 

as the specimen I described. Schuchert's trivial name 

has priority, but the species does not belong in 

M esopalaeaste1· or any genus erected prior to 

Lanthanaster. 

Paleoecology.-Until the ecological significance of 

the ventral madreporite is known, it will be difficult 

to determine the paleoecology of Lanthanaste1·. The 

Kentucky specim,ens are from a unit reported to be 

representative of outer infralittoral (Cressman and 

Karklins, 1970, p. 21). The cruciform ossicles provided a fenestrated dorsal surface, probably as an 

aid to papular respiration-a necessity in an infralittoral habitat. 

Family STENASTERIDAE Schuchert, 1914 

Genus STENASTER Billings, 1858 

Stenaster obtusus (Forbes, 1848) 

Plate 2, figures 7, 8 

Uraster obtusus Forbes, 1848, p. 463; 1849, p. 2, pl. 1, fig. 3. 

Stenaster salteri Billings, 1858, p. 78, pl. 10, fig. 1a. 

Schuchert, 1915, p. 165-166, p. 32, fig. 1. 

Stenaster obtusus (Forbes). Sturtz, 1886, p. 152; Spencer, 

1914, p. 23, pl. 1, figs. 6-7; Schuchert, 1915, p. 167; 

Spencer, 1927, p. 356-359, pl. 23, figs. 1-9; pl. 24, 

fig. 10; Fedotov, 1936, p. 10-17, pl. 1, figs. 3-6; Spencer 

and Wright, 1966, p. 82, text figs. 70, 2a-d. . 

Diagnosis.-Only ambulacral and adambulacral 

primary ossicles in the brachial skeleton. Dorsal 

skeleton of minute granules originally invested in an 

integument, but commonly not apparent in fossils. 

A deep groove between opposite pairs of dorsoventrally thick ambulacral ossicles accommodated the 

radial vessels. 

Materials and occurrence.-The holotype is a 

mold in a mudstone of Caradocian Age from Wat,erford, Ireland. Spencer (1927, pl. 23, fig. 8) illustrated a cast of the specimen. He also included in 

the species specimens from the Cardocian of Bala, 

Wales, the Ashgillian of Scotland, and North Ameri-
F6 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

can specimens referred to Stenaster salteri Billings 

by Schuchert (1915, p. 165-166). Most North 

American specimens come from Ontario, where S. 

obtusus is common in the Hull Limestone (Middle 

Ordovician) at the Kirkfield quarries. In addition, 

Marshall Kay found a well-preserved specimen in 

the Long Point Limestone (Middle Ordovician), 

Newfoundland. Fedotov (1936) reported it from 

two Middle Ordovician localities in Kazakhstan 

(U.S.S.R.). 

Three coarsely silicified brachial fragments of 

Stenaster cf. S. obtusus (USNM 263054) have been 

etched from the Curdsville Limestone Member of the 

Lexington Limestone at USGS locality 5101-CO. 

Schuchert (1915, p. 166) report~ed that Ulrich obtained four isolated brachial fragments from the 

same rock unit near Curdsville, Ky. 

Description.-Beekite has replaced the calcitic 

stereom in the USNM 263054 specimens, but the 

diagnostic characteristics of the primary ossicles are 

apparent (pl. 2, fig. 8). Only ambulacral and adambulacral ossicles are present, and the deep groove 

that accommodated the radial vessels is apparent. 

The typical asteroid dorsal skeleton of massive 

primary and intercalated ossicles is absent in Stenaster. The dorsal integument was ossified by small 

elongate granules (Ruedemann, 1916, p. 54) that are 

commonly not apparent in fossils. A specimen (UC 

36426) from Kirkfi·eld, Ontario, retains some of 

these granules (pl. 2, fig. 7), but they are not ap ... 

parent on the Kentucky specimens owing to poor 

pres,erva tion. 

The Curdsville Limestone Member of the Lexington from which the Kentucky specimens· were extracted is reported to have been a calcarenite de ... 

posited in littoral and infralittoral zones (Cressman 

and Karklins, 1970, p. 18). The Welsh specimen is 

also preserved in a calcarenite. The peculiar disarrangement of individuals in the rich faunas associated with ·the Kirkfield, Ontario, and the Scottish 

specimens suggest that they were swept some distance and then buried as the results of storms. 

Species inquirenda 

Plate 3, figures 5-8 

Several asteroid specimens of indeterminable affinities are known from Kentucky rocks and deserve 

mention because they have' been designated holotypes of species or have been mentioned in the 

literature. 

The holotype of "Hudsonaster milleri" Schuchert 

(1915), UK 1344, shows its ventral surface and is 

preserved in a recrystallized calcarenite of the lower 

part of the Lexington Limestone in Fayette County, 

Ky. Parts of four brachia remain, although preservation is poor and taxonomically significant details 

have been obs~cured. The large axial inferomarginals 

(pl. 3, fig. 5}, which did not function as odontophores, suggest that Schuchert's generic placement 

of the specimen was incorrect because axillary inferomarginals are odontophores in Hudsonaster. 

Schuchert (1915, p. 60) conditionally placed a 

coarsely silicified specimen (YPM 13178) found at 

Curdsville, Ky., in Hudsonaster narrawayi (Hudson), 1912 [ =Protopalaeaster narrawayi Hudson] 

because it posseses a smaller disc, a stouter appearance, and smaller axillary ossicles than other specimens of that species known to· him. The specimen 

(pl. 3, figs. 6A-B) has a few adradial and intermarginal ossicles on its dorsal surface, however, 

which suggests that it is a developmental form of 

Promopalaeaster. The suite of young P. finei donated 

to University of Cincinnati by William H. White, Jr., 

shows such a hudsonasterid-like stage in the very 

early postlarval development of that specie's. 

Schuchert (1915, p. 62) reported a specimen 

(USNM 60617, Ulrich Colin.) of "Hudsonaster incomptus" from the "Maysville formation" south of 

Covington, Ky. The specimen is disarranged and 

abraded, however, and generic determination is 

impossible. 

A specimen (MCZ 25) from the "river quarries" 

(Point Pleasant Tongue of the Clays Ferry Forma,... 

tion) at Ludlow, Ky., was designated the holotype 

of "Palaeaster ?dubius" Miller and Dyer (1878). 

More of this specimen (pl. 3, fig. 7) has been rendered from its matrix since its original description, 

but still no diagnostic characters can be seen. It 

appears to be an asteroid and therefore distinct from 

a poorly preserved oegophiurid (YPM 11771) from 

the same quarries. The oegophiurid specimen (pl. 

3, fig. 8) has unusually long mouth-angle ossicles, 

distinct tori, and long narrow ambulacral ossicles. 

REFERENCES CITED 

Billings, Elkanah, 1858, On the Asteriadae of the Lower 

Silurian rocks of Canada: Canada Geol. Survey, Canadian Organic Remains, decade 3, p. 75-85, pis. 8-10. 

Branstrator, J. W., 1972, Lanthanaster crucijormis, a new 

Upper Ordovician sea star from Cincinnati, Ohio: Jour. 

Paleontology, v. 46, no. 1, p. 66-69, pl. 1. 

--1975, Podia! efficacy of some Ordovician asteroids 

(Echinodermata) from North America: Bulls. Am. 

Paleontology, v. 67, no. 287, p. 57-69, 2 pls. 

Cressman, E. R., and Karklins, 0. L., 1970, Lithology and 

fauna of Lexington Limestone (Ordovician) of central 

Kentucky, Field trip number 2, in Geological Society of 
ASTEROIDEA (ECHINODERMATA) F7 

America, southeastern Section, 18th Annual Meeting, 

Lexington, Kentucky guidebook for field trips: Lexington, Ky., Kentucky Geol. Survey: p. 17-28. 

Fedotov, D. M., 1936, Zur morphologie und evolution der 

seesterne und Ophiuren des unteren Silur: Akad. Nauk 

SSSR Inst. Paleozool. Trudy, v. 5, p. 3-33, 2 pls. 

Forbes, E., 1848, On the Asteriadae found fossil in British 

strata: Great Britain Geol. Survey Mem., v. 2, pt. 2, 

p. 457-482. 

---1849, British organic remains: Mem. Geol. Survey 

United Kingdom, dec. 1, p. 2, pl. 1. 

Hudson, G. H., 1912, A fossil starfish with ambulacral cove·ring plates: Ottawa Naturalist, v. 26, p. 21-26, 45-52, 

pls. 1-3. 

Meek, F. B., 1872, Descriptions of two new starfishes and a 

crinoid from the Cincinnati Group of Ohio and Indiana: 

Am. Jour. Sci., 3d ser., v. 3, no. 16, p. 257-262. 

---1873, Descriptions of the invertebrate fossils of the 

Silurian and Devonian systems: Ohio l)iv. Geol. Survey 

Paleontology, v. 1, p. 1-243, pis. 1-23. 

Miller, S. A., and Dyer, C. B., 1878, Contributions to palaeontology, no. 2: Cincinnati, Ohio, J. Barclay, (Independent 

publication). 

Rasmussen, B. N., 1965, On taxonomy and biology of the 

north Atlantic species of the asteroid genus Henricia 

Gray: Danmarks Fiskeri- og Havundersoegelser, Medd. 

new series, v. 4, no. 7, p. 157-213. 

Ruedemann, Rudolf, 1916, Paleontologic contributions from 

the New York State Museum: New York State Bull., 

no. 189, 225 p., 36 pls. 

Schuchert, Charles, 1914, Stelleroidea palaeozoica, in Frech, 

F., ed., Fossilium Catalogus, I, Animalia, part 3: Berlin, 

W. Junk, 53 p. 

---1915, Revision of Palaeozoic Stelleroidea with special 

reference to North American Asteroidea: U.S. N atl. 

Mus. Bull., no. 88, 311 p., 38 pls. 

Spencer, W. K., 1914, A monograph of the British Palaeozoic 

Asterozoa part 1: London, Pala.eontographical Society, 

p. 1-56, pl. 1. 

---1916, A monograph of the British Palaeozoic Asterozoa, part 2: London, Palaeontographical Society, p. 

57-108, pis. 2-5. 

---1927, A monograph of the British Palaeozoic· Asterozoa, part 7: London, Palaeontographical Society, p. 

325-388, pls. 23-24. 

Spencer, W. K., and Wright, C. W., 1966, Asterozoans, in 

Moore, R. C., ed., Treatise on invertebrate paleontology, 

part U, Echinodermata 3, volume 1: New York and 

Lawrence, Kans., Geol. Soc. America and Univ. Kansas 

Press, p. 4-107. 

Ulrich, E. 0., 1879, Descriptions of new genera and species 

of fossils: Cincinnati Soc. Nat. History Jour., v. 2, p. 

19-20. 

Verrill, A. E., 1914, Monograph of the shallow-water starfishes of the north Pacific Coast from the Arctic Ocean 

to California: Smithsonian Inst., Harriman Alaska ser., 

v. 14, pt. 1 and 2, 408 p., 110 pls. 
PLATES 1-3 

Contact photographs of the plates in this report are available, at cost, from U.S. Geological Survey Library, Federal Center, 

Denver, Colorado 80225 
PLATE 1 

FIGURE 1. Promopalaeaster speciosus (Meek). Unknown horizon, Cincinnati, Ohio; MCZ 22, holotype. A, Arm, dorsolateral aspect, arrow 1 points ossicle of smaller intermarginal subseries; arrow 2 points ossicle of larger 

intermarginal subse-ries, X 8 (p. F2). B, Theca, dorsal aspect X 2 (p. F2). C, Theca, ventral aspect, arrow 

points to perradial node X 2 (p. F2). 

2. Promopalaester speciosus (Meek). Lexington Limestone, near Frankfort, Ky.; UK 403 (holotype of P. 

prenuntius Schuchert). Ventral aspect with one brachial tip (arrow) overturned, X 1.5 (p. F2'). 

3. Promopalaeaste-r· speciosus (Meek). Lexington Limestone, near Frankfort, Ky.; YPM 3405. Arm, ventrolateral 

aspect showing relic- structure of spine stereom (arrow), X 9 (p. F2). 

4,5. Promopalaester finei (Ulrich) n. comb. Kope Formati:m, Covington, Ky.; FM 54069. 4, Lectotype of Mesopalaeaster proavitus Schuchert, X 3 (p. F4). 5, Paralectotype in ventral aspe-ct, X 6 (p. F4). 

6, 7. Promopalaeaster finei (Ulrich) n. comb. Logana Member of Lexington Limestone, USGS locality 6419-CO; 

USNM 236052. 6, Dorsal aspect of larger fragment, X 4 (p. F4). 7, Ventral aspect of smaller fragment, 

X 4 (p. F4). 

8. Promopalaeaster .finei (Ulrich) n. comb. Unknown horizon, Cincinnati, Ohio; UM 6230. Brachium, dorsolateral aspect showing relative prominence of dorsal primary and secondary ossicles. Note biserial arrangement of adradials and intermarginals, X 5 (p. F4). 

9. Promopalaeaster finei (Ulrich) n. comb. Unknown horizon, near Augusta, Ky.; UC 40758. Theca, dorsal aspect with exposed buccal frame showing internal odontophores (arrow on one), X 2 (p. F4). 
GEOLOGICAL SU RVEY PROFESSIONAL PAPER 106&--F PLATE I 

PROMOPALAEASTER 
PLATE 2 

FIGURE 1. Promopalaeaster finei (Ulrich) n. comb. Kope Formation, Cincinnati, Ohio; USNM 60604, lectotype. Ventra] 

aspect of disarticulated juvenile, X 6 (p. F4). 

2. Promopalaeaster finei (Ulrich) n. comb. Unknown horizon, Cincinnati, Ohio; AMNH 1196, (largest specimen in 

suite). A, Dorsal aspect, X 2.4 (p. F4). B, Ventral aspect, arrow points to adoral carina, X 2.5 (p. F4). 

3. Promopalaeaster finei (Ulrich) n. comb. Clays Ferry Formation, USGS locality 6143-CO; USNM 236050. A, 

Theca, dorsal aspect. (Most ossicles removed by preparational acidiza tion; interossicle fillings remain.) X 2 

(p. F4). B, Oral area, X 4 (p. F4). 

4. Promopalaeaster finei (Ulrich) n. comb. Unknown horizon, Covington, Ky.; USNM 92613. Brachial fragment, 

ventral aspect. Note tendency toward quadriserial podial cupules on proximal (left) end, X 2 (p. F4). 

5. Promopa.laeaster finei (Ulrich) n. comb. Clays Ferry Formation, USGS locality 6143-CO; USNM 236051. Brachium, ventral aspect, X 11 (p. F4). 

6. Promopa.laeaster finei (Ulrich) n. comb. Kope Formation, Cincinnati, Ohio. A, A brachium and disc, ventral 

aspect (photographed in xylol). UC 40371, X 7 (p. F4). B, Theca, dorsal aspect. (Arrows point developing 

adradials.) UC 40371, X 5 (p. F4). C, Brachium, dorsal aspect. (Arrow points early adradial.) UC 40381, 

X 10 (p. F4). D, Brachium, dorsal view (Arrow points intermarginals.) UC 40382, X 6 (p. F4). 

7. Stenaster obtusus (Forbes). Hull Limestone, Kirkfield, Ontario; UC 36426. Interbrachial area, ventrolateral aspect. (Arrows point granular ossicles of lateral integument.) Note deep furrow between opposing ambulacral 

oss'icles, X 6 (p. F5). 

8. Stenaster cf. S. obtusus (Forbes). Curdsville Limestone Member of Lexington Limestone, USGS locality 5101-

CO; USNM 263054. Brachial fragment, ventral aspect. (Arrow points deep radial furrow.) X 6 (p. F6). 
PROFESSIONAL PAPER 106&-F PLATE 2 

PROMOPALAEASTER,STENASTER 
PLATE 3 

FIGURE 1. La.nthanaster intermedius (Schuchert) n. comb. Maysvillian Age (horizon unknown), Cincinnati, Ohio; FM 

9575, holotype. Ventral aspect, X 3 (p. F4). 

2. Lanthanaster intermedius ( Schuchert) n. comb. Maysvillian Age (horizon unknown), Cincinnati, Ohio; UC 

6433 (holotype of Lanthanaster cruciformis Branstrator). A, Theca, ventral aspect. (Arrow points madreporite.) X 1.5 (p. F4). B, Theca, dorsal aspect, X 1.5 (p. F4). 

3. Lanthanastwr intermedius (Schuchert) n. comb. Clays Ferry Formation, USGS locality 6143-CO; USNM 

236053. A, Brachium, dorsal aspect, X 8 (p. F4). B, Theca, ventral aspect. (Arrowpoints madreporite) X 2.5 

(p. F4). C, Theca, dorsal aspect, X 2.5 (p. F4). 

4. Mesopalaeaster shafferi (Hall). Maysvillian Age (horizon unknown), Cincinnati, Ohio; USNM 60621. Brachium, 

dorsal aspect, X 2.5 (p. F4). 

5. "Huclsonaster milleri" Schuchert. Lexington Limestone, Fayette County, Ky.; UK 1344. Theca, ventral aspect 

(photographed in xylol), X 4 (p. F6). 

6. "Hudsonaster narrawayi" (Hudson) fide Schuchert. Unknown horizon, near Curdsville, Ky.; YPM 13178. A, 

Theca, ventral aspect, X 3.5 (p. F6). B, Brachia and disc, dorsal aspect (note adradial columns.), X 7 (p. F6). 

