Middle and Late Ordovician 

Solitary Rugose Corals of the 

Cincinnati Arch Region 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-N 

Prepared £n cooperatz'on wz'th the 

Commonwealth of Kentucky, 

University of Kentucky, 

Kentucky Geological Survey 
Middle and Late Ordovician 

Solitary Rugose Corals of the 

Cincinnati Arch Region 

By ROBERT J. ELIAS 

CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF 

KENTUCKY AND NEARBY STATES 

Edited by JOHN POJETA, JR. 

GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066-N 

Prepared in cooperatz"on with the 

Commonwealth of Kentucky, 

University of Kentucky, 

Kentucky Geological Survey 

Taxonomy, paleoecology, and 

paleobiogeography of four species 

ranging in age from Kirkfieldian 

to Richmondian 

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON: 1983 
UNITED STATES DEPARTMENT OF THE INTERIOR 

JAMES G. WATT, Secretary 

GEOLOGICAL SURVEY 

Dallas L. Peck, Director 

Elias, Robert J. 

Middle and Late Ordovician solitary rugose corals of the Cincinnati Arch region. 

(Contributions to the Ordovician paleontology of Kentucky and nearby states) (Geological Survey professional paper ; 1066-N) 

"Prepared in cooperation with the Commonwealth of Kentucky, University of Kentucky, Kentucky Geological Survey." 

Supt. of Docs. no.: I 19.16:1066-N 

1. Rugosa. 2. Paleontology-Ordovician. 3. Paleontology-Kentucky. 

I. Kentucky Geological Survey. II. Title. III. Series. IV. Series: Geological Survey professional paper ; 1066-N. 

QE778.E643 1983 563 '.6 83-600180 

For sale by the Distribution Branch, U.S. Geological Survey, 

604 South Pickett Street, Alexandria, VA 22304 
CONTENTS 

Page 

Abstract--------------------------------------------------------------------- N1 

Introduction------------------------------------------------------------------ 1 

Acknowledgments---------------------------------------------------------- 1 

Middle Ordovician solitary Rugosa ----------------------------------------------- 2 

Late Ordovician solitary Rugosa ------------------------------------------------- 2 

Paleoecology -------------------------------------------------------------- 2 

Geographic variation ------------------------------------------------------- 3 

Stratigraphic variation--------------..:--------------------------------------- 5 

Paleobiogeography --------------------------------------------------------- 6 

Description of solitary Rugosa --------------------------------------------------- 7 

Larnbeophyllurn?sp.A ------------------------------------------------------ 7 

Larnbeophyllurn? sp. B ------------------------------------------------------ 7 

Grewingkia canadensis (Billings, 1862) ----------------------------------------- 8 

Streptelasrna divaricans (Nicholson, 1875b)-------------------------------------- 9 

Locality register -------------------------------------------------------------- 10 

References cited--------------------------------------------------------------- 11 

ILLUSTRATIONS 

PLATE 1. Larnbeophyllurn? sp. A and sp. B. 

2. Grewingkia canadensis and Streptelasrna divaricans. 

Page 

FIGURE 1. Index map and Richmondian stratigraphic sections ------------------------------------------------------------ N4 

2-5. Graphs showing: 

2. Length-frequency distributions for Grewingkia canadensis---------------------------------------------------- 5 

3. Relation between number of septa and coral diameter for Grewingkia canadensis---------------------------------- 5 

4. Axial region variability in Grewingkia canadensis and Streptelasrna divaricans----------------------------------- 6 

5. Relation between number of septa and coral diameter for Larnbeophyllurn? sp. A ---------------------------------- 7 

m 
CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

MIDDLE AND LATE ORDOVICIAN SOLITARY RUGOSE CORALS 

OF THE CINCINNATI ARCH REGION 

By ROBERT J. ELIAS1 

ABSTRACT 

Middle Ordovician (Kirkfieldian) solitary rugose corals have been 

reported from the Tyrone Limestone of the High Bridge Group and 

the Curdsville Limestone Member of the Lexington Limestone in 

central Kentucky. Lambeophyllum? spp. A and Bare recognized in 

the Tyrone Limestone. 

Grewingkia canadensis (Billings, 1862) and Streptelasma 

divaricans (Nicholson, 1875b) are the only solitary Rugosa known 

from the Upper Ordovician in the Cincinnati Arch region of KentuckyIndiana-Ohio. Their earliest occurrence suggests introduction during 

an early Richmondian transgression. The two species have similar 

distributions; they favored normal marine waters of intermediate 

depth where calcium carbonate sediments accumulated and brachiopods and bryozoans thrived. G. canadensis probably lived in stable, 

low-energy environments, but the corals were transported during 

higher energy conditions before final deposition and rapid burial. 

S. divaricans was epifaunal on stabilized carbonate substrates during 

periods of nondeposition. Energy conditions -remained low, and subsequent, usually argillaceous sediments often buried these corals in 

growth position. 

G. canadensis and S. divaricans attained their greatest diameter 

and length, respectively, on the southwestern side of the Cincinnati 

Arch region. The average number of septa in G. canadensis generally 

increased during Richmondian time, and simpler axial regions 

became more predominant in both species. These trends may be 

related to decreasing water depth. G. canadensis and S. divaricans 

are confined to the Richmond Solitary Coral Province, which formed 

a narrow belt extending from the Nashville Dome, along the Cincinnati Arch region to northern Michigan, and through southern Ontario 

and Quebec. The Red River-Stony Mountain Solitary Coral Province 

occupied the remainder of North America during the Richmondian. 