7. "Palaeaster ?dubius" Miller and Dyer. Point Pleasant Tongue of Clays Ferry Formation, Ludlow, Ky.; MCZ 

25. Fragmented and eroded theca, ventral aspect, X 10 (p. F6). 

8. Oegophiurid. Point Pleasant Tongue of Clays Ferry Formation, Ludlow, Ky.; YPM 11771. Theca, ventral aspect, 

X6(p.F6). 
GEOLOGICAL SU RVEY PROFESSIONAL PAPER 1066-F PLATE: 3 

LANTHANASTER , MESOPALAEASTER , SPECIES INQUIRENDA 
Conodonts and Conodont Biostratigraphy 

of Post-Tyrone Ordovician Rocks 

of the Cincinnati Region 

By WALTER C. SWEET 

CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF 

KENTUCKY AND NEARBY STATES 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-G 

Prepared in cooperation with the 

Commonwealth of Kentucky, 

University of Kentucky, 

Kentucky Geological Survey 

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON 1979 
l. 
CONTENTS 

Page 

Albstract ----------------------------------------------------------------- G1 

Introduction ------------------------------------------------------------- 1 

Sample material --------------------------------------------------------- 2 

Alcknowledgments ----------- ________ ------ _ ------------------------------ 2 

The conodont faunas ----------------------------------------------------- 4 

Midcontinent faunal elements ----------------------------------------- 5 

North Altlantic faunal elements --------------------------------------- 6 

Biostratigraphy ______________________________________________ --- __ _ _ _ _ __ _ 6 

Alssembling the record ------------------------------------------------ 6 

The composite section --------~---------------------------------------- 11 

Conodont zones ------------------------------------------------------- 12 

Correlations --------------------------------------------------------- 13 Taxonomic remarks ---- ____________________ ------- ______ - --- _____ -------- _ 14 

Locality register --------------------------------------------------------- 22 

References cited ---------------------------------------------------------- 24 

ILLUSTRATIONS 

Page 

FIGURE 1. Index map of the Cincinnati region, showing location of sections containing post-Tyrone Ordovician conodonts --------,----------- G3 

2. Composite logs showing the relative abundance of Phragmodus undatus, Plectodina, Aphelognathus + Oulodus, and Rhipidognathus in post-Tyrone Ordovic-ian rocks of the Cincinnati region __ 8 

3. Correlation of post-Tyrone Ordovician rocks of the Cincinnati region, 

as suggested by the distribution of conodonts ---------------- 13 

TABLE 

Page 

TABLE 1. Composite and district ranges of post-Tyrone Ordovician conodonts Gll 

SYSTEM OF MEASUREMENT UNITS 

The investigations underlying this series of reports were made over a period of 

years, and distances and stratigraphic measurements appear fairly uniformly in 

English units. Measurements of fossil specimens, ori the other hand, follow the Iong-

.standing convention of appearing in metric units. Because of the dates of the investigations and the amount of resulting data, the English measurements have been 

retained. Conversions to metric units may be made by using the following conversion 

table: 

To convert 

English unit: 

Mile (mi) 

Foot (ft) 

To metric unit: 

Kilometer (km) 

Meter (m) 

Multiply by: 

1.61 

.305 

III 
CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

CONODONTS AND CONODONT BIOSTRATIGRAPHY OF 

POST-TYRONE ORDOVICIAN ROCKS OF THE 

CINCINNATI REGION 

By WALTER c. SWEET 1 

ABSTRACT 

Conodonts representing 35 species of 20 genera have been 

collected from post-Tyrone Ordovician rocks at 51 localities 

in the Cincinnati region of north-central Kentucky and adjacent parts of Ohio and Indiana. Most species are longranging components of the conodont fauna of the North 

American Midcontinent Province. Logs charting v~rtical 

fluctuations in relative abundance of common midcontinent 

species are used to correlate short sections and combine them 

into synthetic composites for four districts of the Cincinnati 

region. A regional correlation chart is derived from correlation of the four district composites, as is a composite range 

table that summarizes all available information on stratigraphic distribution of conodonts in post-Tyrone Ordovician 

rocks of the Cincinnati region. Taxonomy of all the conodonts represented is reviewed and updated. 

INTRODUCTION 

Conodonts are abundantly represented in Ordovician rocks of the Cincinnati Region, 2 from the base 

of the Lexington Limestone upward to the top of the 

Cincinnatian Series. The first conodonts to be described from Ordovician rocks of the Cincinnati region are apparently the ones figured by James 

(1884), although Grinnell (1877) and Ulrich (1878) 

speculated on the conodont affinities of some· scolecodonts they collected from rocks of the same area. 

Branson and Branson ( 1942) noted that conodonts 

are present throughout the Cincinnatian in Kentucky 

and adjacent States, but they provided no descriptions or illustrations o.f their specimens. 

Extensive studie·s of conodonts from the Ordovician of the Cincinnati region began in 1951, when 

Branson, Mehl, and Branson published desc·riptions 

and illustrations of typi~cal Richmondian forms from 

Kentucky and Indiana. Subsequently (Sweet and 

others, 1959; Pulse and Sweet, 1960; Bergstrom and 

Sweet, 1966; Kohut and Sweet, 1968), the entire 

complex of conodont species characteristic of Lexington and younger Ordovician .strata has been described, in at least preliminary form, and the faunas 

represented by these species are now among the best 

known from any part of the Ordovician anywhere in 

the world. 

Descriptions· and interpretations of Cincinnati 

region Ordovician conodonts have been completed 

and published piecemeal over a period of more than 

25 years. Except for understanding based on material asse·mbled by Branson, Mehl, and Branson (1951), 

current knowledge of Cincinnati region Ordovician 

conodonts is founded almost entirely on collections at 

The Ohio State University that now include more 

than 418,000 identified and cataloged specimens. As 

collections have grown in size and have come to 

·represent more and more of the interval between the 

base of the Lexington Limestone and the top of the 

Cincinnatian Series, and as additional sections have 

been sampled to provide ever wider geographic coverage within the Cincinnati region, our taxonomic 

and stratigraphic concepts have also evolved. Early 

reports (Branson and others, 19·51; Sweet and others, 1959; Pulse and Sweet, 1960) were made in a 

stratigraphic context inherited from turn-of-thecentury studies largely in the environs of the city of 

Cincinnati and in a form-taxonomic framework that 

was generally acceptable at the time. Later studies 

(Bergstrom and S.weet, 1966; Kohut and Sweet, 

1968) had the advantage of :at least P·reliminary information fro.m modem stratigraphic work on, and 

mapping of, Ordovici·an ·rocks in the Cincinnati .re1 The Ohio State University, Columbus, Ohio. 2 As used in this and previous reports on Ordovician conodonts and 

stratigraphy, the designation, Cincinnati region, refers to the entire area 

of Ordovician exposure in southwest Ohio and adjacent parts of Indiana 

and Kentucky. The Cincinnati region is the stippled area of figure 1. 

Gl 
G2 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

gion, and were also set in the context of an evolving 

multi-element taxonomy for conodonts. Although advances between 1951 and 1966 were important to a 

detailed understanding of Ordovician conodonts and 

history in the Cincinnati region, an unfortunate consequence of the evolution in stratigraphic and taxonomic ·concepts has been that earlier descriptions, as 

well as the statements on stratigraphic range that 

ac.company them, are difficult to interpr·et accurately 

in present-day taxonomic or stratigraphic terms. 

Consequently, it is the principal purpose of this report to summarize and to bring up to date information on the taxonomy and stratigraphic distribution 

of Ordovician conodonts f~om the Cincinnati region. 

It is hoped that this summary will be more useful to 

stratigraphe·rs and paleontologists than are the scattered reports, both published and unpublished, on 

which it is based. 

SAMPLE MATERIAL 

Present knowledge of the geographic and stratigraphic distribution of Ordovician conodonts in the 

Cincinnati region is based on a collection of 418,144 

identified conodont-elements, assembled from 2,358 

300- to 500-gram samples, which have been collected 

from sections at 51 sites (fig. 1 and "Locality Register"). A majority of the specimens were derived 

from the acid-insoluble residues of limesto:p·e samples, but about 20,000 of them were collected from 

shale samples, which had been disaggregated and 

washed through 100-mesh s·creens. At present, all of 

the collections are kept in the Micropaleontological 

Laboratories of the Department of Geology and Mineralogy, The Ohio State University. 

More than 90 percent of the samples and specimens were collected and prepared by students and 

faculty at The Ohio Stafu Universi·ty in connection 

with long-range biostratigraphic studies of the Ordovician rocks of the Cincinnati region. About 27,000 

specimens, however, derived from 266 samples that 

were colle·cted at 10 loc~lities in Kentucky, were submitted for study by various members of the U.S. 

Geological Survey. The latter specimens are now included in permanent collections at The Ohio 8tate 

University, but they are in distinctly numbered slides 

and are filed separately from the bulk of the collections, which a.re identified by distinctive Ohio State 

University sample- and catalog-number designations 

of the general 7 4XY -000 type. 

It should be noted that non-type bulk ·collections of 

conodonts from the "Eden Formation" of the Cincinnati region (Sweet and others, 195.9) are· not included in tabula,tions reported in the preceding paragraph, nor ar·e most of the localities from which 

those conodonts were derived listed in the "Locality 

Register." "Eden" bulk collections were destroyed by 

an untrained museum assistant, who, however, was 

careful to preserve the types of all taxa des.cribed 

and illustrated by Sweet and ·othe,rs in their report 

of 1959. Large collections have subsequently been 

derived from rocks of Edenian Age, but most of them 

ar·e from different sections fro~m the ones listed in 

Sweet and others (1959). 

ACKNOWLEDGMENTS 

Many of the conclusions and most of the speculation in this report are the writer's responsibility. 

However, the material on which this report is based 

has been assembled by a number of persons, to all of 

whom sincere appreciation is expressed. Earl Warner, Jr., of Lafayette, La., Lorna C. Wilkie, of Washington, D.C., and Caroline A. Turco, of Ridgefield 

Park, N.J., collected conodonts from Eden ian rocks 

and did much of the original interpretive work. Richard R. Pulse, now of Denver, Colo., made extensive 

collections from Maysvillian rocks; and Richard F. 

McClish of New Orleans, La., measured and collected many conodonts from sections of Richmondian 

strata. Claude C. Rust, of Houston, Tex., prepared 

sampl·es from the Middletown Core ( OSU section 

61Z), helped develop the relative-abundance-analysis 

technique, and assisted in the field as many samples 

from the Lexington Limestone were collect,ed. Joseph 

J. Kohut, now of Portland, Oreg., substantially augmented our collections of Richmondian conodonts, 

tabulated and described them, and developed an 

imaginative and useful technique for statistical 

analysis of the taxa represented in our entire collection. Anita G. Harris, of Washington, D.C., prepared 

material from the Ohio Brush Creek locality ( OSU 

section 62DA), and Howard Harper, Jr., of Cambridge, Mass., and Dennis Zlatkin, of Springdale, 

Ohio, sampled, described, and collected conodonts 

from the upper part of Cominco American Core C-38 

(OSU section 70ZA). 

A special debt is owed Stig M. Bergstrom, of The 

Ohio State University, who has participated in all 

but the earliest studies of Cincinnati region conodonts. Dr. Bergstrom did much of the fieldwork, 

processed most of the samples, and shared equally in 

the job of picking conodonts from Lexington Limestone residues. He has been generous in discussing 

special problems and in ·OOoperatively preparing 

many reports on conodonts from the Cincinnati region. His help in reading and suggesting improve-
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION 

0 10 20 30 40 50 60 70 KILOMETERS 

I I 

I 

I I 

I 

I 

I 

I I I I 

0 10 20 30 40 MILES 0 100 200 300 400 KILOMETERS 

I I 

I 

I I 

I I I 

0 100 200 MILES 

FIGURE 1.-Index map of the Cincinnati region (patterned) showing location of sections (numbered, 

circled dots) from which post-Tyrone Ordovician conodonts have been collected. Sections are 

more fully identified in "Locality Register," beginning page G22. Sets of sections enclosed by 

dashed lines are combined to produce the logs of figure 2. 

G3 
G4 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

ments to the text of the present report is warmly 

acknowledged. 

It is also a pleasure to acknowledge the help received from various members of the U.S. Geological 

Survey involved in mapping Ordovician bedrock in 

the Cincinnati region. Eade Cressman, Gordon Wier, 

Douglas Black, John Peck, and Warren Peterson 

have been' particularly generous with their time in 

the field, and have submitted samples from sections 

that have greatly increased our kno·wledge of the distribution of Cincinnati region Ordovician conodonts. 

We also acknowledge a considerable debt to Malcolm P. Weiss, now of Northern Illinois University, 

DeKalb, Ill., with whom we worked very closely during much of the time we were developing our collections and our knowledge of the rocks and fossils of 

the Cincinnati region. 

THE CONODONT FAUNAS 

In 1959, Sweet and others concluded that conodont 

collections from Edenian rocks of the Cincinnati region included representativ·es of the faunas of two 

distinct provinces, a warm-temperate North American Midcontinent Province, and a cold-temperate 

Anglo-Scandinavian-Appalachian Province. Intermingling in the Cincinnati region of conodonts characteristic of these two provinces was interpreted to 

be a result of periodic shifting of the interprovincial 

boundary, permitting occasional immigration of certain Anglo-Scandinavian-Appalachian speeies into 

waters of the North American Midcontinent 

Province. 

Pulse and Sweet (1960) recognized that spe·des of 

Anglo-Scandinavian-Appalachian affinities were also 

periodic contributors to the Maysvillian conodont 

faunas of the Cincinnati region, and they noted the 

appearance in rocks of Early Maysvillian Age of the 

northern Cincinnati region of a group of robust elements of Aphelognathus and Oulodus that are obviously related to more delicate forms characteristic of 

the North American Midcontinent Province. The 

provincial affinities of species represented by the 

robust Maysvillian elements were not determined, 

but it was tentatively suggested that they might be 

the local results of peculiar ecologic conditions. Following Sweet and others (1959), Pulse and Sweet 

(1960) also recognized that Richmondian rocks contain many conodonts that seem unrelated to either 

the North American Midcontinent or Anglo-Scandinavian-Appalachian elements of Edenian and Maysvillian faunas. Some of the species· represented by 

elements of Richmondian aspect appear in Maysvillian rocks, and Pulse and Sweet suggested that they 

might represent the initial migration into the Cincinnati region of a third fauna, which made its principal contribution to that of the Cincinnati region in 

Richmondian time. 

Bergstrom and Sweet ( 1966) concluded fro·m their 

s~tudy of conodonts from the Lexington Limestone 

and its lateral equivalents that their collections included representatives of both the North American 

Midcontinent Province and the Anglo-ScandinavianAppalachian Province. They proposed, however, that 

the designation, European Province, was a less cumbersome term than Anglo-Scandinavian-Appalachian, and noted (p. 283) that"* * *the North American midcontinental fauna is not developed in the 

same way throughout the vast region in which its 

components are known." That is, they pointed out 

that Phragmf)dus and Plectodina are the midcontinent genera most characteristi-c of the eastern part 

of the North American Midcontinent Province; that 

Panderodus and B elodina seem to be the most characteristic genera of midcontinent faunas in Iowa, 

Minnesota, and areas north and west of those States; 

and that Aphelognathus, Oulodus, and Rhipidognathus characterize a third subprovince that is best 

developed in the Nashville-Ozark region. 

Kohut and Sweet (1968) also recognized European and midcontinent components in conodont faunas 

re·constructed from specimens .they collected from 

rocks of Late Maysvillian and Richmondian Age in 

the Cincinnati region. They noted, however, that 

European faunal elements are not represented in 

Richmondian strata above the top of the "Arnheim" 

Formation, and they introduced the informal designations "northern fauna" for the subprovincial midcontinent fauna dominated by Phragmodus and Plectodina, and "southern fauna" for the subprovincial 

midoontinent fauna distinguished by the conodonts 

referred in this report to Aphelognathus, Oulodus, 

and Rhipidognathus. Elements of the southern fauna 

were also shown to be associated in abundance with 

rocks whose lithic and structural features indicate 

deposition in very shallow water environments. 

Seddon and Sweet ( 1971) distinguished between 

"indigenous," "interior," and "European" ·Components of the Ordovician conodont faunas of the Cincinnati region. The indigenous and interior faunas 

were regarded as subprovincial ·components of the 

North American midcontinent fauna. The former included the northern and southern faunas of Kohut 

and Sweet (1968); the latter was a name applied to 

the subprovincial midcontinent fauna dominated by 

Panderodus and B elodina and first recognized by 

Bergstrom and Sweet (1966). 
• 

CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G5 

In this report, the name "North Atlantic Province" is used for the region characterized in the 

Ordovician by the conodont fauna termed AngloScandinavian-Appalachian by Sweet and others 

(1959) and Pulse and Sweet (1960), or European 

by Bergstrom and Sweet ( 1966), Kohut and Sweet 

( 1968), and Seddon and Sweet ( 1971) . This substitution of names follows the practice of Bergstrom 

(1971a, 1971b, among other repo·rts), who has written extensively about the conodont faunas of the 

North Atlantic Province. The designation North 

American Midcontinent Province (or Midcontinent 

Province) is still adequate for the region dominated 

in the Ordovician by conodonts referable to Phragmodus, Plectodina, Oulodus, Aphelognathus, Rhipidognathus, Panderodus, and Belodina, but it is also 

appropriate to recognize, at least informally, that 

composition of the midcontinent conodont fauna 

varied from place to place, and from time to time, 

within the province. Consequently, it is possible to 

distinguish an "exterior" subprovince, in which the 

characteristic conodont genera were Phragmodus 

and Plectodina, and an "interioT" subprovince, in 

which the indigenous conodont fauna was dominated 

by certain species of Panderodus and B elodina. For 

much of Middle and Late Ordovician time, the ex- · 

terior subprovince included the Trenton type area of 

southern Ontario and adjacent New York, the Appalachians west of the Saltville fault, the Cincinnati 

region, the Nashville Basin of Tennessee, the Ozarks, 

the Batesville district of northeastern Arkansas, the 

Arbuckle Mountains of Oklahoma, and the Ma;rathon 

district of Texas. The interior subprovince included 

a vast area west and north of the exterio·r subprovince. Faunas of interior-subprovince type are known 

from sections in northeast Iowa and adjacen~t Minnesota, Wisconsin, and Illinois, and from the 

Dakotas, southern Manitoba, Wyoming, Kansas, Nebraska, Colo·rado, California and Nevada. Additionally, the Ozarks and the Batesville district of 

northeast Arkansas came to be dominated by faunal 

elements of the interior subprovince· in the Late Ordovician, at a time when there was also a conspicuous influx .of such conodonts into the eas.tern se·gment 

of the exterior subprovince. It should be· noted that, 

for that part of the Ordovician considered in this 

report, Barnes, Rexroad, and Miller ( 1973) also 

recognized two divisions of the Midcontinent Province, which they termed eastern and western subprovinces. These correspond to the exterior and 

interior subprovinces of this report. 