Because the taxa in these provinces are different, solitary corals cannot now be used to correlate strata outside the geographically restricted Richmond Province with the North American Upper Ordovician type sections in the Cincinnati Arch region. G. canadensis and 

S. divaricans became extinct during regression of the epicontinental 

sea at the end of Richmondian time. 

•University of Manitoba, Winnipeg, Manitoba, R3T 2N2, Canada. 

INTRODU~TION 

Ordovician strata exposed in the Cincinnati Arch 

region of Kentucky-Indiana-Ohio range from Middle 

Ordovician (probably Blackriveran) through Late 

Ordovician (Richmondian) in age (Pojeta, 1979). Solitary 

rugose corals are known from the Middle Ordovician 

(Kirkfieldian) Tyrone Limestone and Curdsville Limestone Member, Lexington Limestone, in Kentucky, 

and from the Upper Ordovician Richmondian Stage in 

Kentucky, Indiana, and Ohio. Two species from the 

Tyrone Limestone and two from the Richmondian Stage 

are described in this paper. A comprehensive study of 

the Richmondian solitary Rugosa was presented in 

Elias (1982). 

Abbreviations used herein are: AMNH (American 

Museum of Natural History), FMNH UC (Field Museum of Natural History), GSC (Geological Survey of 

Canada), USNM (National Museum of Nat ural History), 

USGS (U.S. Geological Survey), and UCGM (University 

of Cincinnati Geological Museum). 

ACKNOWLEDGMENTS 

The portion of this paper dealing with Late Ordovician corals is based on part of a doctoral dissertation 

supervised by Kenneth E. Caster, David L. Meyer, and 

Paul Edwin Potter of the University of Cincinnati, to 

whom my sincere thanks are extended. That study was 

supported by Geological Society of America, Research 

Grant (1977); Sigma Xi, Grant-in-Aid of Research 

(1977); U.S. National Academy of Sciences, Bache Fund 

Grant (1977); University .of Cincinnati, Summer Research Fellowships (1977, 1978); University of Cincinnati, Department of Geology, Travel and Research 

N1 
N2 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

Funds (1977, 1978). Subsequent research was funded 

by the Natural Sciences and Engineering Research 

Council of Canada (1980, 1981). 

Thin sections were prepared by Per-Erik Litz (University of Cincinnati). I am grateful toR. C. Kepferle, 

W. L. Peterson, John Pojeta, Jr., and W C Swadley 

(USGS) for providing information on stratigraphic sections in Kentucky. F. J. Collier and W. A. Oliver, Jr., 

provided specimens on loan from USNM and USGS collections in Washington, D.C. I thank W. A. Oliver, Jr., 

John Pojeta, Jr., and E. R. Cressman (USGS) and M. C. 

N oger (Kentucky Geological Survey) for reviewing this 

manuscript. 

MIDDLE ORDOVICIAN SOLITARY RUGOSA 

Solitary corals have been reported from the Middle 

Ordovician Tyrone Limestone and Curdsville Limestone Member, Lexington Limestone, in the Cincinnati 

Arch region of central Kentucky. The Tyrone is the 

uppermost unit in the High Bridge Group; it consists of 

calcilutite and some dolomite. The sedimentary structures suggest deposition on tidal flats and in shallow 

lagoons (Pojeta, 1979, p. 9, 13). Bassler (1950, p. 13, 14) 

listed Lambeophyllum profundum (Conrad, 1843) and 

Streptelasma parasiticum Ulrich in Winchell and 

Schuchert, 1895, from the Tyrone. The High Bridge 

Group is locally overlain disconformably by the Curdsville Limestone Member of the Lexington Limestone. 

This member consists primarily of bioclastic 

calcarenite and calcirudite and was deposited during a 

marine transgression (Pojeta, 1979, p. 10). Bassler 

(1950, p. 16) listed Lambeophyllum profundum and 

Streptelasma corniculum Hall, 184 7, from the Curdsville. No solitary Rugosa from the Curdsville were 

available for this study. Both the Tyrone and the Curdsville are placed i~ the Kirkfieldian Stage of the Champlainian Provincial Series (Pojeta, 1979, p. 15). 

In this study, approximately 200 silicified solitary 

corals were examined from USGS locality 6034-CO at 

the top of the Little Hickman A Section (see Locality 

Register). They are from a 0.6- to 1.0-m-thick calcarenite 

bed about 8 m below the Pencil Cave bentonite of drillers, which is about 7 m below the top of the Tyrone 

Limestone. Two species are recognized, and they are 

referred to as Lambeophyllum? spp. A and B. The latter 

is represented by only 1 percent of the specimens. Both 

species have deep calices and septa with denticulate 

edges that do not twist axially, and both species lack 

tabulae. Middle Ordovician solitary corals with these 

characteristics have generally been assigned to 

Lambeophyllum Okulitch, 1938, but this genus and its 

species are poorly known (Weyer, 1973, p. 34, 35). Definite generic and specific assignments for the taxa described herein, an evaluation of species previously 

reported from the Tyrone and the Curdsville, and stabilization of Middle Ordovician solitary coral taxonomy 

in general will be possible only upon completion of a 

comprehensive study of these Rugosa in eastern North 

America. 

LATE ORDOVICIAN SOLITARY RUGOSA 

Solitary rugose corals have not been found in the 

Edenian and Maysvillian Stages of the Cincinnatian 

Provincial Series (Upper Ordovician) in the Cincinnati 

Arch region of Kentucky-Indiana-Ohio. Two species, 

Grewingkia canadensis (Billings, 1862) and Streptelasma divaricans (Nicholson, 1875b), are known from 

the Richmondian Stage. I examined 32 stratigraphic 

sections during the summers of 1977 and 1978 in order 

to prepare composite sections through the Richmondian 

sequence at 14 locations around the region (fig. 1). 

Almost 800 specimens of solitary corals, most of them 

calcareous, were collected and placed in the UCGM. I 

also examined additional material in collections of the 

USNM and the FMNH UC. The modern lithostratigraphic units referred to in this study were defined by 

several workers over the last two decades and were 

described by Pojeta (1979), who referred to the original 

authors, and by Elias (1982). In order to consider corals 

from the entire Cincinnati Arch region in a temporal 

framework, I have also used the traditional formation 

names. These names have commonly been used in the 

sense of time-stratigraphic subdivisions of the Richmondian Stage (fig. 1). Because these are not formal 

units, they are here placed in quotation marks. 

PALEOECOLOGY 

Grewingkia canadensis and Streptelasma divaricans 

have similar stratigraphic and geographic distributions 

(fig. 1); they are generally found in fossiliferous limestone beds containing abundant brachiopods and bryozoans. G. canadensis is more abundant than S. divaricans. That the earliest occurrence ·of Late Ordovician 

solitary corals is in basal HWaynesville" -age strata at 

locations 1a (Bull Fork Formation), 2 (Rowland Member, Drakes Formation), and 11 b (Dillsboro Formation) 

suggests that they were introduced during an early 

Richmondian transgression (Hay, 1977, fig. 1-4). This 

initial distribution about halfway between the deeper 

northern and shallower, periodically subaerially exposed, southern ends of the region indicates preference 

for normal marine water in the intermediate depth 

range where calcium carbonate sediments accumulated 
MIDDLE AND LATE ORDOVICIAN SOLITARY RUGOSE CORALS OF CINCINNATI ARCH REGION N3 

and brachiopods and bryozoans thrived. The two species 

dispersed northward and southward as favorable environmental conditions appeared elsewhere, and they 

were distributed throughout the Cincinnati Arch region 

during ccLiberty-early Whitewater" time. They did not 

live in the restricted Saluda lagoon (Hatfield, 1968) or 

in very shallow environments associated with the regression at the end of Richmondian time. 

Grewingkia canadensis.-Unattached solitary Rugosa 

having slightly curved to straight and cylindrical external form such as G. canadensis are thought to have 

inhabited low-energy, stable environments in which 

the corals slowly sank vertically into the sediment 

because of added weight during growth (Wells, 1957). 

However, virtually all specimens of this species were 

lying on their sides when buried within and on limestone beds. Of 143 specimens, 76 percent were oriented 

in the most stable position with an alar side facing up 

(that is, having plane of curvature and bilateral symmetry horizontal), and only 15 percent and 9 percent 

were oriented with the concave counter and convex cardinal sides up, respectively. Almost all the corals show 

evidence of preburial abrasion, and the calice rims of 

some were broken. Directional orientation measurements of specimens on bedding surfaces suggest alinement due to predominant currents from the south and 

west. These observations indicate that corals of this 

species were overturned and transported during higher 

energy conditions before final deposition. 

The length-frequency distribution for specimens of 

G. canadensis in the Cincinnati Arch region is bimodal, 

having peaks at 22.5 and 57.5 mm. This general distribution is independent of stratigraphic position and geographic location; it is also found at Drummond Island, 

Mich. (fig. 2B). The low-frequency area between these 

peaks may be due to current sorting that removed 

some corals between about 20 and 60 mm long, and 

especially those about 35 mm long. Changes in external 

form and degree of septal dilation during ontogeny 

determined shape, surface area, and weight, which 

would have affected the behavior of different-sized 

corals in a particular current. Unimodal distributions 

corresponding to this low-frequency area occur in the 

Goodlettsville-Gallatin area of Tennessee and on Manitoulin Island, Ontario, which were near-shore zones at 

extremities of the geographic range of G. canadensis 

(fig. 2A). Corals removed from initial populations may 

have been transported to locations such as these. The 

stereozones of several specimens at Gallatin, Tenn., 

were completely stripped by abrasion before deposition, 

indicating extensive transportation. If the corals removed by currents could be added to those left behind, 

it would be possible to reconstruct the initial lengthfrequency distribution for G. canadensis. Combining 

figures 2A and B suggests that the population may 

have followed the solid curve in figure 2B. Such a distribution resembles those of the other Late Ordovician 

species for which data have been collected-all are unimodal and positively skewed (Elias, 1982, 1983). 