MIDCONTINENT FAUNAL ELEMENTS 

In that part of the Ordovician represented by the 

stratigraphic succession considered in this report, 

the Cincinnati region was apparently situated about 

100 miles west of what is now the east edge of the 

North American Midcontinent Province. Consequently, the bulk of the conodonts recovered from 

Lexington and younger Ordovician rocks of the Cincinnati region are referable to species characteristic 

of the ex·terior subprovince of the North American 

Midcontinent Province. From time to time, however, 

immigrants from either the North Atlantic Province 

or the interior subprovince of the Midcontinent 

Province made contributions 1x> the fauna of the Cincinnati region. Thus, about 8 percent of the conodonts in our collections represent immigrant species 

from the North Atlantic Province, and another 1 percent of our specimens is referable to· Panderodus 

gracilis, P. sp. aff. P. panderi, P. angularis, P. staufferi, and various species of Belodina, which we regard as typical of the interior subprovince of the 

North American Midcontinent Province. 

On the basis of their geographic and stratigraphic 

distribution, midcontinent elements of Cincinnati 

region Ordovician conodont faunas can be s·eparated 

into two groups. One, characterized by Phragmodus 

undatus and Plectodina furcata, is dominant in the 

north half o.f the Cincinnati region through virtually 

all of the stratigraphic interval considered here; 

whereas, the other, typified by various species of 

Aphelognathus, Oulodus, and Rhipidognathus, is 

best and mo.st continuously developed in the south 

half of the Cincinna-ti region. It now appears probable, from data summarized by Seddon and Sweet 

(1971), that the northern element of the indigenous 

fauna of the exterior subp.rovince flourished in 

waters above the deeper depositional sites in the 

Cincinnati region and that the southern element was 

adapted to waters over the more shallowly submerged depositional sit.es. As noted in the section on 

biostratigraphy in this report, extensive use has been 

made of areal and vertical fluctuations in the relative 

abundance of the northern and southern elements of 

the indigenous fauna of the exterior subprovince to 

effect correlations between the 51 sections from 

which we have collected conodonts in the Cincinnati 

region. 

Specimens assignable to Panderodus and Belodina, 

which we regard as indexes to the fauna of the 

interior subprovince of the Midcontinent Province, 

are minor but consistent oomponenrts of conodont collections from the base o.f the Lexington Limestone to 

·a level about 85 feet above the base of the Maysvilli-
''I 

G6 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

an Stage. The upper 125 feet of the Maysvillian 

Stage lacks interior faunal elements, but they reappear in force at the base of the Richmondian Stage 

and are conspicuous constituents of all our collections 

above that level to the top of the Cincinnatian Se:ries. 

It is suspected that the absence of interior faunal 

elements in rocks of late Maysvillian age indicates 

that no direct marine connection was open between 

the Cincinnati region and more interior areas of the 

continent at that time. Perhaps it was during this 

interval that the unconformity separating the Dubuque Formation and Maquoketa Shale of the Upper 

Mississippi Valley was ~ormed. 

NORTH ATLANTIC FAUNAL ELEMENTS 

Immigrants from the North Atlantic Province into the exterior subprovince of the North American 

Midcontinent Province include: Amorphognathus ordovicicus, A. superbus, A. tvaerensis, Icriodella superba, Paroistodus? mutattt.,S, Periodon grandis, Protopanderodus n. sp. cf. P. insculptus, P. sp. cf. P. 

dissimilaris, and Rhodesognathus elegans. Of these 

nine species, only four are represented in any abundance in the Cincinnati region. These are lcriodella 

superba and the three species of Amorphognathus. 

Collectively, however, the North Atlantic contingent 

of immigrants ranges from 40 to 785 feet abo·ve the 

base of the Lexington Limestone; that is, from a 

level in rocks of the Kirkfieldian Stage to one about 

30 feet above the base of the Richmondian Sta~e. 

Amorphognathus and Icriodella, the two North 

Atlantic conodont genera most abundantly represented in the Cincinnati region, differ conspicuously 

in their distribution. Icriodella is the North Atlantic 

form most prominently represented in samples dominated by elements of the southern component of the 

indigenous midcontinent fauna, whereas Amorphognathus is the genus most prominently represented 

in samples dominated by elements of the northern 

component o.f that fauna. 

Seddon and Sweet ( 1971) interpreted these distributional vagaries to mean that Icriodella inhabited 

a depth zone that was closer to the surface of the 

water body than was the one inhabited by Amorphognathus. However, in assembling the data for this 

report, it was noted that in only 88 (or 14 percent) of 

the 613 samples containing spedmens of I criodella 

and (or) Amorphognathus do the two occur together. Through much of the Edenian Stage in the north 

half of the Cincinnati region, Amorphognathus is the 

only North Atlantic genus represented, and the same 

is true in the Maysville area. I criodella is, indeed, 

more abundantly and continuously represented in the 

southern Cincinnati region than in the northern part, 

but even there only 9 of the 135 samples that yield 

North Atlantic elements include specimens of both 

Icriodella and Amorphognathus. If Seddon's and 

Sweet's (1971) conclusion about these conodonts was 

correct, both should be represented in the no·rthern 

Cincinnati region, even though it might be expected 

that I criodella, the shallower water form, would occur by itself in the southern part of that region. 

From the data reported here, however, it appears 

that I criodella was, indeed, adapted to a shallower 

water environment than Amorphognathus; or, more 

precisely, that I criodella inhabited wate·r over the 

more shallowly submerged depositional sites, whereas Amorphognathus flourished in water over the 

more deeply submerged depositional sites, at least in 

the Midcontinent Province. (In the Balto-Scandic 

area, however, representatives of Amorphognathus 

are common in some rocks that are demonstrably of 

very shallow water origin ( S. M. Bergstrom, oral 

oommun., 1974) .) 

The fact that a few specimens of Amorphognathus 

do occur with elements of Rhipidognathus in several 

samples from the southern Cincinnati region suggests that Amorphognathus was occasionally able to 

invade the shallowly submerged areas favored by 

Icriodella. And this, in turn, suggests that species of 

the two genera ·may have occupied the same depth 

zone, but in deeper water and shallower water environments, respeetively. 

The stratigraphic distribution of North Atlantic 

faunal elements in the Ordovician succession of the 

Cincinnati region has been helpful in co:rrelating that 

suc·cession with the sequence in the .type area of the 

Trenton Group (Sweet and Bergstrom, 1971), and 

with the sequence of -conodont zones established by 

Bergstrom (1971a) for rocks in the North Atlantic 

Province. Conodonts of North Atlantic affinities are 

of less value for ·correlation within the Cincinnati 

region, as indicated in the next section of this report. 

BIOSTRATIGRAPHY 

ASSEMBLING THE RECORD 

Long ·continuous sections are rare in the area of 

Ordovician ·exposure in the Cincinnati region, and 

assembling short, scattered s~ections into a ·C:hronologically meaningful composite has been difficult and 

time consuming. Further, we have had to rely on 

I 

methods that differ substantially from those· ordinarily used in building a biostratigraphic frame-
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G7 

work. Consequently, the procedures employed to develop the four composite sections of figure 2 merit 

extended description and discussion. 

Early in the study of Ordovician conodonts from 

the Cincinnati region it was noted (Sweet and others, 1959; Pulse and Sweet, 1960) that at least two 

provincially distinct conodont faunas made periodic 

contributions to the fauna of the Cincinnati region, 

and that there were substantial lateral and vertical 

variations in the composition of the indigenous fauna 

itself. The latter variations, express·ed vertically by 

fluctuations in the relative abundance of long-ranging components of the indigenous fauna and laterally 

by the gradual appearance of different species, were 

not understood at first, but have come to be of prime 

importance in building the biostratigraphic framework depicted in figure 2. 

In an abstract of 1965, Sweet, Bergstrom, and 

Rust ·Commented on the potential utility of relativeabundance analysis in effecting a conodont biostratigraphy for Ordovician rocks of the Cincinnati 

region, · and the methods they discussed were described more fully by Bergstrom and Sweet in 1966. 

Briefly, it was noted that the conodont species most 

abundantly and commonly represented in Lexington 

and younger Ordovician rocks of the Cincinnati region range from the bottom to the top of individual 

sections, but vary in their relative abundance from 

level to level in these sections in a seemingly systematic way. Because logs showing these vertical 

fluctuations in abundance are strikingly similar from 

section to section and appear to be related in only a 

general way to concordant variations in measured 

lithic features, it was concluded that correlation in 

time could be effected by matching relative-abundance logs for at least adjacent sections, particularly 

if it were assumed that the fluctuations were related 

to basin-wide changes in water-body conditions. 

Factors controlling vertical and lateral variations in 

relative abundance were unknown, however, and this 

inhibited full acceptance of the correlations made in 

1966. 

In 1968, Kohut and Sweet distinguished between 

northern and southe:rn elements of the indigenous 

Richmondian conodont fauna and pointed out that 

transition from the area dominated by the former to 

that dominated by the latter is accompanied by lithic 

features that indicate progressively shallower water. 

This suggestion that late:i·al changes in composition 

of the indigenous conodont fauna were related to 

changes in water depth was subsequently amplified 

by Seddon and Sweet (1971), who proposed a general ecologic model for conodonts, in which it was · 

postulated that these animals were pelagic and that 

species or groups of species were segregated by depth 

in somewhat the same manner that obtains for living 

·chaetognaths. According to the Seddon-Sweet model, 

the diverse conodont fauna of the northern Cincinnati region changed character southward into progressively shallower water largely through the loss 

of deeper water species as the upper limits of their 

life zones "dragged bottom." Fluctuations with the 

passage of time in the distribution of relatively deeper and relatively shallower water areas would then 

produce variations in the relative abundance of deeper and shallower wat.er conodonts that fell to and 

accumulated on the bottom at a particular depositional site. In short, the relative abundance of any 

conodont species that was confined in its lifetime to a 

restricted depth zone should provide, at any particular level in the stratigraphic record, at least a crude 

measure of the relative water depth at the depositional site. Further, vertical abundance variations in 

a section should be measures of changes in water 

depth at that site with the passage of tim·e. Because 

it seems unlikely that a change in depth sufficient to 

influence the relative abundance of a particular species in a measurably significant way could have been 

confined to just a single depositional site, the conclusion of Bergstrom and Sweet ( 1966) that pattern 

similarities in relative-abundance logs for sections 

throughout the Cincinnati region imply time-correlative basin-wide changes in water-body conditions 

still seems valid. 

The Seddon-Sweet depth-stratification model for 

conodonts is adequate as a general framework within 

which to interpret vertical and lateral fluctuations in 

relative abundance of species common throughout 

the Cincinnati region, but it needs elaboration to aceount for lateral changes in taxonomic composition 

of the indigenous fauna. That is, Phragmodus undatus Branson and Mehl and Plectodina furcata 

(Hinde) are the dominant members of the indigenous conodont fauna in the northern part of the 

Cincinnati region from the base of the Lexington 

Limestone almost to the top of the Cincinnatian 

Series. Southward, P. ju1·cata becomes relatively 

more abundant, but the two species are still important components of the indigenous fauna. However, species of Aphelognathus, Oulodus, and ultimately Rhipidognathus, which are rare or absent in 

the northern Cincinnati region until very late in the 

Ordovician, are conspicuously long ranging and 

abundantly represented components of the indigenous fauna in the relatively shallower water deposits 

of the southern Cincinnati region. If, as the evidence 
G8 CONTRIBUTIONS TO THE ·oRDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

0 

Decatur Co., 

SE Indiana 

100 

Cincinnati Area, 

SW Ohio 

2 

Maysville Area, 

Ohio- Kentucky 

3 

0 100 0 

PERCENT 

Southeast 

Cincinnati 

Region, 

Kentucky 

4 

100 

FIGURE 2.-Composite logs showing the relative abundances of Phragmodus undatus 

(coarse dots), Plectodina (black), Aphelognathus + Oulodus (white), and Rhipidognathus (fine dots) in post-Tyrone Ordovician rocks, in the four districts of the Cincinnati region enclosed in dashed lines in figure 1. 
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G9 

suggests, species of these latter genera inhabited 

wate:r that was relatively shallower than that to 

which Phragmodus and Plectodina were adap.ted, 

and if water depth were the only control on their 

distribution, we should expect from the depth-stratification model that Aphelognathus, Oulodus, and 

Rhipidognathus would be represented in nearly every 

sample throughout the Cincinnati region. That is, as 

inhabitants of the shallowest wa,ter life-zone, they 

should have been parts of the conodont infall at 

every depositional site in the Cincinnati region, regardless of the absolute water depth. This is clearly 

not true, as is shown graphically in figure 2. Consequently, we must apparently distinguish not only between the inhabitants of vario.us depth-zones, but 

also between different species that may have inhabited the same depth zone in areas of deeper or 

shallower water. Perhaps so·me of these species were 

benthic or nekto-benthic in habitat, as suggested by 

Barnes and Fahraeus (1975). 

In the mo.re deeply submerged parts of the Cincinnati region, it appears that Plectodina furcata was 

the shallower and P hragmodus undatus the deeper 

water species; but in more shallowly submerged 

areas, P. undatus declines in relative abundance and 

P. furcata gradually gives way to Aphelognathus 

politus, which is closely related toP. furcata and apparently flourished in the same depth zone in shoalwater environments. In rocks that represent these 

shoal-water environments, specimens of Oulodus are 

also more abundant than in rocks that represent accumulation in de·eper water. However, the relation of 

Oulodus to Aphelognathus and Plectodina is not 

clear: it may be mo·re closely related to ce•rtain 

"fibrous" conodonts, as Sweet and Schonlaub ( 1975) 

have recently suggested, and the distribution of that 

group in rocks of pre-Lexington age very strongly 

suggests adaptation to very shallow water. 

Rhipidognathus, as Kohut and Sweet (1968) 

noted, is most abundantly represented in calcareous 

or dolomitic mudstones that are mudcracked, ripplemarked, and may have been deposited in very shalhw 

water environments-perhaps on intertidal mudflats. 

The migration of Rhipidognathus into the northern 

part of the Cincinnati region in late Cincinnatian 

time is clearly associated with the northward translation of such environments. 

On the premise that fluctuations in the relative 

abundance of conodont species in the indigenous 

fauna of the Cincinnati region reflect basin-wide, but 

systematic, variations in bathymetry, but recognizing that the indigenous fauna also changes in taxonomic 0omposition from shallower to deeper water 

areas, information from the 51 sections listed in the 

"Locality Registe·r" has been compiled into the four 

areal composite s·ections of figure 2, rather than into 

a single composite, which would be too generalized to 

show conditions in any particular part of the Cincinnati region. 

The composite log for the southeast Cincinnati 

region (fig. 2) includes information from all the sections in the southernmost of the areas enclosed in 

dashed lines in figure 1. In ass·embling this log, information from localities 20 and 43 ( OSU sections 

60P and 73SA) was first combined with additional 

information from locality 20 (USGS sections CF, 

CF-CHIEF, and CF-WEIR), for these sections collectively represent an essentially 0omplete and continuous record in one place (Clays Ferry, Ky.) of the 

stratigraphic interval from low in the Lexington 

Limestone to the top of the Calloway Creek Limestone. To this initial "Clays Fe·rry composite" information was then added from locality 40 ( OSU section 66KK), which is not physically continuous with 

the Clays Ferry composite, but begins stratigraphically at about the top of that composite section and 

is situated only a few miles away from it (fig. 1). 

From info,rmation on stratigraphic thickness and 

conodont frequency in all thes·e sections, a single log 

(or "Clays Ferry-Agawam composite") was then 

constructed to show vertical fluctuations in the rela.-

tive abundance of the several components of the indigenous 0onodont fauna of that area. Similar logs 

were then prepared for all the other, mostly shorter, 

sections of the southern Cincinnati region indicated 

in figure 1. These logs were compared with the 

"Clays Ferry-Agawam composite," and congruence 

of pattern, which is striking in most cases, was taken 

to indicate correlation. After correlation of all sections in the southern area with the "Clays FerryAgawam composite," a new composite frequency log 

was compiled, based on all available information 

from s,ections in the southern area. That log is on the 

right side of figure 2. 

The log of figure 2 headed "Maysville area, OhioKentucky" summarizes data on conodont distribution in a group of 15 sections in the east-central Cincinnati region. These sections are enclosed in a 

dashed line in figure 1 and are described in the Locality Register." The composite log for the Maysville 

area was compiled in a manner similar to that used 

in building the southern Cincinnati region composite. 

In the Maysville area, however, we compiled the 

initial composite by combining information from 
G10 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

localities 42 and 1 (OSU sections 70ZA and 58A), 

which are close together geographically and which 

overlap appreciably stratigraphically. To this "Minerva-Maysville composite," data we~re then added 

from locality 25 (OSU s·ection 63AA), which is about 

10 miles east of Maysville but begins at about the 

same stratigraphic level as the top of the Maysville 

section (OSU section 58A) and continues upward to 

the top of the Ordovician. With the relative-abundance log for the "Minerva-Maysville-Isaac~ Creek 

composite," logs for all the other sections shown to 

be parts of the "Maysville co·mposite" in figure 1 

were then compared and correlated. Ultimately, from 

a combination of information from all these sections, 

the compo,site frequency log for the Maysville area 

shown in figure 2 was constructed. 

The composite frequency log for the Cincinnati 

area of southwest Ohio and adjaoent parts of Indiana and Kentucky is the second log fro~m the left in 

figure 2, and is based on information from the 14 

sections enclosed by a dashed line in the north-c-entral part of the Cincinna,ti region in figure 1. The 

initial composite was constructed from info-rmation 

obtained at localities 23, 34, and 26, which are respectively OSU sections 61Z (a 626-ft core drilled at 

Middletown, Ohio) , 66KE (type section of the Maysvillian Stage, in near-downto-wn Cincinnati, Ohio) , 

and 63AB (a long section of upper Maysvillian and 

Richmondian strata near China, Ind). These s·eetions 

are more widely separated geographically than are 

those nn which initial co-mposites for the southern 

and Maysville areas were based, but they overlap 

stratigraphically, show closely si·milar patterns on 

relative-abundance logs, and display essentially the 

same sequences of lithofacies in the intervals of overlap. To this initial composite, information from other 

sections in the Cincinnati area was added to yield the 

composite log shown in figure 2. 

The frequency log in figure 2 for Decatur County, 

Ind., is nnt a composite. As indicated in figure 1, this 

log is based ·on information from a singl~e section, 

OSU 65GV (locality 31), which is a long co.re drilled 

by the Indiana Geological Survey and generously 

made available for conodont studies. 

After the four· regional co~mposites just discussed 

were constructed, the correlations indicated in figure 

2 were effected by alining the logs ve~r~tically so that 

events indicated by major fluctuations in the. data 

logged were matched horizontally. In detail, the logs 

are noisy and out of phase at many levels. Howeve·r, 

it is submitted that the degree to which major fluctuations in frequency and faunal composition are refleeted laterally is indicative of relationships between 

these logs that must be more than coincidental. 

Stadia! boundaries indicated in figure 2 are drawn 

at the levels indicated by the positions of contaots in 

the co-mposite log for the Cincinnati area of southwest Ohio. The base of the Maysvillian Stage, for 

example, is fixed by tradition at the base of the Fairview Formation in the city of Cincinnati, hence is 

drawn in figure 2 at the level of the Fairview base in 

OSU section 66KE (lo-cality 34), which may be regarded as the Fairview type section. The base of 

what has become the Richmondian Stage was fixed 

by Orton in 1873 at the top of the "Orthis lynx beds" 

in a section in the Little Miami River valley that is 

very close to OSU section 58L (locality 11). Consequently, we draw the base of the Richmondian Stage 

in figure 2 at the level of the top of the "Orthis lynx 

beds" ( =Platystrophia ponderosa beds) in OSU section 58L, which is part of the Cincinnati area composite. The base of the Kope Formation is no longer 

exposed in the dty of Cincinnati, but it defines the 

base of the Edenian Stage and is about 230 feet belnw the base of the Fairview in Cincinnati (Ford, 

1967). Hence the base of the Edenian Stage, and of 

the Cincinnatian Series, is drawn 230 feet belo-w the 

bas·e of the Fairview in OSU section 66KE (lo-cality 

34), which is also part of the Cincinnati area compo-site section. 

Ass.embly of the areal co.mposites and the correlations sho·wn in figure 2 are based on the assumption 

that no large-scale or sysrtematic variations occur 

within presumably oonte~mporaneous units from 

place to place in the Cincinnati region. The assumption itself is based on the observation that the rock 

sequence throughout the Cincinnati region consists 

of essentially the same array of lithic types, arranged 

spatially in about the same stratigraphic order. 

Thus, although depositional rate may have varied 

with time, concomitant with differenc,es in accumulation rat,e across the Cincinnati region, it seems unlikely that these differenc-es were ever very great, 

and as data points in the logs are 5 feet apart, contemporaneous a-ccumulation-rate differences are 

pvobably averaged out over the thickness of formations or of the logs themselves. Furthe·r, the congruence in pattern, or signature, between the logs themselves is regarded as a forceful and graphic argument for accepting the assumption that the thickness of units regarded as contemporary varies little 

from place to place in the Cincinnati region. 
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G11 

THE COMPOSITE SECTION 

Conodonts from Lexington and younger Ordovician strata in the Cincinnati region a.re referable to 

35 specific taxa and one collective category identified 

only as "fibrous ·conodonts." These 36 entities a.re 

listed alphabetically in table 1, along with their 

ranges in the four areal composite sections of figure 

2. The right-hand column, "Composite," summarizes 

the known ranges for the entire Cincinnati region. In 

the composite, the base, or "0" point, is the base of 

the Lexington Limestone in the Maysville area, and 

the top, or "1040" point, is the top of the Cincinnatian Series in the New Point, Ind., -core (OSU section 

65GV; locality 31 in "Locality Register"). It is emphasized that ranges listed are merely the lowest and 

highest levels at which the taxa listed have been 

recognized: they are not intended to suggest that the 

species in question is continuously represented 

throughout the interval given by the range figures. 

Current concepts of the taxa identified by name in 

table 1 are given in the s·e-ction of this report ti·tled 

"Taxono.mic Remarks." 

For purposes of reference, it may be useful to note 

that the bas·e of the Edenian Stage, and thus of the 

Cincinnatian Series, is at 315 feet in the composite 

section; that of the Maysvillian Stage is at 545 feet; 

and that of the Richmondian Stage is at 755 feet. In 

table 1 it is app-arent, however, that neither the base 

nor the top of the range of any conodont spedes coincides with any of these boundaries. Consequently, 

none of the Cincinnatian stages can be characterized 

specifically by any conodont species. Six s·pecies 

(A morphognathus tvaerensi's~ Aphelognathus kimmswickensis, Belodina monit01·ensis, Plectod ·na aculeata, PolyJJlacognathus ramo sus, and Protopanderro-

. dus sp. cf. P. dissimila-r·is) are restricted to rocks of 

pre-Edenian age in the Cincinnati region, and these 

and five others (Bryantodina abntpta, Oulodus subundulatus, Paroistodus? mutatus, Periodon g'tandis, 

and Synprioniodina? forsenta) are locally restricted 

to pre-Maysvillian strata. Fibrous conodonts and an· 

additional six .species (Amorphognathus superrbus, 

Belodina compressa, Oulodus oregonia, Panderodus 

sp. aff. P. pande1·i, Rhodesognathus elegans, and 

Stau:(fe1·ella falcata) are confined locally to preTABLE 1.-Composite and district ranges of post-Tyrone O·rdovician conodonts 

[Range in feet above base of composite section; dashed lines indicate not present] 

Species 

A·morphognathus ordovicicns -------------

superbus --------------------------- tvaerensis -------------------------- Aphelognathus kimmswickensis _________ _ politus ____________________________ _ 

Belodina compressa --------------------- monitorensis ______________________ _ 

profunda -------------------------- Bryantodina abrupta --------------------

staufferi --------------------------- Cyrtoniodus sinclairi ___________________ _ D·repanoistodus suberectus ______________ _ 

Fibrous conodonts ---------------------- / criodella superba _____________________ _ 

Oulodus oregonia ----------------------- robustus __________________________ _ 

subundulatus ______________________ _ ulrichi ___________________________ --

Panclerod.u.s angularis ------------------- gractl?s ___________________________ _ 

sp. aff. P. panderi -------------------

staufferi --------------------------- Paroistodus? mutatus ------------------- Periodon grand is ______________________ _ Pltragmodus undatus ___________________ _ 

Plectodina aculeata --------------------- fnrcata. ___________________________ _ 

? undulata ------------------------- PohfPla.coanathns ra.mosus --------------- P?·otopancle?·odus so. cf. P. dissimilaris ___ _ 

so. cf. P. insculpt?.ts ----------------- Rhipidoana.thts rowla.ndensis ------------ symm.etricus ______________________ _ 

Rhod~>so.ana.thus ele,qans ----------------- Sta.uffM'Plla. fa.lca.f.a --------------------- Synp?·ioniocUna.? forsenta ----------------

Southern 

205-560 

40-180 

0 

125-875 

20-485 

30-50 

830-865 

30-475 

70-225 

820-865 

30-865 

20-555 

70-470 

410-n45 

550-875 

140-385 

830-870 

835-870 

20-880 

30-365 

825-870 

70-80 

85-160 

30-365 

20-40 

55-645 

630-880 

25-65 

340 

600-805 

215-890 

40-315 

325-580 

240 

Maysville 

210-580 

60-180 

200-1,000 

0-510 

0 

915-985 

5-465 

200-210 

875-975 

0-995 

0-275 

45-760 

410-655 

635-1,000 

165-405 

805-990 

0-1,000 

990 210-4~0 

130-360 

0-910 

0-20 

55-1.000 

675-1.000 

15-35 

105-355 

635-1.000 

135-390 

85-585 

195-350 

Section 

Cincinnati 

585-740 

210-575 

75-200 

135-960 

45-565 

55 

800-960 

60-430 

180-200 

760-895 

45-910 

55-190 

80-725 

480-655 

660-945 

180-355 

850-900 

915-955 

55-970 

185-560 

915-955 

75-495 

80-385 

45-900 

55-65 

100-900 

850-955 

70-210 

135-200 

135-295 

915-960 

80-665 

410-555 

140-395 

Indiana 

585-785 

410-580 

60-185 

44 

655-1,025 

50-535 

900-1.015 

95-110 

60-410 

875-1,040 

50-1,040 

30-45 

60-645 

485-635 

810-895 

115? 

885-1,025 

955 

30-995 

55-425 

950-975 

55-490 

65-450 

50-990 

50-65 

80-1,020 

900-1,015 

55-60 

80-780 

940-1,025 

60-700 

550 

Composite 

585-785 

205-580 

40-200 

0-44 

125-1,025 

0-565 

0-55 

800-1.015 

5-475 

60-410 

820-1,040 

0-1,040 

0-555 

45-760 

410-655 

550-1,000 

115?, 140-405 

805-1,025 

835-955 

0-1,000 

30-560 

825-990 

55-495 

65-450 

0-990 

0-65 

55-1,020 

630-1,015 

15-210 

135-200 

105-780 

600-805 

215-1.025 

40-700 

85-585 

140-395 
G12 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Richmondian rocks. Five species (Belodina profunda, Cyrtoniodus sinclairi, Oulodus ulrichi, Panderodus angularis, and P. staufferi) are known in the 

Cincinnati region only from Richmondian strata, ·and 

locally these species are of considerable significance 

biostratigraphically (Kohut and Sweet, 1968). However, all the latter species are typical components of 

conodont faunas of the interior subprovince of the 

Midcontinent Province, and they may well make 

their debuts there in rocks of pre-Richmondian age. 

CONODONT ZONES 

When systematic studies of conodonts from Ordovician rocks in the Cincinnati region began it was 

hoped that a sequence of zones could be delineated, 

which would be useful not only in effecting detailed 

local correlations but also in recognizing the equivalents of these rocks elsewhere in North America and 

the world. This goal has been only partly achieved. 

Nevertheless, local correlations have been effected in 

other ways than zonal "matching," and the regional 

and international equivalents of .the rocks of the Cincinnati region can be broadly identified within the 

framework of a zonal scheme worked out in the 

North Atlantic Province by Bergstrom (1971a). 

Rocks 40 to 200 feet above the base of the composite section for the Cincinnati region yield representa.tives of Amorphognathus tvaeTensis Bergstrom; hence, they represent at least the upper part 

of the A. tvaeTensis Zone (Bergstrom, 1971a). Between 205 and approximately 580 feet above the 

base of the composite section, strata of the Cincinnati region yield specimens of AmoTphognathus sur 

peTbus (Rhodes), which evolved from A. tvaerensis 

and defines the A. supeTbus Zone in Bergstrom's 

zonal scheme. 

Specimens of Amorphognathus from rocks 585 to 

785 feet above the base of the composite section are 

assigned to A. oTdovicicus Branson and Mehl, although the holodontiform elements that are distinctive of this species have not been recovered from the 

Cincinnati region. These specimens are probably 

representatives of A. oTdovicicus, however, because 

Bergstrom (1971a) has shown convincingly that 

that species evolved from A. superbus, and the specimens in question are from samples above the level at 

which very advanced representatives of A. superbus 

have been positively identified. If identification of 

these specimens with A. or·dovicicus is correct, the 

rocks from which they were derived repres~ent the A. 

oTdovicicus Zone in Bergstrom's North Atlantic 

Province zonal succession. 

Bergstrom (1971a, 1971b) has discussed the relationship between the three zones identified, zones in 

the standard graptolite s·equence, and the stages and 

series into which they are grouped in the North Atlantic Province. It is sufficient here to note that the 

A. superbusj A. oTdovicicus zonal boundary may approximate the Caradocian-Ashgillian Series boundary of the British standard sequence and that this 

level is likely to be within the lower 40 feet of the 

Maysvillian Stage of the standard Cincinnatian sequence of North America. 

Sweet and others (1971) described a sequence of 

conodont faunas that could be reconstructed from 

collections derived from sections of Middle and Upper Ordovician rocks at various places in the North 

American Midcontinent Province. These faunas are 

readily distinguished from one another, but it could 

not be concluded with assurance that they represent 

an unbroken sequence, and they characterize rock 

successions of greatly different thickness and areal 

extent. Consequently, rocks yielding representatives 

of these faunas were not formally described as zones, 

and it does not se·em useful to do so now. It may be 

noted, however, that rncks distinguished by elements 

of Fauna 8 of Sweet and others ( 1971) occupy the 

lower 55 feet of the composite section of this report; 

that strata between 55 and 200 feet above the base of 

the composite section yield repres·entatives of Fauna 

9; that Fauna 10 is represented in rncks 200 to 410 

feet above the base of the composite; that Oulodus 

oregonia (in the sense of this report), which is the 

index to Fauna 11, characterizes an interval 410 to 

655 fe·et above the base of the composite section; and 

that species characteristic of Fauna 12 are represented in at least modest abundance from 800 to 

1,040 feet above the base of the sam·e composite section. Rocks between 655 and 800 feet above the base 

of the composite section lack conodonts that are restricted to any of the several faunas described by 

Sweet and others (1971). Figure 2 shows that this 

latter interval is marked by pronounced shallowing 

at all depositional sites in the Cincinnati region, and 

by the first major spread of Rhipidognathus in this 

area. As mentioned previously, this interval is also 

characterized by complete disappearance from the 

Cincinnati region of PandeTodus and Belodina, which 

are regarded as typical of the interior subprovince 

of the North American Midcontinent Province. As 

characteristic components of Fauna 12 of Sweet and 

others (1971) are interior-subprovince faunal elements, it seems reasonable to conclude that during 

the latter half of Maysvillian time, the Cincinnati region was not in open communication with the in-
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G13 

terior subprovince, and that it may well have been 

during this interval that broad uplift and erosion 

produced the unconformity that separates, for example, the Dubuque Formation and Maquoketa Shale 

of the Upper Mississippi Valley. 

CORRELATIONS 

Correlation of sections within the Cincinnati region has been effected by comparison of relativeabundance logs, in the manner described in a previous section of this report. These correlations are 

translated into a more general diagram in figure 3. It 

is difficult to show in a single two-dimensional chart 

all the relations between the many named facies in 

the Ordovician of the Cincinnati region. However, 

figure 3 summarizes the arrangement of major postTyrone lithic units indicated by the distribution of 

conodonts along the general southeast-to-northwest 

line on which the logs of figure 2 are arrayed. 

No attempt is made here to interpret the arrangement of stratigraphic units displayed in figure 3 historically. However, it may 'be appropriate to note 

that, from 31t least the midparl of the Lexington 

Limestone upward, facies along the right side of 

figure 3, beneath the heading "N .-central Kentucky," 

appear to have accumulated in water that was relatively shallower and1 more agitated than was the 

water in which contemporaneous facies shown in the 

left side of the diagram were deposited. 

Conodont-based correlation of the Lexington 

Limestone and younger Ordovician rocks of the Cincinnati region with strata in the type area of the 

SERIES Sl AGE SE. INDIANA SW. OHIO N. CENTRAL KENTUCKY 

z 

<( 

~ 

<( 

z 

z 

u 

z 

·u 

z 

<( 

(5 

z 

0 

~ 

I 

~ 

a: 

••••• 

z 

<( 

::J 

...J 

> (/'J 

>- <( 

~ 

z 

~ 

z 

w 

0 

w 

•••••••• 

z 

<( 

z 

~ Cl. 