Probable polychaete annelid borings, assigned to 

Trypanites weisei Magdefrau, 1932 (Elias, 1980), are 

present in 38 percent of 466 G. canadensis specimens 

from the Cincinnati Arch region (pl. 2, fig. 5; Cameron, 

1969, fig. 4g). They are located predominantly in the 

counter side of the hosts. If all borings were produced 

after deposition of the corals, most would be expected 

in an alar side, which usually faced upward. Epizoic 

bryozoans were observed on 54 percent of 529 G. canadensis specimens. They are found in approximately 

equal numbers on the upper exposed and the lower 

buried sides of corals preserved on bedding surfaces. 

The distribution of borings and epizoans suggests that 

organisms usually became associated with host corals 

before final deposition and that burial was generally 

rapid, allowing little or no time for colonization of the 

exposed surface. 

Streptelasma divaricans.-Whereas· corals assigned 

to G. canadensis formed a transported constituent 

within and on carbonate beds, S. divaricans was epifaunal on stabilized carbonate substrates during periods 

of nondeposition. This species was commonly attached 

to elevated areas especially on bryozoans (pl. 2, figs. 16, 

17, 20, 21, 30) but also on brachiopods (pl. 2, figs. 31, 

32) and on solitary or colonial corals. The larvae frequently attached to living hosts, as demonstrated by 

upward growth of bryozoans around the corals (pl. 2, 

fig. 30) and by their orientation on brachiopods (Richards, 1972, p. 401, fig. 10). At location 4 (Bardstown 

Member, Drakes Formation), these solitary corals 

occur on the tops of globular colonial corals. Pseudocolonies of S. divaricans (pl. 2, figs. 20, 30-33) probably 

resulted from selection of a favorable attachment site 

by more than one larva. Many corals were buried in 

growth position by subsequent, generally argillaceous 

sediments deposited in low-energy conditions (pl. 2, fig. 

33). The length-frequency histogram of corals is positively skewed and has a mode at 10 mm. 

Trypanites weisei borings and epizoic organisms are 

rare on S. divaricans, probably because of the small 

size of individuals in this species. Also, the corals attached to bryozoans were frequently surrounded and 

protected by the host. 

GEOGRAPHIC VARIATION 

The diameter of Grewingkia canadensis specimens in 

late ontogenetic stages is almost always greater in the 

Bardstown and Saluda Dolomite Members of the 
N4 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

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FIGURE 1.-Index map and Richmondian stratigraphic sections. 

Shows 32 exposures (see Locality Register) used to prepare composite sections through the Richmondian sequence at 14 locations 

around the Cincinnati Arch region. Stratigraphic sections in six 

geographic areas (drawn to scale shown in upper left) summarize 

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Grewingkia canadensis and Streptelasma divaricans (on right side 

of columns). Section on east side of region has not been subdivided 

into informal time-stratigraphic units. 
MIDDLE AND LATE ORDOVICIAN SOLITARY RUGOSE CORALS OF CINCINNATI ARCH REGION N5 

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FIGURE 2.-Length-frequency distributions for all specimens in this 

study of Grewingkia canadensis. Percent frequency refers to percent 

of total sample (n) having a particular length. A, GoodlettsvilleGallatin area, Tennessee, and Manitoulin Island, Ontario. B, Cincinnati Arch region, Kentucky-Indiana-Ohio, and Drummond 

Island, Mich. Dotted line connects data points. Solid line with 

arrow is postulated curve of original population before modification 

by current movement. 

Drakes Formation at locations 2, 3, and 4 than elsewhere in the Cincinnati Arch region (compare pl. 2, fig. 

5 with figs. 1,. 9, 13). The longest specimens of Streptelasma divaricans occur in the Bardstown Member of 

the Drakes Formation at location 4. 

Microscopic algal borings of the type that have been 

described from Richmondian brachiopod shells in Ohio 

(Kobluk and Risk, 1977) are very common in the outer 

wall of solitary corals. They are present in 53 of 57 

G. canadensis specimens for which thin sections were 

examined. The only locations at which not all specimens 

have borings are 5, 12, and 13. The borings attain maximum diameters and lengths in the Bardstown and 

Saluda Dolomite Members of the Drakes Formation at 

location 4 and are finer and very short in the Dillsboro 

and Whitewater Formations at locations 12, 13, and 

14. These borings are present in 32 of 45 S. divaricans 

specimens. The specimens without borings are not 

restricted to the northern part of the region, as are the 

unbored G. canadensis specimens, but the borings are 

best developed south of locations 12; 13, and 14. 

On the southwestern side of the Cincinnati Arch 

region, algal borings were best developed, colonial 

coral biostromes were most prominent (Browne, 1964, 

p. 389), and G. canadensis and S. divaricans attained 

their greatest diameter and length, respectively. This 

shallow, open shelf edge of the Richmondian carbonate 

platform seems to have been an area of high productivity that was especially favorable for corals. 