~ 

<( 

I 

u 

z 

~ 

z 

<( 

~ 

a: 

w 

I 

(/'J 

Dillsboro 

Formation 

Kope Formation 

• • • • • • • • • • • • • • • • • • • • • • Lexington Limestone • • • • • • • • • • • • • • • • • • • • • 

Tyrone Limestone 

------------- ---------~ FIGURE 3.-Correlation of post-Tyrone Ordovician rocks of the Cincinnati region, as suggested by the distribution of 

. conodonts in the sections whose locations are shown in figure 1. 
G14 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Trenton Group was effected by Sweet and Bergstrom 

( 1971), who have reported the1ir procedures and conclusions elsewhere. Their correlations indicate that 

the base of the typical Edenian Stage and the top of 

the typical Shermanian Stage are at essentially the 

same biostratigraphic level. As a consequence of 

thos~e correlations, they suggested that the top of the 

Champlain~an Series (the North American Middle 

Ordovician) be defined by ·the base of the Cincinnatian Series, which, by convention, is the base of 

the Edenian Stage at its type locality. They also 

noted that a substantial part of the Trenton Group, 

long thought to be entirely pre-Cincinnatian in age, 

is, in fact, laterally equivalent to rocks of Edenian 

and early Maysvillian age. To recognize this equivalence, they suggested ·that the· Cobourgian Stage be 

dropped from the standard sequence of time-stratigraphic units for North American Ordovician rocks, 

and that the term "Trenton" be used only in the combination "Trenton Group" to distinguish a major 

body of rock in N·ew York and adjacent Ontarionot in a time-stratigraphic sense, as has been cus"" 

tomary for many yea:rs. 

A·ccording to Bergstrom (1971a, 1971b) the upper 

boundary of the Amorphognathus tvaerensis Zone, 

which is about 200 feet above the base of the composite section for the Cincinnati re~gion, is probably 

in the upper part of the Diplograptus multidens 

graptolite zone; the A. superbus Zone 200 to 580 feet 

above the base of the ·Composite, includes strata elsewhere that are assignable to the upper D. multidens, 

the Dicranograptus clingani, and the lower Pleurograptus linearis graptoUte zones; and the A. ordovicicus Zone, above 585 feet in the composite, includes equivalents of the upper Pleurograptus linearis, the Dicellograptus complanatus, and, presumably, the D. anceps graptolite zones. Thus, at least 

broadly, rocks between the base of the Lexington 

Limestone and a level 30 to 40 feet above the base of 

the Mays villi an Stage are of Caradocian Age ; and 

rocks above 585 feet in the composite section are 

Ashgillian. 

TAXONOMIC REMARKS 

As collections have grown and experience with 

multielement taxonomy has enlarged, ·concepts of the 

species and genera of conodonts represented in Ordovician rocks of the Cincinnati region have also 

changed. Thus, concepts currently represented by the 

names used in preceding sections of this report and 

in table 1 are .indicated in the following paragraphs. 

As will be apparent, several taxa need additional 

study, and others can be revised on the basis of 

existing information. Systematic treatments of the 

latter category are not included, however, for this is 

intended to be a synoptic report, or status summary, 

on Cincinnati region Ordovician conodonts, not a 

complete systematic catalog. 

Amorphognathus ordovicicus Branson and Mehl, 1933 

The current concept of this species is that of 

Bergstrom (1971a), who recognized that elements of 

the so-rt referred to· the form-species Goniodontus 

superbus Ethington, 1959, are the d.iagnoSJtic components of the ske·letal apparatus of A. ordovicicus. 

Holodontiform elements of this type have not yert 

been collected from Ordovician rocks in the Cincinnati region. However, we do have very advanced 

specimens of A. superbus, the evolutionary predecessor of A. O'rdovicicus, from rocks in the lower 30 feet 

of the Maysvillian Stage, and numerous specimens o.f 

the other skeletal components of an A·morphognathus 

have been recovered from rocks well above that level. 

Thus specimens of Amorphognathus from above 585 

feet in the composite section have been arbitrarily 

assigned to A. ordovicicus and in table 1, the species 

is shown to range as high as 785 feet above the base 

of the composite section. · 

Amorphognathus superbus (Rhodes, 1953) 

Bergstrom's ( 1971a) concept of this species is 

followed. The apparatus is distinguished by ele·ments 

of the type p·reviously identified as H olo-dontus super bus Rhodes ( 1953). Elements of the latter type 

ar·e quite s.mall, and they are not numerous in collections from the Cincinnati region. However, enough 

of them occur to indicate that A. superb'US ranges 

from 205 to about 580 feet above the base of the 

composite section (table 1). 

Amorphognathus tvaerensis Bergstrom, 1962 

Representatives of Amorphognathus from samples 

below 200 feet in ·the oomposite section are assigned 

to this species, which is characterized by its distinctive amorphognathiform elements (Bergstrom, 

1971a, pl. 2, fig. 10; Sweet and others, 1971, pl. 1, fig. 

24). In the Cincinnati region, A. tvaerensis ranges 

from 40 to 200 feet above the base of the composite 

s!ection. 

Aphelognathus kimmswickensis 

Sweet, Thompson, and Satterfield, 1975 

In two samples ( OSU 65GV -0.5 and 70ZA-665) in 

the lower 44 feet of the ·composite s·ection, a large 

number of distinctive aphelognathiform elements are 

associated with an array of ramiform and prioni-
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION Gl5 

odiniform elements like thos·e on which Sweet, 

Thompson, and Satterfield (1975) based A. kimmsw·ickensis. All these specimens are here assigned to 

A. ki·mmswickensis, which is based on material from 

the Kimmswick Limes.tone of Missouri. 

AtJiwlognatlms fJOlitrts (Hinde, 1879) 

Bergstrom and Sweet ( 1966) regarded robust 

ozarkodiniform elements with a prominent gap in 

the denticle profile just ante·rio.r to the cusp as representatives of a single-element species, OzaTkodina 

polita (Hinde). Subsequently (Sweet and others, 

1971), after comparisons with the type material of 

Aphelognathus gTandis Branson, Mehl, and Branson 

(1951), the species was transferred to Aphelognathus. Further, in the reexamination of colle·ctions that 

preceded preparation of this report, it has been noted 

that elements assignable to A. politus are especially 

characteristic of collections from the southern Cincinnati region, where they occur with robust ramiform and prioniodiniform elements that were previously regarded as co.mponents of the Plectodina fuTcata apparatus. It now seems likely that P. fuTcata 

and A. politus had skeletal app·aratus•es of closely 

similar archite·cture, which differed most prominently in the conformation of ·their ozarkodiniform elements. Thus, in samples that contain the ozarkodiniform elements of bo.th species, it is difficult or impossible to determine which ramiform and prioniodiniform elements should be assigned to which species. 

In samples that contain only politus-type ozarkodiniform elements, however, associated ramiform and 

prioniodiniform elements do differ somewhat from 

those typical of Plectodina [u1·cata. That is, they are 

not only more robust than those of P. fuTcata, but 

their cusps also tend to develop lateral flanges; the 

antero-basal corner of their cyrtoniodiform elements 

tends to be produc·ed into a denticulate anterior process; and their cordylodiform elements tend to develop the inwardly deflected, denticulated anterior 

process that Branson, Mehl, and Branson ( 1951) 

regarded as chara.cteristic of the form-genus 

Eoligouodina. 

Aphelognath·us politus, as characterized in the preceding paragraph, ranges from 125 to 1,025 feet 

above the base of the composite section. Distribution 

in the Cincinnati region suggests that A. pol?:t·us inhabited essentially the same depth zone as Plectodhza 

fm·cata but that it replaced P. fur-cata in the shallower water environments of the southern Cincinnati 

region. Because of the obviously close relationship 

between A. politus and P. [u1·cata, it may well be that 

assignment to different genera is overly artificial. A 

separate assignment is retained, however, pending 

completion of a thorough study of phylogenies in 

the Plectodina-Aphelognathus-Oulodus complex of 

speeies. 

Belodina compressa (Branson and Mehl, 1933) 

The current concept of this s:pecies is the same as 

that of Bergstrom and Sweet (1966, p. 312-315, Pl. 

31, figs. 12-19). The skelebal apparatus was co.mposed of two belodiniform elements (Belodus gYandis 

and B. wyko.ffensis of Stauff·e-r, 1935b) and an ois.todiform elem·ent ( Oistodus foTnicalus Stauffer, 1935b; 

or Eobelodina foTnicala (Stauffer) of Swee.t and 

others, 1959). Belodina compTessa .is regarded as a 

member of the fauna ·Of the interior subprovince of 

the Midcontinent Province, and it ranges from the 

ba.se to a level 565 feet above t.he base o.f the compo~ite section. 

Beloclina monitorensis Ethington and Schumacher, 1969 

The lowe·r Lexington specimens described as Beladina sp. ·cf. B. inoTnata (Branson and Mehl) by 

Bergstrom and Sweet (1966, p. 315-317, pl. 32, figs. 

6-8) are herein assigned to Belodina monitoTensis, 

which was established by Ethington and Schumacher 

( 1969) for material fro·m the Copenhagen Formation of Nevada. The skeletal apparatus of this s.pedes 

consists of three morphologically distinct ele.ments. 

Two are prominently costate along the ·convex margin and differ primarily in degree of longitudinal 

curvature. The third element, which may be homologous with the oistodifo:rm ·component of B. compTessa, is strongly curved, distinctly bowed, marginally acos.tate, and does not develop the basal notch 

and midlateral groove of the other two elements of 

the ass·embly. In the Cincinnati region, B. monitoTensis ranges fro·m the bas·e to 55 feet above the base of 

the composite section. 

Beloclina profunda (Branson and Mehl, 1933) 

Collections from Richmondian rocks of the Cincinnatian type area include a few specimens that appea.r 

to represent this form-taxon. These specimens were 

described and illustrated by Kohut and Sweet 

( 1968), and no additional material has been collected. Spedmens like this probably were co·mponents 

of skeletal apparatuses that were at least broadly 

similar to those of B. compTessa and B. monitorensis, 

but the material at hand does not justify recognition 

or description of such an assembly. It might be noted, 

however, that elements identified as B. pr-ofunda, B. 

ornata, and B. inoTnata have the s.ame stratigraphic 

range in Ordovician rocks of the Batesville district, 

Ark. (Craig, 1968), and these three form-spe·cies to-
G16 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

gethe·r may represent the apparatus of a single multielement species. Forms identified as B. profunda. 

range from 800 to 1,015 feet above the base of the 

Cincinnati region composite section. 

Bryantodina abrupta (Branson and Mehl, 1933) 

Bergstrom and Sw·eet ( 1966) used this name fo·r a 

multielement species whose skeletal apparatus was 

known to contain only bryantodiniform and prioniodiniform elements. A distinctive assembly of ramiform elements having a stratigraphic range very 

similar to that of B. abrupta, was assigned to Plectodina? posterocostata Bergstrom and Sweet, 1966, 

and a few distinctive cyrtoniodiform elements that 

oc·cur in the same stratigraphic interval we~re described as Cyrtonio-dus s~p. nov. Although none of 

these elements is abundantly represented in the collections at hand, it may be noted that, coUeCJtively, 

they form an assembly that is strikingly similar to 

that of multielement B. typicalis Sttauffer, 1935a, and 

various species of Plectodina, Aphelognathus, Oulodus, and Ozarkodina. Thus, in this summ·ary the conc·ept of-· the s·keletal architecture of"'Bryan-todina 

abrupta has been broadened to include all the specimens described as Plectodina? posterocostata and 

Cyrtoniodus sp. nov., by Bergstrom and Sweet 

( 1966). Roscoe ( 1973) noted a similar association in 

samples from the Middle Ordovician of the Lake 

Champlain district. B. abrupta ranges from 5 to 475 

feet above the base of the composite section, but the 

speeies is not abundantly represented at any level in 

the Cincinnati region. 

Bryantodina staufferi Bergstrom and Sweet, 1966 

Current collections contain only a few more specimens of this distinctive spedes than were available 

to Bergstrom and Sweet ( 1966) when they prepared 

the original diagnosis and illustrations of it. These 

new specimens indicate that the trichonodelliforn1 

elements tentatively associated with B. staufjeri by 

Bergstrom and Sweet ( 1966) were surely parts of 

its skeletal apparatus, which also included fragile 

hindeodeHiform elements that are morphologically 

gradational with the p·rioniodiniform ones o·riginally 

included. B. stau.f!eri ranges from 60 to 410 feet 

above the base of the composite section. 

Cyrtoniodus sinclairi Ethington and Furnish, 1960 

The concept of this form-species followed here is 

that of Ethington and Furnish ( 1960) and Kohut 

and Sweet (1968), who originally reported it from 

rocks of the Cincinnati region. These distinctive elements are suspected to have been components of the 

apparatus of an Aphelognathus or Oulodus species, 

but a conclusion on this m~tter will not be poss-ible 

until a major study of conodonts from rocks of the 

western midcontinent is completed. Elements identified as C. sinclai1·i range from 820 to 1,040 feet above 

the base of the Cincinnruti region composite section. 

Drepanojstodus suberectus (Branson and Mehl, 1933) 

The current concept of this species is the same as 

that expressed by Bergstrom and Sweet ( 1966, p. 

330-333 ; pl. 35, figs. 22-27) , but the species is referred to Drepanoistodus Lindstrom, 1971, rather 

than to Drepanodus Pander (1856). The three coniform e~lements of this distinctive and apparently cosmopolitan species occur in virtually every sample in 

the collections from Dooatur County, Ind., the Cincinnati area, and the Maysville· area of the Cincinnati region. In the southern Cincinnati re-gion, however, D. suberectus is abundantly represented only 

below the level at which Rhipidognathus appears in 

force (fig. 2), and elements of this species are absent 

or rare in the uppermost parts of composi~te sections 

in the northern Cincinnati region, which are also 

dominated by Rhipidognathus. The cosmopolitan occurrence of D. suberectus is interpreted to indicate 

that it inhabited near-surface waters. However, the 

absence or greatly diminished abundance of D. suberectus elementis in rocks dominated by spec'imens of 

Rhipidognathus may indicate that its optimum habitat was an offshore, open-water environment, rather 

than the nearer shore, very shallow water environment apparently favored by Rhipidognathus. 

"Fibrous" conodonts 

In this catego-ry are included ·conodont elements of 

a variety of mo-rphologic types, which are distinguished by their robust construction, peglike denticulation, fibrous fracture, and minor content of "white 

matter." Almost certainly, these elements were components of several multielement apparatuses and the 

entire category they represent merits detailed study 

and revision. Such a study must be based on much 

larger collections than the ones at hand, ho·wever. 

Hence, all elements of fibrous habitus are grouped 

together here. They clearly represent species that 

were most abundant and most widely distributed in 

very shallow water, ne,arshore environments. Fibrous 

conodonts are represented sporadically in collections 

from Lexington and younger Ordovician strata, from 

the base of the Lexington to a level 555 feet above 

the base of the composite section. They are the principal components, however, of ptre-Lexington conodont faunas in the Cincinnati region. 
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G17 

lcriodella superba Rhodes, 1953 

The complete skeletal apparatus of this species 

was des·cribed and illustrated by Bergstrom ·and 

Swe•et (1966, p. 337-340; pl. 29, figs. 1-11), and the 

current concept of it remains the same as theirs. I. 

supe?·ba was interpreted as a member of the fauna 

of the North AUantic (or European) Province by 

Bergstrom and Sweet, and the do.minan:ce of I. supe?·ba elements over those of other North Atlantic 

species in .the relatively shallower water rocks of the 

southern Cincinnati re·g.ion l·ed Seddon and Sweet 

(1971) to ·conclude that I. superba inhabited a shallower depth-zone tha.n Amorphognathus, the other 

major North Atlantic ·component in Ordovician rocks 

of the Cincinnati region. However, the distributional 

data presented by Seddon and Sweet might also be 

interpreted to mean that Icriodella and Amorphognathus inhabited ·essentially the same depth-zone, 

but that I criodella was relatively more .abundant 

than AmO?·phognathus in the nearer ,shore environmenrts in which rocks of the southern Cincinnati region were deposited. 

Oulodus oregonia (Branson, Mehl, and Branson, 1951) 

Bergstrom and Sweet ( 1966) united under this 

name a distinctive assembly of prioniodiniform, cordylodiform, and oulodiform elements, :to which they 

later added (Sweet and Bergstrom, 1972) some of 

the trichonodelliform and zygognathiform elements 

they had previously refe,rred to Plectodina furcata 

(Hinde). Currently, then, t.he skeletal apparatus of 

this species is thought to have been composed of a 

complete .symmetry-transition s•e·ries of trichonodelliform, zygognathifo·rm, and cordylodiform elements; an oulodiform element; a pTioniodiniform 

element with a short anterior process, which may be 

homologized with the neoprioniodiform element of 

younger prioniodinacean skeletal apparatuses; and a 

prioniodinifo,rm elem·ent with subequal anterior and 

posterior processes. A full description of this species, 

as presently conceived, is included in a general study 

of Ordovician and Sil U1rian species of Oulodus by 

Sweet a.nd Schonlaub ( 1975). It should be noted 

here, ho·wever, that the species to which Bergstrom 

and Sweet referred in 1966 is the one herein named 

Oulodus subund-ulatus (Sweet and others, 1959). 

That is, i·t now .seems certain tha.t, although elements 

indistinguishable from those nam·ed Prioniodina 

oregonia by Branson, Mehl, and Branson (1951) 

have a long stratigraphic range in the Cincinnati 

region, the type specimen of that form-species (and 

thus the namegiver of multielement 0. oregonia) 

was part of an apparatus in which the neoprioniodiform element wa.s the distinctive form named Prioniodina velicuspis by Pulse and Sweet ( 1960) -not the 

slender-cusped neoprioniodiform element included by 

Bergstrom and Swe,et. In short, the· skeletal apparatus of the species named Oulodus oregonia in 

this report is distinguished by its broad-cusped neoprioniodi:Dorm element, which is the element Pulse 

and Sweet ( 1960, p. 259-260, Pl. 36, figs. 5, 13) 

named Prioniodina velicuspis. 

Oulodus oregonia is very useful as a guide to rocks 

of middle Edenian to middle Maysvillian Age in the 

southern part of the Cincinnati region. The species 

ranges from 410 to 655 f,eet above the base of the 

composite section. 