STRATIGRAPHIC VARIATION 

A general increase throughout ontogeny occurs in 

the number of major septa in Grewingkia canadensis in 

the Cincinnati Arch region, as can be seen by comparing 

values for specimens from uwaynesville" -, ULiberty" -, 

and uWhitewater-Elkhorn" -age strata (fig. 3). At location 1, however, values through the entire Richmondian 

sequence (Bull Fork and Drakes Formations) resemble 

those for ccLiberty"-age strata elsewhere. This is the 

only area in the Cincinnati Arch region where there 

are no major lithologic changes, although there is an 

upward increase in shale probably related to progradation of the Queenston delta from the east. Environmental conditions apparently remained uniform during 

Richmondian time in the vicinity of location 1.. The 

increase in number of septa that occurred elsewhere 

may have been a result of environmental change. Perhaps it was related to a decrease in water depth, as suggested by regressive uLiberty"- and ccWhitewaterElkhorn" -age sequences (Hay, 1977, fig. 1-4). Changes 

in the number of septa are not apparent in Streptelasma divaricans. 

Axial-region complexity in the late ontogenetic stage 

varies considerably within G. canadensis and S. divaricans. In both species, there was a trend through time 

toward predominantly simpler axial regions, although 

the total range of variability remained approximately 

constant during the Richmondian (fig. 4). This trend 

may also be related to decreasing water depth. Too few 

data are available to determine whether or not a change 

occurred at location 1. 

EXPLANATION 

• "WHITEWATER-ELKHORN" (based on 172 sections from 97 corals) 

!:::. "LIBERTY" (based on 109 sections from 58 corals) 

0 "WAYNESVILLE" (based on 63 sections from 35 corals) 

FIGURE 3.-Relation between number of major septa and coral 

diameter for Grewingkia canadensis from three intervals in the 

Richmondian sequence, Cincinnati Arch region, Kentucky-IndianaOhio. Each symbol represents the average number of septa at a 

particular diameter. 
N6 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

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FIGURE 4.-Frequency of corals within the range of late ontogenetic 

axial·region variability, for intervals in the Richmondian sequence, 

Cincinnati Arch region, Kentucky-Indiana-Ohio. A, Grewingkia 

canadensis. B, Streptelasma divaricans. The method used to plot 

these distributions is presented in Elias (1982, p. 22, 26). n, number 

of samples. 

PALEOBIOGEOGRAPHY 

Grewingkia canadensis and Streptelasma divaricans 

are confined to the Richmond Solitary Coral Province, 

which occupied a narrow belt extending northward 

from the Nashville Dome of Tennessee along the Cin-

· cinnati Arch region of Kentucky-Indiana-Ohio to 

northern Michigan and then eastward through southern Ontario and Quebec (Elias, ~982). It coincided with 

a carbonate platform at the margin of an epicontinental 

sea that was receiving clastic sediments from the 

Queenston delta to the east (Ontario, New York, Pennsylvania, Ohio). 

Solitary Rugosa were apparently reintroduced to this 

geographic region during an early Richmondian transgression and probably arrived from the west. Forms in 

the HTrentonian" -lower Cincinnatian of Minnesota, 

described as S. corniculum and S. rusticum in Winchell 

and Schuchert (1895, p. 90, 91, 93; pl. G, figs. 20-23), 

resemble G. canadensis externally. The HTrentonian" 

S. (?) parasiticum Ulrich in Winchell and Schuchert, 

1895 (p. 89, 90, fig. 6), is remarkably similar in growth 

form to S. divaricans. 

Following introduction to the carbonate platform, solitary corals dispersed latenilly as favorable environments 

became more widespread. They attained a maximum 

geographic range during HLiberty-early Whitewater" 

time. Dispersal out of and into the Richmond Solitary 

Coral Province was restricted shoreward by the Queenston delta and Taconic upland and by the positive 

Canadian Shield. Seaward of the platform, a deeper 

water zone in which the Maquoketa Shale was deposited proved to be a barrier. Withdrawal of the epicontinental sea from eastern North America at the end of 

Richmondian time, possibly due to a glacioeustatic sealevel drop (Berry and Boucot, 1973; Dennison, 1976), 

resulted in extinction of the Richmond Province solitary 

corals. 

Biostratigraphic implications.-During Richmondian 

time, the Red River-Stony Mountain Solitary Coral 

Province occupied all of North America outside the 

boundaries of the Richmond Province. The Red RiverStony Mountain assemblage is characterized by taxa 

having unusual external form (Elias, 1981, 1982, 

1983). Grewingkia includes species that are triangulate 

and trilobate in cross section. Deiracorallium and 

Lobocorallium are compressed and trilobate, respectively. Bighornia is distinct in having its cardinal septum on the concave side of a depressed corallum. Biostratigraphic correlation between the Richmond and 

Red River-Stony Mountain Solitary Coral Provinces is 

not possible because the solitary coral species and 

assemblages are different. Consequently, strata outside 

the geographically restricted Richmond Province cannot be correlated at present, by means of this group of 

fossils, with the North American Upper Ordovician 

type sections in the Cincinnati Arch region. The absence ~f Edenian and Maysvillian solitary Rugosa in 

the type area adds to the biostratigraphic problem. 
MIDDLE AND LATE ORDOVICIAN SOLITARY RUGOSE CORALS OF CINCINNATI ARCH REGION N7 

DESCRIPTION OF SOLITARY RUGOSA 

Lambeophyllum? sp. A 

Plate 1, figures 1-10 

Figured specimens.-USNM 334851-334856, about 

8 m below Pencil Cave bentonite of drillers, which is 

about 7 m below the top of Tyrone Limestone, High 

Bridge Group, USGS locality 6034-CO, Jessamine 

County, Ky. 

Additional material.-Approximately 200 specimens 

in USGS collection 6034-CO, same horizon and locality 

as above. 

Occurrence.-Middle Ordovician (Kirkfieldian), Tyrone Limestone, High Bridge Group, Jessamine 

County, Ky. 

Description.-The maximum observed length and 

diameter are 26 mm and 19 mm, respectively. The 

corals are trochoid and conical (pl. 1, figs. 1, 4, 6, 9). 

Two specimens consist of a pair of coralla joined laterally. It is not known if these represent colonies or pseudocolonies. A small, flattened attachment area was 

observed on the cardinal side at the tip of one specimen 

(pl. 1, fig. 9). Depth of the calice in 34 specimens varies 

between 33 and 58 percent ofthe coral length and averages 4 7 percent. The septa are acanthine, having denticulate edges (pl. 1, figs. 2, 3, 5, 7, 8, 10). The number 

of major septa is shown in figure 5. The major septa are 

greatly to completely dilated until immediately below 

the base of the calice, where they generally become 

thinner. They extend to the axis without twisting. Cardinal and alar fossulae are prominent. The cardinal 

septum is thinner and shorter than the other major 

septa, which form a calicular boss. All major septa are 

• 35 • •2 • • 

<t: • • 

I- • •2 a.. n=59 • UJ 

(/) 30 • • • 0:: • • • • • 

0 • e2 

-, • 

<t: •2 • ~ 25 • • • •2 • ·2. u.. • •2. 0 • •3 

ffi 20 

•2. 

• •2 • cc • 3. 

~ • 

:::> • z 15 • 

• 

0 5 10 15 

DIAMETER (mm) 

FIGURE 5.-Relation between number of major septa and coral 

diameter for Lambeophyllum? sp. A. 

short along the sides of the calice from its base to the 

top of the coral. The minor septa are very short. Tabulae 

are absent. 

Discussion.-This species is the predominant solitary 

coral in USGS collection 6034-CO. It is represented by 

all but two of approximately 200 specimens examined. 

Lambeophyllum? sp. A differs from L.? sp. Bin being 

conical, having a shallower calice with a calicular boss, 

and having prominent cardinal and alar fossulae. The 

septal arrangement and fossulae of L.? sp. A resemble 

Lambelasma lambei Weyer, 1973, from the upper Middle Ordovician of Baltoscandia, but a calicular boss is 

not developed in that species and the major septa 

shorten gradually from the base of calice to the top of 

the coral. North American Middle Ordovician solitary 

Rugosa having a coral form and septal arrangement of 

the type seen in Lambeophyllum? sp. A have all been 

assigned to Lambeophyllum profundum (Conrad, 1843) 

by previous workers. However, the presence of a calicular boss has not been reported in the latter species, and 

A. E. Wilson (1948, p. 32) described the calice as 

funnel-shaped. 

Lambeophyllum? sp. B 

Plate 1, figures 11-13 

Figured and only specimens.-USNM 334857,334858, 

about 8 m below Pencil Cave bentonite of drillers, which 

is about 7 m below the top of Tyrone Limestone, High 

Bridge Group, USGS locality 6034-CO, Jessamine 

County, Ky. 

Occurrence.-Middle Ordovician (Kirkfieldian), Tyrone Limestone, High Bridge Group, Jessamine County, 

Ky. 

Description.-USNM 334857 is 13 mm long and has a 

maximum diameter of 9 mm. USNM 334858 has a 

length of 4 mm and is 3 mm in diameter. The corals are 

trochoid and, in early ontogenetic stages, strongly 

curved (pl. 1, fig. 11). The calice is very deep, extending 

to within 1 mm of the tip in USNM 334858 (pl. 1, fig. 13) . 

Its base cannot be seen in USNM 334857, indicating 

that the calice extends to within several millimeters of 

the tip (pl. 1, fig. 12). The septa are acanthine, having 

denticulate edges. The major septa are short. Twentythree are present at the top ofUSNM 334857. The cardinal septum is located on the concave side of the coral. 

In USNM 334858, the cardinal and alar septa appear 

to be prominent at the base of the calice. The minor 

septa are extremely short. Tabulae are absent. 

Discussion.-This species is rare in USGS collection 

6034-CO. It is represented by only 2 of approximately 

200 solitary corals examined. Lambeophyllum? sp. B 

differs from L.? sp. A in being strongly curved apically 
N8 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

and having a much deeper calice. In Primitophyllum 

primum Kaljo, 1956, from the Middle Ordovician of 

Estonia, the calice extends to the apex of the coral and 

the acanthine septa are discontinuous, resulting in 

septal combs. Although the major septa in L.? sp. Bare 

very short, they are continuous. This species resembles 

Lambelasma lambei Weyer, 1973, from the upper Middle Ordovician of Baltoscandia in having the cardinal 

septum on the concave side of an apically curved coral, 

but Lambeophyllum? sp. B has a much deeper calice 

and shorter major septa. North American Middle Ordovician corals assigned to Lambeophyllum profundum 

(Conrad, 1843) have generally been described as conical 

or very slightly curved (Okulitch, 1938, p. 101; Stumm, 

1963, p. 24, 25), and the cardinal septum has not been 

reported on the concave side. However, apically curved 

specimens have been found in Wisconsin (Winchell and 

Schuchert, 1895, p. 88, pl. G, fig. 18). L.? sp. B is definitely not conspecific with the specimens of L. profundum figured by Stumm (1963, pl. 1, figs. 17, 18, 24-26), 

which have a much shallower calice and longer major 

septa. 