\ 

Oulodus robustus (Branson, Mehl, and Branson, 1951) 

Kohut and Sweet (1968, p. 1471, pl. 185, figs. 12, 

14, 15, 17, 24) described the essentially complete 

apparatus of this species as Plectodina robusta, but 

they failed to note that oulodiform el·ements associated in the same samples with representatives of 

this species are clearly parts of the same skeletal 

apparatus. Such elements (referred to Oulodus 

oregonia by Kohut and Sweet) are here included in 

the apparatus, and the species is thereby transferred 

from Plectodina to Oulodus. The complete apparatus, 

as now interpreted, is illustrated by Sweet and 

Schonlaub (1975). 0. robustus ranges from the base 

of the Maysvillian Stage to a level very near the 

top of the Richmondian Stage in the Cincinnati region (from 550 to 1,000 feet above the bas,e of the 

composite section). 

Oulodus subun.dulatus (Sweet and others, 1959) 

As noted in a previous paragraph, the species 

named Oulodus oregonia by Bergstrom and Sweet 

(1966, p. 342-347, pl. 32, figs. 20, 21; pl. 33, fig. 5; 

pl. 34, figs. 13-16) requires another name because the 

type specimen of the namegiving prioniodiniform 

element was almost certainly a component of a multielement apparatus distinguished by neoprioniodiform 

elements of the type named Prioniodina velicuspis by 

Pulse and Sweet (1960). Sweet and Schonlaub 

(1975) used the trivial name subundulatus for this 

species because at least one of the cotypes of T?·ichonodella subundulata Sweet and others (1959) 

was undoubtedly part of the apparatus of this 

Oulodus species. As thus defined, 0. subundulatus 

may be represented 115 feet above the base of our 

composite section but is almost continuously present 

in samples betwe·en 140 and 405 feet above the base 

of that section. 0. subundulatus was apparently the 

progenitor of 0. oregonia, and the level of transition 
G18 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

from this species to 0. oregonia is a very useful biostratigraphic horizon in at least the southern and 

Maysville districts of the Cincinnati region. 

OulOtlus ulrichi (Stone and Furnish, 1959) 

Available collections include only a small number 

of specimens of the eoligonodiniform element that 

distinguishes this species, which was regarded by 

Kohut and Sweet (1968, p. 1469, pl. 185, figs. 7, 11) 

as a subspecies of 0. oregonia (Branson, Mehl, and 

Branson, 1951). From a study of these specimens, 

little can be added to the discussion of Kohut and 

Sweet except the obs1ervation that the species is 

probably more closely related to 0. robustus (Branson, Mehl, and Branson, 1951) than to 0. oregonia 

and might as appropriately be regarded as a subspecies of 0. robustus. In the co-mposite section, 0. 

ulrichi ranges from 805 to 1,025 feet above the base 

and is a rare but distinctive component of the Richmondian conodont fauna locally. 

Panderodus angularis (Branson, Mehl, and Branson, 1951) 

The description and illustration of elements charact~eristic of this species presented by Branson, Mehl, 

and Branson (1951, p. 8, pl. 1, figs. 34-39) and by 

Kohut and Sweet (1968, p. 1469, pl. 185, figs. 20, 

23, 27) are adequate for recognition of the species, 

which is regarded as a Late Ordovician component 

of the fauna of the interior subprovince of the North 

American Midcontinent Pro-vince. 

Parulerodus gracilis (Branson and Mehl, 1933) 

The concept of this spec,ies employed here is that 

of Bergstrom and Sweet (1966, p. 355-359, pl. 35, 

figs. 1-6) and Kohut and Sweet (1968, p. 1469-1470, 

pl. 185, figs. 1, 6, 9, 10, 13, 16), whose studies were 

based on essentially the sam~e material. P. gracilis, a 

component of the conodont fauna of the interior subprovince, was interpreted by Seddon and Sweet 

(1971) as an inhabitant of a depth zone that was 

relatively shallower than that favored by Belodina, 

which is also charact,eristic of the interior subprovince. 

Panderodus sp. aff. P. panderi (Stauffer, 1940) 

Specimens discussed under this cumbersome designation are the same ones that were referred by Bergstrom and Sweet ( 1966) to Panderodus panderi 

(Stauffer), which is common, but rarely represented 

in abundance, in rocks of late Maysvillian and Richmondian age elsewhere in the North American Midcontin-ent Province, but is yet unknown in the Cincinnati region. Craig (1968) has made a detailed 

study of P. panderi, and has pointed out that typical 

forms differ from those of middle Maysvillian and 

older rocks in having an ungrooved face that is flat 

and inclined slightly toward the posterior. Cincinnati 

re·gion specimens assigned to P. panderi by Bergstrom and Sweet ( 1966), on the other hand, are 

typically smaller and more slender, and both lateral 

faces are convex. Craig referred elements of the 

latter type to a new species, but the name he has 

proposed for that species and his diagnosis of it have 

not yet been published. 

Panderodus staufferi (Branson, Mehl, and Branson, 1951) 

Available collections contain only a few representatives of this single-element species, but those specimens conform closely to the types (Branson, Mehl, 

and Branson, 1951, p. 7, 8, pl. 1, figs. 23-27; Kohut 

and Sweet, 1968, p. 1470, pl. 186, figs. 4, 5). P. 

staufjeri, like other species of Pande1·odus, is regarded as a component of the fauna of the interior 

subprovince. 

Paroistodus? mutatus (Branson and Mehl, 1933) 

Bergstrom and Sweet (1966) united acodiform 

and acontiodiform elements previously referred to 

the form-species Belodus? mutatus Branson and 

Mehl 1933; Acodus inornatus Ethington, 1959; and 

Distacodus procerus Ethington, 1959, as co·mponents 

of the skeletal apparatus of a single multielement 

species, for which they used the name Acodus mutatus (Branson and Mehl, 1933). Barnes and Poplawski ( 1973) suggested that the specimens Bergstrom and Sweet (1966) identified with Oistodus 

venustus Stauffer, 1935b, may also· have been components of the A. mutatus apparatus, and that the 

species thus represented might be more properly referred to Paroistodus Lindstrom, 1971, than to 

Acodus Pander, 1856. Although it is not ·Certain that 

the oistodiform elements identified with 0. venustus 

by Bergstrom and Swe,et ( 1966) were components 

of the same apparatus as elements identified as A. 

mutatus, they are included tentatively with those 

elements under the name Paroistodus? mutatus in 

the tabulations in this report because they have essentially the same stratigraphic range in the composite section as do el,ements of A. mutatus. It is 

also not certain that Paroistodus is the best generic 

assignment, for Lindstrom (1971) noted that the 

basal cavity of Paroistodus elements tends to become "inverted" anteriorly whereas this feature is 

not'r:. ~en in any of the elements at hand. Possibly 

these elements are skeletal components of a species 

of an undescribed and unnamed genus. 
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G19 

Periodon gramlis (Ethington, 1959) 

The complete multielem,ent apparatus of this 

North Atlantic Province species was described by 

Bergstrom and Sweet ( 1966, p. 363-365, pl. 30, figs. 

1-8) and the concept of it remains unchanged. In 

the composite s~ection, P. gTandis ranges from 65 to 

450 feet above the base, but it is n'ot a conspicuous 

faunal element at any level. 

Phrngmotlus llllllatus Bnmson and Mchl, 1933 

Representatives of this multielement sp,ecies dominate collections of oonodonts from the Cincinnati 

region, where the species ranges from the base to 

990 f·eet above the base of the composite section. The 

skeletal apparatus of P. undatus was fully described 

by Bergstrom and Sweet (1966, p. 369-372, pl. 28, 

figs. 13-20), and additional n1aterial collected since 

1966 merely confirms their reconstruction and interpretation. Seddon and Sweet ( 1971) .concluded 

that P. undatus inhabited a relatively deeper lifezone in Ordovician seas than did Plectodina fuTcata, 

the other major component of the indigenous fauna 

of the Cincinnati region. 

Plectotliua aculeata (Stauffer ,1930) 

In their study of Lexington Limestone conodonts, 

Bergstrom and Sweet (1966, p. 373, pl. 32, figs. 15, 

16; pl. 33, figs. 22, 23; pl. 34, figs. 5, 6; text fig. 9AF) recognized a close association in range and a 

striking simjlarity in morphology between certain 

trichonodelliform, zygognathiform, and cordylodiform elements from the lower part of the Lexington, 

and they concluded that all these elements were once 

parts of the skeletal apparatus of a single species, 

Plectodina aculeata (Stauffer). Subsequently, it became apparent that the group of elements assigned 

to P. aculeata by Bergstrom and Sweet has the same 

geographic and stratigraphic distribution as the 

group of ozarkodinif·orm, prioniodiniform, and 

dichognathiform elements they united as Ozarkodina? obliqua (Stauffer, 1930). Hence, elements of 

both these groups have been combined and are referred collectively to P. aculeata. As presently conceived, the skeletal apparatus ·Of P. aculeata includes 

not only the symmetry-transition series of elements 

originally included in it by Bergstrom and Sweet, 

but also the ozarkodiniform, dichognathiform, and 

prioniodiniform elements they assigned to 0.? obliqua (Stauffer) (Sweet and Bergstrom, 1970). The 

base of the range of P. aculeata is well below that of 

the stratigraphic interval considered in this report, 

and the top of its range locally is 65 feet above the 

base of the c.omposite section. 

Plectodirw furcata (Hinde, 1879) 

Elements of this species, and those of Phragmodus undatus, make up the bulk of conodont collections from the Ordovician of the Cincinnati region. The ooncept of the skeletal architecture of the 

species has evolved and is now somewhat broader 

than was that of Bergstrom and Sweet (1966, p. 

377-382), who were the first to recognize its occurrence in the rocks discussed in this report. Further, 

it has also become clear (Sweet and Bergstrom, 

1970) that the specimens assigned to OzaTkodina 

tenuis Branson and Mehl, 1933, and Cyrtonio.dus 

fiexuosus (Branson and Mehl, 1933) were parts of 

the P. ju1·cata apparatus, but that some of the other 

form-categories united in P. fuTcata by Bergstrom 

and Sweet (1966) and by Kohut and Sweet (1968) 

were interpreted so broadly as to include components of the skeletal apparatuses of various species 

of Aphelognathus and Oulod~ts. Brief discussion of 

these matters is clearly appropriate here so that it 

will be clear what is meant by P. fuTcata elsewhere 

in this report. 

In 1969, Kohut reported that the trichonodelliform, zygognathiform, cordylodiform, and prioniodiniform elements united by Bergstrom and Sweet 

(1966) as Plectodina furcata (Hinde) form a recurrent group that also includes the cyrtoniodiform 

elements assigned to CyTtoniodus fiexuosus (Branson and Mehl) and the ozarkodiniform elements assigned to OzaTkodina tenuis Branson and Mehl by 

Bergstrom and Sweet (1966). Mutual affinities in 

this group were reported to be 0.93, and rank-correlations between all pairs in thjs group, except 

those containing 0. tenuis, were significantly positive. Kohut thus expanded Bergstrom and Sweet's 

concept of P. ju1·cata by including the elements they 

assigned to Cyrtoniodus fiexuosus; but, despite their 

occurrence in the initial group, he excluded the elements they referred to 0. tenuis because rank-correlation values were not significant. 

Kohut's conclusions were appropriately conservative, but we believe that other considerations argue 

strongly in favor of including in P. furcata the 

ozarkodiniform elements he excluded on rank-correlation grounds. That is, comparison of the P. fuTcata apparatus· with that of other prioniodont and 

polygnathacean apparatuses (Sweet and Bergstrom, 

1972) suggests that the P. ju1··cata apparatus is incomplete without an ozarkodiniform element, which 

Kohut showed to be an essentially constant member 

of the recurrent P. furcata group. Failure of this 

element to show significant rank-correlation with 
G20 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

other elements of the group is attributable, we believe, to several factors. Probably the most important o.f these is the fact that fragments were included 

in many of the frequency tabulations used by Kohut 

and no assurance exists that some specimens were 

not counted twice or several times. In addition, it 

now seems certain that the ramiform-element plexus 

assigned in its entirety to P. furcata by Bergstrom 

and Sweet (1966) and Kohut (1969) was shared by 

P. furcata, Oulodus oregonia, and Aphelognathus 

politus. Thus frequencies of these ramiform elements 

used by Kohut shoul<L-Probaqly .. hav.e-~.been __adjusted 

· ···· by removal of elements now thought to be assignable 

to species of Oulodus and Aphelognathus. Consequently, including in P. furcata the elements referred by Bergstrom and Sweet (1966) to Ozqrkodina tenuis, .the high level of affinity they exhibit to 

others of the P. furcata group is emphasized and the 

importance of rank-correlation values obtained by 

Kohut is minimized. 

As now conceived, the skeletal apparatus of 

Plectodina furcata (Hinde) includes a symmetrytransition series of trichonodelliform, zygognathiform, and cordylodif.orm elements; a cyrtoniodiform 

element of the type assigned by Bergstrom and 

Sweet (1966) to Cyrtoniodus fiexuosus (Branson 

and Mehl) ; a prioniodiniform element; and an 

ozarkodiniform elem-ent of the type described as 

Ozarkodina tenuis Branson and Mehl by Bergstrom 

and Sweet. Process denticles of all elements tend to 

be compressed in the plane of the process and laterally confluent, and this feature serves to distinguish 

them from comparable structures of various species 

of Oulodus, which are characterized by discrete, peglike denticles. In samples that contain both the 

ozarkodiniform elements of P. furcata and the 

aphelognathiform elements of Aphelognathus politus, it is difficult to distinguish between ramiform 

elements of the two species. In samoles that have 

only aphelognathiform elements, howe~er, associated 

ramiform components are more stoutly constructed; 

cusp·s tend. to be· prominently costate marginally; 

and cyrtoniodiform elements tend to develop downwardly directed, denticulated anterior processes. 

Seddon and Sweet (1971) concluded that Plectodina furcata inhabited relatively shallower water 

than Phragmodus undatus, a common associate. 

They did not distinguish between Plectodina and 

Aphelognathus, however, so their conclusion also requires some m!Odification. That is, it is now clear 

that P. furcata was replaced laterally, in the same 

depth-zone but in the shallower water of the southern Cincinnati region, by Aphelognathus politus. 

Thus, P. furcata may still be regarded as an inhabitant of a relatively shallow depth-zone, but it was 

probably most characteristic of the more offshore 

environment and the deeper water areas of the 

northern Cincinnati region. 

Plectodina? undulata (Branson, Mehl, and Branson, 1951) 

The concept of this multielement species adopted 

here is essentially that of Kohut and Sweet (1968, 

p. 1471, pl. 186, figs. 1-3, 14, 16). However, the 

skeletal apparatus of this species is expanded to include the robust, twisted ozarkodiniform elements 

that occur in the same samples but were tabulated 

by Kohut and Sweet as Ozarkodina tenuis Branson 

and Mehl. Som.e reservations are also expressed 

about the reference of this species to Plectodina. 

That is, ·the ozarkodiniform element .associated with 

the apparatus of this species is similar to that of 

P. aculeata and P. furcata, burt rami form elements 

display discrete, peglike denticles of the sort regarded as typical of Oulodus and later genera of the 

Prioniodinacea. 

The characters by which the ramiform components of the skeletal apparatus of Plectod·ina? undulata are distinguished appear for the first time in a 

small group of specimens from the Lexington Limest.one, between 17 4 and 178 feet above the base of 

the composite section. The species is more or less 

continuously represented, however, only from 630 

to 1,015 feet in that section, and in that interval it 

is commonly associated with specimens of OulodU8 

robustus and Rhipidognathus. Thus, P.? undulata is 

regarded as a member of the southern element of 

the indigenous conodont fauna of the Cincinnati 

region, and as an inhabitant of the very shallow 

water environments that prevailed in the southern 

Cincinnati region during much of the Middle and 

Late Ordovician. 

Polyplacognathus ramosus Stauffer, 1935b 

The concept of this spe-cies used here is the same 

as that given by Bergstrom and Sweet (1966, p. 386-

388, pl. 28, figs. 9-12). The species ranges from 15 

to 210 feet above the base of the comp•osite section, 

is known from rocks much older than the Lexington 

Limestone, and is not abundantly represented at any 

level in any of the sections considered in this report. 

Protopanderodus sp. cf. P. dissimilaris 

(Branson and Mehl, 1933) 

Bergstrom and Sweet (1966) described five specimens from the Lexington Limestone as Scandodus 

sp. cf. S. dissimilaris. No additional material has 

been collected, but it should be noted that the speci-
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G21 

mens probably do not represent Scandodus Lindstrom, 1955, as that genus is currently interpreted 

(Lindstrom, 1971). They may well be components 

of the apparatus of the species listed here as Protopanderodus n. sp. cf. P. insculptus, but available material is too small to support this suggestion adequately. Consequently, we ·suggest the possibility 

that these specimens are closely related to those referred to P. n. sp. cf. P. insculptus, by transferring 

them, as a sep·arate entity, from Scandodus to Protopanderodus. The five specimens in question occur 

in samples from an interval 135 to 200 feet above 

the base of the composite section. 

Protopanderodus n. sp. cf. P. insculptus 

(Branson and Mehl, 1933) 

Collections at hand contain only a few specimens 

of this distinctive species, and they are the same ones 

that were referred by Bergstrom and Sweet (1966, 

p. 398-400, pl. 34, figs. 26, 27) to Scolopodus insculptus. These specimens are not included in Scolopodus here, however, for Lindstrom (1971) has 

listed a number of features not recognizable in these 

specimens as characters of specimens he regards as 

typical of Scolopodus. Thus, at least for purposes of 

reference, the species is assigned to Protopanderodus Lindstrom, 1971, although a more comprehensive study of larger collections than are now available probably will result in assignment of specimens 

like this t" a new genus. It also seems likely that 

specimens from the Cincinnati region differ enough 

from the type-specimen of Phragmodus insculptus 

Branson and Mehl, 1933, to be :regarded as representatives of a different species. 