Grewingkia canadensis (Billings, 1862) 

Plate 2, figures 1-15 

Streptelasma corniculum Hall. Milne-Edwards and Haime, 1851, 

p. 398, 399 [partim], pl. 7, fig. 4, 4a, 4b. 

Zaphrentis canadensis Billings, 1862, p. 105, 106, fig. 93a-c. 

Petraia canadensis (Billings). Geological Survey of Canada, 1863, 

fig. 205. 

Streptelasma corniculum Hall. Nicholson, 1875a, p. 26, 27 [partim]. 

Streptelasma corniculum Hall. Nicholson, 1875b, p. 218, 219 [partim]. 

Streptelasma corniculum Hall. Nicholson, 1876, p. 94, pl. 5, fig. 15, 

15a. 

Streptelasma corniculum Hall. Rominger, 1876, p. 142, 143 [partim], 

pl. 51, upper tier [partim]. 

Streptelasma corniculum Hall. White, 1882, p. 376 [partim], pl. 51, 

figs. 2-4. 

Streptelasma rusticum (Billings). Lambe, 1901, p. 110-

112 [partim], non pl. 7, figs. 2, 2a, 3. 

Streptelasma rusticum (Billings). Cumings, 1908, p. 708, 709 [partim], 

pl. 2, fig. 2, 2a, 2b. 

Streptelasma vagans Foerste, 1909, p. 305, 306, pl. 11, fig. la-c. 

Streptelasma insolitum Foerste, 1909, p. 306, pl. 10, fig. 3. 

Streptelasma dispandum Foerste, 1909, p. 307, pl. 9, fig. 4a, 4b. 

Streptelasma rusticum (Billings). Foerste, 1924, p. 65, 66 [partim], 

pl. 1, figs. la-c, 2a-c, pl. 2, fig. 6a-c. 

Streptelasma dispandum Foerste. Foerste, 1924, p. 66, 67, pl. 2, fig. 4. 

Streptelasma rusticum (Billings). Bassler, 1932, pl. 24, figs. 16, 17. 

Streptelasma rusticum (Billings). Cox, 1937, p. 11-13 [partim], pl. 2, 

figs. 11, 12a-c, 13a-d. 

Streptelasma rusticum (Billings). C. W. Wilson, 1948, pl. 19, figs. 26, 

27. 

Streptelasma rusticum (Billings). C. W. Wilson, 1949, pl. 19, figs. 26, 

27. 

Streptelasma sp. Hill, 1961, pl. 1, figs 7, 8. 

Streptelasma arcticum drummondense Stumm, 1963, p. 27, .pl. 2, 

figs. 4-7. 

Grewingkia rustica (Billings). Liberty, 1964, pl. 6, fig. 8. 

Grewingkia rustica (Billings). Oliver in Simmons and Oliver, 1967, 

p. 9, 10. 

"Streptelasma" spp. A-E and "S." angulatum (Billings). Oliver in 

Simmons and Oliver, 1967, p. 10. 

Grewingkia rustica (Billings). Bolton and Copeland, 1972, pl. B, 

figs. 9, 11. 

Grewingkia sp. Copper, 1978, pl. 6, figs. 3, 4. 

Grewingkia canadensis (Billings). Elias, 1982, p. 66-69, pl. 7, figs. 1-

21; pl. 8, figs. 1-30; pl. 9, figs. 1-21; pl. 10, figs. 1-28. 

Lectotype (designated by Elias, 1982, p. 66).-GSC 

1983h, i, upper member, Georgian Bay Formation,2 

Drummond Island, Mich., A. Murray collection, 184 7 

(Billings, 1862, fig. 93b; Elias, 1982, pl. 10, figs. 9-11). 

Paralectotypes (designated by Elias, 1982, p. 66).-

GSC 1983, q,, 1983b, c, e (Billings, 1862, fig. 93c; Liberty, 

1964, pl. 6, fig. 8; Bolton and Copeland, 1972, pl. B, 

fig. 11), 1983d, 1983{, g, upper member, Georgian Bay 

Formation, Drummond Island, Mich., A. Murray collection, 184 7. 

Occurrences.-G. canadensis is a Late Ordovician 

(Richmondian) species. It is known from: ((Meaford" 

beds, upper member, Georgian Bay Formation, Drummond Island, Mich.; top of the lower member (HWekwemikongsing" beds) and HMeaford" beds of the upper 

member, Georgian Bay Formation, Manitoulin Island, 

Ontario; top of the Georgian Bay Formation, Meaford, 

Ontario; top of the Maquoketa Shale, Little Sturgeon 

Bay, Wis.; Bull Fork Formation, Dillsboro Formation, 

Rowland, Bardstown, Preachersville, and Saluda Dolomite Members of the Drakes Formation, and Whitewater Formation, Cincinnati Arch region, KentuckyIndiana-Ohio (see fig. 1); uArnheim," Fernvale, and 

Sequatchie Formations, Goodlettsville-Gallatin area, 

Tennessee. 