Rhipidognathus rowlandensis Kohut and Sweet, 1968 

The concept of this species is unchanged from that 

given by Kohut and Sweet (1968, p. 1472-1473, pl. 

185, figs. 4, 5) and no new ·material has been collected. R. rowlandensis is an associate of R. symmetricus symmetricus, and a majority of the specimens 

in the collection are from the Rowland Member of 

the Drakes Formation. -

Rhipidognathus symmetricus 

Branson, Mehl, and Branson, 1951 

This species is interpreted here as it was by Kohut 

and Sweet (1968), who recognized two subspecies, 

R. symmet1icus symmetricus Branson, Mehl, and 

Branson, 1951, and R. symmetricus discretus Bergstrom and Sweet, 1966. In representatives of the 

latter subspecies, denticles are robust, elliptical in 

cross section, and discrete at all stages of growth, 

whereas in specimens of the former subspecies, denticles are fragile, compressed, overgrown by successive lamellae, and come to be engulfed in broad 

bladelike structures in late growth stages. R. symmetricus discretus appears first and has the widest 

geographic distribution of the two subspecies, but 

the species as a whole is interpreted to have been an 

inhabitant of the shallowest water and nearest shor~ 

environments represented by any of the many 

lithic facies in the stratigraphic interval under 

consideration. 

Rhodesognathus elegans (Rhodes, 1953) 

Bergstrom and Sweet (1966, p. 393--394, pl. 34, 

figs. 19-23) concluded that the skeletal apparatus 

of this species was hi-elemental; that is, that it 

consisted of only two morphologically distinct ambalodiform elements. Roscoe (1973), however, concluded that some of the elements referred by Bergstrom and Sweet to the multielement species Tetraprioniodus delicatus (Branson and Mehl) were, in 

fact, components of the apparatus of Rhodesognathus elegans and that all of them were not assignable to Amorphognathus as had been concluded by 

Bergstrom (1971a). In support of his opinion, 

Roscoe noted that in tables given by Bergstrom and 

Sweet ( 1966) the ratio between representatives of 

T. delicatus and A. ordovicicus is 1:4 in samples 

that contain specimens of both Amorphognathus 

and Rhodesognathus, whereas it is 1:5.5 in samples 

that contain representatives only of Amorphognathus. Furthermore, Roscoe reported that several of 

his samples from the Glens Falls Limestone in Vermont contained numerous elements of Rhodesognathus and Tetraprioniodus but lacked amorphognathiform or prioniodiform elements that might suggest 

the presence of species in which a Tetraprionioduslike ramiform assembly was also characteristic. 

Roscoe's (1973) interpretation of Rhodesognathus 

elegans is convincing, and my tabulations of Cincinnati region conodonts have been revised to reflect that interpretation. Rhodesognathus will be discussed more fully in a report by Roscoe and 

Bergstrom. 

Stauf!erella falcata (Stauffer, l935b) 

In a report on conodonts from the Cape Limestone 

of Missouri by Sweet, Thompson, and Satterfield 

(1975), the elements referred by Bergstrom and 

Sweet (1966, p. 306-307, 329; pl. 35, fig. 6-16 and 

10-13) and others to Acontiodus alveolaris Stauffer, 

1935b, and Distacodus falcatus Stauffer, 1935b, are 

united as representatives of' a single multielement 

species, for which the generic name Stauff erella is 
G22 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

proposed. This species is a distinctive one, but it is 

rep-resented by only a few specimens in coUe0tions 

from the Cincinn3Jti region, whe,re it ranges fro·m 85 

to 585 feet above the bas~e of the composite section. 

Synprioniodina? forsenta Stauffer, 1940 

No further information about this form-species 

now exists than was available to Bergstrom and 

Sweet ( 1966), who first recognized it in Ordovician 

strata of the Cincinnati region. Elements of the sort 

included in this form-taxon may have been ·co·mponents of a multielement appar.atus like the one identified as BTyantodina staufferi, and they range from 

140 to 395 feet above the base of the composite 

section. 

LOCALITY REGISTER 

Localities are numbered .serially, then identified by their 

Ohio State University (OSU) or U.S. Geological Survey 

(USGS) field designation. Figures in parentheses following 

field-designation numbers, indicate the approximate range 

(in feet) of the section in the composite section for the Cincinnati region, which is 1,040 feet thick. Locality numbers 

correspond to figure 1. 

The Point Pleasant Limestone of figure 3 and the 

following locality descriptions as used by me is a 

body of rock between the top of the Grier Limestone Member of the Lexington Limestone and bases 

of the Clays Ferry or Kope Formations. Use of the 

name Point Pleasant in this sense is consistent with 

that in descriptions· of Cincinnati region geologic 

quadrangle maps published by the U.S. Geological 

Survey prior to 1975, and is the usage advocated by 

Sweet, Harper, and Zlatkin (1974) in their description of the section at locality 42 of this report. Since 

1975, however, the U.S. Geological Survey has confined the name Point Pleasant to a body of shaly 

carbonate rocks interpreted as a northwest-projecting tongue of the Clays Ferry Formation. Such a 

body includes all the rocks exposed at the type locality of the Point Pleasant, but embraces only the 

upper 42 feet of the 111-foot interval assigned by 

Sweet, Harper, and Zlatkin (1974) to the Point 

Pleasant Limestone at locality 42 of this report. 

This is not the place to debate the relative merits of 

these two rather different uses of the name Point 

Pleasant. It is sufficient to indicate the way in which 

the name is used in this report. 

Where U.S. Geological Survey stratigraphic terminology differs from that in the following locality 

register, both sets of terms are used with the U.S. 

Geological Survey nam~s being placed in brackets. 

l. OSU-58A ( 400-738). Maysville (Mason County), Ky. 

Cuts along U.S. Highway 62-68, 1 mi south of Maysville, Ky., Maysville West 7.5-minute quadrangle. Kope 

and Fairview Formations and Grant Lake Limestone; 

58 samples; 4,030 conodont elements. 

2. OSU-58B (545-643). Stonelick Creek (Clermont 

County), Ohio. Natural exposures in bed and banks of 

valley, upstream from a point about 3 mi north of 

Owensville, Stonelick T., Ohio. Batavia 7.5-minute 

quadrangle. Fairview Formation and Grant Lake 

Limestone; 144 samples; 921 conodont elements. 

3. OSU-58C (525-683). White Oak Creek (Brown County), 

Ohio. Exposures in valley of White Oak Creek and in 

cuts along Ohio-U.S. Highway 125, 0.75 mi west of 

Georgetown, Lewis T., Higginsport 7.5-minute quadrangle. Fairview Formation and Grant Lake Lime 

stone; 100 samples; 1,190 conodont elements. 

4. OSU-58D (545-657). Bald Knob (Hamilton County), 

Ohio. Cuts in Cleveland Wrecking Co. storage lot, 

0.5 mi southwest of junction of Western Hills viaduct 

and State A venue, Cincinnati, Ohio. West Cincinnati 

quadrangle. Fairview Formation; 50 samples; 949 

conodont elements. 

5. OSU-58E (?653-?745). Rising Sun (Ohio County), 

Ind. Cut along U.S. Highway 56, 3.0 mi southwest of 

Rising Sun. Rising Sun 7.5 minute quadrangle. Kope, 

Fairview, and Grant lake equivalents; 65 samples; 

461 conodont elements. 

6. OSU-58F (607-670). Bullock Pen and Rice Creeks (Kenton County), Ky. Exposure at Narrows Road-Turkeyfoot Road intersection, 2.0 mi southeast of Erlanger, 

Ky., Independence 7.5-minute quadrangle. Fairview 

Formation; 48 samples; 470 conodont elements. 

7. OSU-58G (570-660). Dry Run (Clermont County), 

Ohio. Exposure 1.0 mi north of U.S. Route 50, 4.5 mi 

southeast of Milford, Stonelick T., Goshen 7.5-minute 

quadrangle. Fairview Formation; 40 samples; 484 

conodont elements. 

8. OSU-58H ( ?579- ?650). Sharon Woods (Hamilton 

County), Ohio. Exposure in Sharon Run, 0.5 mi northeast of Sharonville, Sycamore T., Glendale 7.5-minute 

conodont-elements. 

9. OSU-58J (550-612). Grog Run (Clermont-Warren 

Counties), Ohio. Natural exposure beginning 3.2 mi 

east of Loveland, Goshen-Hamilton Tps., South Lebanon 7.5-minute quadrangle. Fairview Formation; 35 

samples; 417 conodont elements. 

10. OSU-58K (545-654). Rapid Run (Hamilton County), 

Ohio. Natural exposure beginning 2.5 mi northeast of 

Delhi, Delhi T., Burlington 7.5-minute quadrangle. 

Fairview Formation; 62 samples; 1,385 conodont elements. 

11. 0SU-58L (710-755). Camp Kern Run (Warren 

County), Ohio. Natural exposure beginning 0.3 mi 

west of Ft. Ancient, Washington T., Oregonia 7.5-

minute quadrangle. Grant Lake Limestone; 30 

samples; 1,442 conodont elements. 

12. OSU-60A (275-315). Cynthiana (Harrison County), Ky. 

Northeast face of inactive Poindexter quarry, opposite 

County High School on Kentucky Route 982 (old Ky.-

U.S. 27). SE ~4, south-central rectangle, Cynthiana 

quadrangle. Type section of Cynthiana Formation of 

former usage, but here regarded as Point Pleasant 

Limestone [Clays .F~rry Formation]; 35 samples; 

4,364 conodont elements. 
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G23 

13. OSU-60B (293-305). Greendale Station (Fayette 

County), Ky. Cut along Southern Railroad right-ofway about 4 mi north of Lexington and 1,000 ft south 

of intersection of Spurr Road and railroad tracks. 

Lexington west 7.5-minute quadrangle. Possibly type 

section of Greendale Limestone Member of Cynthiana 

Formation of former usage, but her·e included in 

Point Pleasant Limestone [Gre·endale Lentil]; 8 

samples; 1,096 conodont elements. 

14. OSU-60BCK (Eden locality 13098) (222-359). Bear 

Creek (Clermont County), Ohio. East face of inactive 

quarry, east of mouth of Bear Creek, at junction of 

Ohio-U.S. Highway 52 and Ohio Route 222 southeast 

corner Washington T., Moscow 7.5-minute quadrangle. 

Point Pleasant Limestone Tongue of Clays Ferry Formation (82 ft) and Kope Formation (56 ft); 49 

samples; 37,752 conodont elements. 

15. OSU-600 ( ?-?). Rogers Gap (Scott County), Ky. Cuts 

along Southern Railroad right-of-way, about 1 mi 

south of Rogers Gap. SW%SW1,4 east-central rectangle, Delaplain 7.5-minute quadrangle. Possibly type 

section of Rogers Gap Member of Cynthiana Formation of former usage, but here included in Point 

Pleasant Limestone [Clays Ferry Formation]; 12 samples; 621 conodont elements. 

16. OSU-60G (247-342). Sadieville (Scott County), Ky. 

Weathered cuts on east and west sides of KentuckyU.S. Highway 25, 1.65 mi west of Sadieville. SW 1,4 

south-central rectangle, Sadieville 7.5-minute quadrangle. Point Pleasant Limestone [Clays Ferry Formation]; 40 samples; 26,867 conodont elements. 

17. OSU-60H (220-271). Menzie (Pendleton County), Ky. 

Cut along L. and N. Railroad right-of-way, 0.25 mi 

north of Menzie, Ky. NE 14 northwest rectangle, Falmouth 7.5-minute quadrangle. Point Pleasant Tongue 

of Clays Ferry Formation; 16 samples; 4,573 conodont 

elements. 

18. OSU-60L (197-282). Carntown (Bracken County), Ky. 

Abandoned quarry adjacent to Kentucky Route 8 at 

Carntown. SW%. northwest rectangle, Moscow 7.5-

minute quadrangle. Point Pleasant Tongue of Clays 

Ferry Formation; 39 samples; 28,161 conodont elements. 

19. OSU-60M (278-211). Milford (Bracken County), Ky. 

Abandoned quarry on east side of Kentucky Route 19, 

directly east of Milford across North Fork of Licking 

River. NW% east-central rectangle, Claysville 7.5-

minute quadrangle. Point Pleasant Limestone [Clays 

Ferry Formation]; 19 samples; 4,847 conodont elements. 

20. OSU-60P (102-347), USGS-CF (265-356), USGS-CF 

CHIEF (386-487), USGS-CF WEIR (349-487). Clays 

Ferry (Madison County), Ky. Weathered cuts along 

Clays Ferry Road (old Kentucky-U.S. Highway 25) on 

southeast side of Kentucky River. SE 1,4 southwest 

rectangle, Ford 7.5-minute quadrangle. Section begins 

in Kentucky River fault zone and extends upward in 

downthrown block. Lexington Limestone, Point Pleasant Limestone [Clays Ferry Formation] Clays Ferry 

Formation, and Garrard Siltstone; 211 samples; 29,215 

conodont elements. 

21. OSU-60Q (227-243). Willow Creek (Bracken County), 

Ky. Natural exposure in floor and walls of Willow 

Creek valley, upward from point at which Kentucky 

Route 539 crosses the creek and 1.1 mi west-northwest 

of Milford. SE 1,4 north-central rectangle, Claysville 

7.5-minute quadrangle. Point Pleasant Limestone 

[Clays Ferry Formation]; 10 samples; 5,905 conodont 

elements. 

22. OSU-60T (220-299). Falmouth (Pendleton County), Ky. 

Three road cuts on northeast and southwest sides of 

Kentucky-U.S. Highway 27, beginning 0.25 mi southeast of city limits of Falmouth. NW% south-central 

rectangle, Falmouth 7.5-minute quadrangle. Point 

Pl~asant Tongue of Clays Ferry Formation; 34 

samples; 21,564 conodont elements. 

23. OSU-61Z ( 45-627). Middletown (Butler County), Ohio. 

2.25-in. core drilled in 1957 by Texas Eastern Trans-

. mission Corp. on Valentine Apple Farm, SW 1,4 sec. 19, 

Lemon T. (core numbered 860 in files of Ohio Division 

of Geological Survey). Trenton 7.5-minute quadrangle. 

Lexington Limestone, "Utica" (of drillers), Point 

Pleasant Limestone, Kope Formation and Fairview 

Formation; 202 samples; 36,628 conodont elements. 

24. OSU-62DA (986-1001). Ohio Brush Creek (Adams 

County), Ohio. Cut along north side of Ohio Route 

41, immediately south of point at which Route 41 

crosses Ohio Brush Creek, Oliver T., Pebbles 7.5-

minute quadrangle. Preachersville Member of Drakes 

Formation; 4 samples; 1,143 conodont elements. 

25. OSU-63AA (735-1006). Isaacs Creek (Adams County), 

Ohio. Natural exposure in valley walls of Isaacs 

Creek, Sprigg T. Section begins 1.6 mi north of city 

limits of Manchester, Manchester-Islands 7.5-minute 

quadrangle. Grant Lake Limestone, Bull Fork Formation and Preachersville Member of Drakes Formation; 32 samples; 5,135 conodont elements. 

26. OSU-63AB (650-977). China (Jefferson County), Ind. 

Composite of two overlapping natural sections along 

Dry Fork, 1 mi south of China, Canaan, 7.5-minute 

quadrang-le. Dillsboro and Whitewater Formations; 

63 samples; 8,920 conodont elements. 

27. OSU-63AF (735-779). Arnheim (Brown County), Ohio. 

Natural exposure along Straight Creek, 1 mi south 

of Arnheim, Franklin T., Ash Ridge 7.5 minute quadrang-le. Type section of Arnheim Formation (Foerste, 

1905). Grant Lake and Bull Fork facies; 12 samples; 

2,090 conodont elements. 

28. OSU-64S1 (280-315). Banklick Creek (Kenton County), 

Ky. Natural exposure along south side of Banklick 

Creek, 0.35 mi west of the point at which it crosses 

Kentucky Route 177 in Latonia, Ky .. Covington 7.5-

minute quadrangle. Point Pleasant Tongue of Clays 

Ferry Formation; 11 samples; 11,381 conodont elements. 

29. OSU-64S2 (30-3110). Frankfort East (Franklin 

County), Ky. Cuts along eastbound and westbound 

lanes Of Kentucky-U.S. Interstate Highway I-64 east 

of Kentucky River and about 1 mi south of Frankfort. Frankfort East 7.5- minute quadrangle. Lexington· Limestone and Point Pleasant Limestone [Clays 

Ferry Formation]; 80 samples; 26,019 conodont elements. 

30. OSU-64S3 (225-325). Frankfort West (Franklin 

County), Ky. Cuts along eastbound and westbound 

lanes of Kentucky-U.S. Interstate Highway I-64 west 

of Kentucky River and about 1 mi west of 0SU64S2. Frankfort West 7.5- minute quadrangle. Lexing-
G24 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

ton Limestone and Point Pleasant Limestone [Clays 

Fe~ry Formation] ; 31 samples; 11,262 conodont elements. 

31. OSU-65GV (30-1040). New Point (Decatur County); 

Ind. 2.25-in. core drilled by Indiana Geological Survey,· 

beginning on floor of quarry 0.5 mi west of 850 East 

Road and 0.5 mi north of the junction of that road 

and Indiana-U.S. Interstate Highway 1-74, 0.5 mi 

north of New Point. New Point 7 .5-minute quadrangle. Lexington Limestone and "Utica" (of drillers), 

Kope, Dillsboro, and Whitewater Formation; 146 

samples; 19,769 conodont elements. 

32. OSU-66KB (325-531). (Eden locality 13100). Kope 

Hollow (Brown County), Ohio. Natural exposure in 

Kope Hollow, 0.4 mi east of Levanna, on Ohio-U.S. 

Highway 52, Russellville 7.5-minute quadrangle. Type 

section of Kope Formation (Weiss and Sweet, 1964); 

33 samples; 12,715 conodont elements. 

33. OSU-66KD (765-900). Fort Ancient North (Warren 

County), Ohio. Artificial exposure in three cuts along 

abandoned construction road just south of Ohio-u:s. 

Interstate Highway 1-71 on west bank of Little Miami 

River, 1.0 mi north of Fort Ancient, Oregonia 7.5-

minute quadrangle. Base of section about 10 ft above 

base of Orton's (1873) "Lebanon Beds," the type section of which (and of the "Richmond Group") is on 

the opposite bank of the Little Miami River; 35 

samples; 8,501 conodont elements. 

34. OSU-66KE (505-670). Clifton Avenue, Cincinnati 

(Hamilton County), Ohio. Natural exposure along 

east and southeast side of Clifton Avenue, below Bellevue Park, Cincinnati. Covington 7.5-minute quadrangle. Upper part of Kope Formation, Fairview Formation, and lower part of Grant Lake Limestone; 33 

samples; 7,299 conodont elements. 

35. OSU-66KF (655-850), USGS-FRED. Fredericktown 

(Nelson County), Ky. Cut along U.S.-Highway 150, 

7.0 mi east of Bardstown Courthouse, Maud 7.5-minute 

quadrangle. Section begins in Tate Member of Ashlock Formation and extends upward to base of Brassfield Formation (Silurian); 40 samples (OSU-66KF), 

21 samples (USGS-FRED); 2,746 conodont elements 

(0SU-66KF), 1,837 conodont elements (USGS-FRED). 

36. OSU-66KG (615-675). Ashlock Cemetery West (Lincoln County), Ky. Natural exposure along north bank 

of Dix River, beginning 0.8 mi west of U.S. Highway 

27, about 4 mi north of Stanford, Stanford 7.5-minute 

quadrangle. Ashlock Formation; 13 samples; 1,876 

conodont elements. 

37. OSU-66KH (640-765). Ashlock Cemetery (Lincoln 

County), Ky. Cuts along U.S. Highway 27 beginning 

at Dix River beneath bridge just west of mouth of 

Gilberts Creek and about 500 ft southwest of Ashlock 

Cemetery, about 4 mi northeast of Stanford and 1 mi 

west of Gilbert, Lancaster 7.5-minute quadrangle. 

Ashlock Formation; 24 samples; 2,039 conodont elements. 

38. OSU-66KI (760-855). Rowland West (Lincoln County), 

Ky. Cuts along U.S. Highway 27 on outskirts of 

Stanford, about 1.2 mi west of Rowland, Stanford 

7.5-minute quadrangle. Reba Member of Ashlock Formation and Rowland Member of Drakes Formation; 

20 samples; 1,242 conodont elements. 

39. OSU-66KJ (810-895). Preachersville Southeast (Lincoln County), Ky. Natural exposure in gully and cuts 

along Kentucky Route 38 beginning about 2 mi southeast of Preachersville, Lancaster 7.5-minute quadrangle. Preachersville Member of Drakes Formation; 

18 samples; 2,961 conodont elements. 

40. OSU~66KK (630-930). Agawam South (Clark County), 

Ky. Natural exposures and cuts along L. and N. Railroad right-of-way, about 1.5 mi south of Ruckerville 

and about 8 mi southeast of Winchester, Hedges 7.5-

minu.t.e quadrangle. Ashlock and Drakes Formations; 

49 samples; 6,611 conodont elements. 

41. OSU-66KL (755-870). Middletown (Jefferson County), 

Ky. Cuts along Kentucky-U.S. Interstate Highway 

1-64 between a point 5.2 mi east and a point due 

south of Middletown, Fisherville 7.5-minute quadrangle. Drakes Formation; 27 samples; 2,659 conodont 

elements. 

42. OSU-70ZA (0-642). Cominco American Core CA-38. 

BX wireline core drilled 1,900 ft east of Minerva 

(Mason County), Ky. on Tenie W. Richardson farm, 

Germantown 7.5-minute quadrangle. Lexington Limestone, Point Pleasant Limestone [Clays Ferry Formation], Kope, and Fairview Formations; 125 samples; 

44,157 conodont elements. 

43. OSU-73SA (505-625). Type section of Calloway Creek 

Limestone, Madison County, Ky. Cuts along KentuckyU.S. Interstate Highway 1-75, beginning 0.5 mi south 

of bridge over Kentucky River and continuing southward for about 2 mi to a point 0.6 mi north of the 

Kentucky Highway 388 overpass over 1-75, Richmond 

North and Ford 7.5-minute quadrangles. Calloway 

Creek Limestone; 21 samples; 4,376 conodont elements. 

44. USGS-CUZ (185-255). Cuzick (Madison County), Ky. 

Exposure along unnamed stream from point 3,100 ft 

east of Cuzick Church to point 900 ft N. 30° E. of 

Cuzick Church, Valley View 7.5-minute quadrangle. 

Lexington Limestone and Point Pleasant Limestone 

[Clays Ferry Formation]; 12 samples, 802 conodont 

elements. 

45. USGS-DENNY (20-210). A. J. Denny Heirs Diamond 

Core Hole (Jessamine County), Ky. Nicholasville 7.5-

minute quadrangle, north zone, . 1,910,650 ft east, 

151,450 ft north. Lexington Limestone and Point 

Pleasant Lime,stone [Clays Ferry Formation]; 29 

samples; 5,644 conodont elements. 

46. USGS-GA (165-355). Gratz A (Owen ·county), Ky. 

Cuts and natural exposures along Kentucky Route 355, 

1.7 mi east-southeast of Gratz. Gratz 7.5-minute quadrangle. Lexington Limestone and Point Pleasant 

Limes.tone fClays Ferry Formation]; 11 samples; 806 

conodont elements. 

47. USGS-G-A ( ?-?) . Georgetown A (Fayette and Scott 

Counties), Ky. Cuts along Kentucky-U.S. Interstate 

Highway 1-75, 1.4 mi south of Georgetown exit, 

Georgetown, 7.5 minute quadrangle. Lexington Limestone and Point Pleasant Limestone [Clays Ferry Formation]; 9 samoles; 1,446 conodont elements. 

48. USGS-GLENFARM (205-460). Lexington East Core 

Hole 1, Glen Farm. Lexington East 7.5-minute quadrangle, north zone, 1,934,000 ft east, 184,650 ft north. 

Lexington Limestone, Point Pleasant Limestone [Clays 

Ferry Formation] ; 23 samples; 4,624 conodont elements. 
CONODONT BIOSTRATIGRAPHY OF CINCINNATI REGION G25 

49. USGS-CL (78F.-9u8). County Line Section (Mason and 

Lewis Counties), Ky. Cuts along road that roughly 

parallels county line in the northeast corner of the 

Orangeburg 7.5-minute quadrangle and the· southeast 

c<>rner of the Maysville East quadrangle. Bull Fork 

Formation; 20 samples; 1,041 conodont elements. 

50. USGS-SA (155-370). Switzer A (Franklin County), 

Ky. Natural exposures along Kentucky Route 35 (U.S. 

Highway 127), on south side of Elkhorn Creek, Switzer 7.5-minute quadrangle. Lexington . Limestone and 

Point Pleasant Limestone [Clays Ferry Formation] ; 

26 samples; 2,963 conodont elements. _ · 

51. USGS-SH (515-723). Sleepy Hollow (Mason County), 

Ky. Exposures of Kope Formation, Fairview Formation, and Grant Lake Limestone ·in the NW 14 of. the 

Orangeburg 7.5-minute quadrangle and the SW%, of 

the Maysville East quadrangle; 33 samples; 2,290 

conodont elements. 

REFERENCES CITED 

Barnes, C. R., and Fahraeus, L. E., 1975, Provinces, communities, and the proposed nektobenthic habit of Ordovician conodontophorids: Lethaia, v. 8, p. 133-149. 

Barnes, C. R., and Poplawski, M. L. S., 1973, Lower and 

Middle Ordovician conodonts from the Mystic Formation, Quebec, Canada: Jour. Paleontology, v. 46, p. 760-

790, 5 pis. 

Barnes, C. R., Rexroad, C. B., and Miller, J. F., 1973, Lower 

Paleozoic conodont provincialism: Geol. Soc. America 

Spec·. Paper 141, p. 157-190. 

Bergstrom, S. M., 1962, Conodonts from the Ludibundus 

Limestone (Middle Ordovician) of the Tvaren area (S. 

E. Sweden) : Arkiv Mineralogi och Geologi, v. 3, no. 1, 

p. 1-61, 5 pis. 

---1971a, Conodont biostratigraphy of the Middle and 

Upper Ordovician of Europe and eastern North America, in Sweet, W. C., and Bergstrom, S. M., eds. Symposium on conodont biostratigraphy: Geol. Soc. America Mem. 127, p. 83-157, 2 pls. 

---1971b, Correlation of the North Atlantic Middle and 

Upper Ordovician conodont zonation with the graptolite 

succession: [France] Bur. Recherches Geol. et Minieres 

Mem. 73, p. 177-187. 

Bergstrom, S. M., and Sweet, W. C., 1966, Conodonts from 

the Lexington Limestone (Middle Ordovician) of Kentucky and its lateral equivalents in Ohio and Indiana: 

Bulls. Am. Paleontology, v. 50, no. 229, p. 271-441, 8 pls. 

Branson, E. B., and Branson, C. C., 1942, Sequence of Ordovician conodont faunas in Kentucky and adjacent 

states [abs.] : Geol. Soc. America Bull., v. 53, p. 1796. 

Branson, E. B., and Mehl, M. G., 1933, Conodont studies: 

Missouri Univ. Studies, v. 8, p. 1-349, 28 pis. 

Branson, E.B., Mehl, M. G., and Branson, C. C., 1951, Richmond conodonts of Kentucky and Indiana: Jour. Paleontology, v. 25, no. 1, p. 1-17, 4 pls. 

Craig, W. W., 1968, The stratigraphy and conodont paleontology of Ordovician and Silurian strata, Batesville District, Independence and Izard Counties, Arkansas: Austin, Univ. ·Texas, unpub. Ph.D. thesis, 393 p., 23 pls. 

Ethington, R. L., 1959, Conodonts of the Ordovician Galena 

Formation: Jour. Paleontology, v. 33, p. 257-292, 3 pls. 

Ethington, R. L., and Furnish, W. M., 1960, Upper Ordovician conodonts from southern Manitoba: Jour. Paleontology, v. 34, p. 265-274, 1 pl. 

Ethington, R. L., and Schumacher, Dietmar, 1969, Conodonts 

of the Copenhagen Formation (Middle Ordovician) in 

central Nevada: Jour. Paleontology, v. 43, p. 440-484, 

3 pls. 

Foerste, A. F., 1905, The classification of the Ordovician 

rocks of Ohio and Indiana: Science (new ser.), v. 22, 

no. 553, p. 149-152. 

Ford, J. P., 1967, Cincinnatian geology in southwest Hamilton County, Ohio: Am. Assoc. Petroleum Geologists 

Bull., v. 51, no. 6, p. 918-936. 

Grinnell, G. B., 1877, Notice of a new genus of annelids 

from the Lower Silurian: Am. Jour. Science, ser. 3, v. 

14, no. 81, p .. 229.""230,. .. 

Hinde, G. J., 1879, On conodonts from the. Chazy and Cincinnati group of the Cambro-Silurian, and from the 

Hamilton and Genessee-shale divisions of the Devonian, 

in Canada and the United States: Geol. Soc. London 

Quat. Jour. v. 35, p. 351-369, 3 pls. 

James, U. P., 1884, On conodonts and fossil annelid jaws: 

Cincinnati Soc. Nat. History Jour., v. 7, p. 143-149, 1 pl. 

Kohut, J.J., 1969, Determination, statistical analysis, and 

interpretation of recurrent conodont groups in Middle 

and Upper Ordovician strata of the Cincinnati region 

(Ohio, Kentucky, and Indiana): Jour. Paleontology, v. 

43, p. 392-412. 

Kohut, J. J., and Sweet, W. C., 1968, The American Upper 

Ordovician Standard, X, Upper Maysville and Richmond conodonts from the Cincinnati region of Ohio, 

Indiana, and Kentucky: Jour. Paleontology, v. 42, p. 

1456-1477, 2 pls. 

Lindstrom, Maurits, 1971, Lower Ordovician c<>nodonts of 

Europe, in Sweet, W. C., and Bergstrom, S. M., eds., 

Symposium on Conodont biostratigraphy: Geol. Soc. 

America Mem. 127, p. 21-61, 1 pl. 

O'rton, Edward, 1873, Report on the Third geological district 

-geology of the Cincinnati group, Hamilton, Clermont, 

Clarke Counties: Ohio Geol. Survey Rept., v. 1, pt. 1, 

p, 365-480. 

Pander, C. H., 1856, Monographie der fossilen Fische des 

silurischen Systems der russisch-baltischen Gouvernements: St. Petersburg, K. Akad. Wiss., 91 p., 9 pls. 

Pulse, R. R., and Sweet, W. C., 1960, The American Upper 

Ordovician Standard. III. Conodonts from the Fairview 

and McMillan Formations of Ohio, Kentucky, and Indiana: Jour. Paleontology, v. 34, 237-264, 3 pis. 

Rhodes, F. H. T., 1953, Some British lower Paleozoic conodont faunas: Roval Soc. fLondon 1 Philos. Trans., ser. 

B, no. 647, v. 237, p. 239-264~. 3 pls. 

Roscoe, M. S., 1973, Conodont biostratigraphy and facies relationships of the lower Middle Orddvician strata in the 

upper Lake Champlain valley: Ohio State Univ. M. S., 

thesis, i-viii, 125 p., 3 pls. 

Seddon, George, and Sweet, W. C., 1971, An ecolog-ic model 

for conodonts: Jour. Paleontology, v. 45, p. 869-880. 

Stauffer, C. R., 1930, Conodonts from the Decorah Shale: 

Jour. Paleontology, v. 4, p. 121-128, 1 pl. 

---1935a, Conodonts of the Glenwood beds: Geol. Soc. 

America Bull., v. 46, p. 125-168, 4 pls. 

---1935b, The conodont fauna of the Decorah Shale (Ordovician): Jour. Paleontology, v. 9, p. 596-620, 5 pls. 
G26 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

---1940, Conodonts from the Devonian and associated 

clays of Minnesota: Jour. Paleontology, v. 14, p. 417-

435, 3 pls. 

Stone, G. L., and Furnish, W. M., 1959, Bighorn conodonts 

from Wyoming: Jour. Paleontology, v. 33, p. 211-228, 

2 pls. 

Sweet, W. C., and Bergstrom, S. M., 1970, The generic concept in conodont taxonomy: North Am. Paleont. Convention, Sept. 1969, Proc., pt. C, p. 157-173. 

---1971, The American Upper Ordovician Standard, XIII, 

A revised time-stratigraphic classification of North 

American upper Middle and Upper Ordovician rocks: 

Geol. Soc. America Bull., v. 82, p. 613-628. 

---1972, Multielement taxonomy and Ordovician cono-. 

donts: Geologica et Paleontologica Sonderland 1, p. 

29-42. 

Sweet, W. C., Bergstrom, S. M., and Rust, C. C., 1965, Relative abundance analysis-an aid to Ordovician conodont 

biostratigraphy in the Cincinnati region of Ohio [abs.j: 

Geol. Soc. America Spec. Paper 82, p. 203. 

Sweet, W. C., Ethington, R. L., and Barnes, C. R., 1971 

North American Middle and Upper Ordovician conodont 

faunas, in Sweet, W. C., and Bergstrom, S. M., eds. 

Symposium on conodont biostratigraphy: Geol. Soc. 

America Mem. 127, p. 163-193, 2 pls. 

Sweet, W. C., Harper, H., Jr., and Zlatkin, Dennis, 1974, 

~he American Upper Ordovician Standard, XIX, A Middle and Upper Ordovician Standard for the Eastern Cincinnati region: Ohio Jour. Sci., v. 74, p. 47-54. 

Sweet, W. C., and Schonlaub, H. P., 1975, Conoqonts of the 

genus Oulodus Branson & Mehl, 1933; Geologica et 

Palaeontogica, 9, p. 41-54, 1 fig., 2 pls. 

Sweet, W. C., Thompson, T. L., and Satterfield, I. R., 1975, 

Conodont stratigraphy of the Cape Limestone (Maysvillian) of eastern Missouri: Missouri Geol. Survey 

Rept. Inv. 57, pt. 1, p. 1-60, 3 pls. 

Sweet, W. C., Turco, C. A., Warner, Earl, and Wilkie, L. G., 

1959, The American Upper Ordovician Standard, I, Eden 

conodonts from the Cincinnati region of Ohio and Kentucky: Jour. Paleontology, v. 33, p. 1029-1068, 4 pls. 

Ulrich, E. 0., 1878, Observations of fossil annelids and descriptions of some new forms: Cincinnati Soc. Nat. 

History Jour., v. 1, p. 87-91, 1 pl. 

Weiss, M. P., and Sweet, W. C., 1964,.' Kope Formation 

(Upper Ordovician), Ohio and Kentucky: Science, v. 145, 

p. 1296-1302. 

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