Descri'ption.-G. canadensis is a relatively large species. The corals can be longer than 130 mm and can 

have a diameter greater than 40 mm. External form 

varies from ceratoid to trochoid in early ontogenetic 

stages and is usually cylindrical in late stages. Curva-· 

ture is generally slight in early to intermediate stages, 

and the corals are straight in late stages (pl. 2, figs. 1, 

5, 9, 13). 

In early stages, the major septa are completely dilated 

and extend to or almost to the axis (pl. 2, figs. 2, 6, 10). 

In intermediate stages, the septa are greatly to completely dilated, and a small axial structure consisting 

of a few greatly dilated septal lobes develops (pl. 2, 

figs. 3, 7, 11). In late stages, the septa are nondilated to 

slightly dilated, and the nature of the axial region 

•Georgian Bay Formation of Liberty (1969) geographically extended from 

Ontario, Canada, into: northeastern Michigan on Drummond Island in Lake 

Huron and herein adopted for USGS usage. 
MIDDLE AND LATE ORDOVICIAN SOLITARY RUGOSE CORALS OF CINCINNATI ARCH REGION N9 

varies considerably among corals. There is complete 

gradation from very complex axial structures of septal 

lobes and lamellae, to simple structures of a few septal 

lobes, to open axial regions lacking septal elements 

(pl. 2, fig. 4, complex axial structure; pl. 2, fig. 8, intermediate complexity; pl. 2, fig. 12, simple axial structure). Specimens having moderately complex axial 

structures of septal lobes and lamellae are most frequent. A moderately convex calicular boss is developed 

in corals having an axial structure. The cardinal and 

counter septa are generally distinct in being longer 

than the other major septa throughout ontogeny and in 

often having greatly dilated lobes in intermediate 

stages. The cardinal fossula in late stages is narrow 

and expands at the axial region. Minor septa are generally confined to the stereozone, which is moderately 

broad in late stages. 

Tabellae are present at the periphery of the coral 

(septal region) in incompletely dilated stages. They are 

steeply to moderately inclined up toward the axis in 

intermediate stages and become less steeply inclined 

in later stages. The tabulae in the axial region are 

mostly complete. They are moderately to highly convex 

upward in intermediate stages and in late stages are 

usually moderately convex (pl. 2, figs. 14, 15). 

Discussion.-These corals from the Cincinnati Arch 

region cannot be distinguished from the type specimens 

of Zaphrentis canadensis Billings, 1862. The species is 

assigned to Grewingkia Dybowski, 1873, because it 

generally has an axial structure of the size and complexity characteristic of that genus. In the Cincinnati 

Arch region, these corals were referred to as Streptelasma corniculum Hall, 184 7, by Milne-Edwards and 

Haime (1851), Nicholson (1875b), Rominger (1876), and 

White (1882) and as S. rusticum (Billings, 1858) by Cumings (1908) and Cox (1937). Foerste (1909) described 

S. vagans, S. insolitum, and S. dispandum, distinguishing them primarily on the basis of external form. 

Foerste (1924) synonymized S. vagans with S. rusticum. 

The type specimens of all his species have be~n sectioned; 

they are G. canadensis (USNM 787 42, 787 49, 84870). 

Oliver (in Simmons and Oliver, 1967) reported G. rustica, ffStreptelasma" spp. A-E, and ffS." angulatum 

(Billings, 1862). These represent different growth 

stages and variations of G. canadensis. 

The lectotype of Streptelasma corniculum Hall, 184 7 

(AMNH 645/1) has been described and illustrated by 

Neuman (1969, p. 10, 11, figs. 4-6). This species is presently known only from the lower part of the Trenton 

Group (upper Middle Ordovician) at Middleville, N.Y. 

Zaphrentis canadensis Billings, 1862, was considered a 

synonym of Petraia rustica Billings, 1858, by Lambe 

(1901, p. 110-112), who assigned the species to Streptelasma. Subsequent workers accepted this synonymy. 

Although the two species are similar in external form, 

their internal morphologic features differ. In the lectotype (GSC 5822b, c), paralectotype (GSC 5822, a), and 

topotype material of P. r~stica, the major septa generally form a counterclockwise whorl in early to intermediate stages, and septal dilation is complete to great 

until immediately below the calice in late stages, 

where dilation decreases and a complex axial structure 

of the Grewingkia type develops (Elias, 1982, p. 70-72). 

G. rustica is presently known from the Richmondian at 

Lake St. John, Quebec (type locality), and the HMeaford" beds, upper member, Georgian Bay Formation on 

Manitoulin Island, Ontario. G. canadensis is distinguished by its cardinal and counter septa that are generally longer than the other major septa throughout 

ontogeny and often have greatly dilated lobes in intermediate stages. 

Streptelasma divaricans (Nicholson, 1875b) 

Plate 2, figures 16-33 

Palaeophyllum divaricans Nicholson, 1875b, p. 220, 221, pl. 22, 

.fig. 10, lOa, lOb. 

Palaeophyllum divaricans Nicholson. White, 1882, p. 377, 378, pl. 52, 

fig. 4. 

Streptelasma divaricans (Nicholson). Cumings, 1908, p. 707, 708, 

pl. 1, fig. 6, 6a. 

Streptelasma divaricans (Nicholson). Foerste, 1909, p. 307, 308, pl. 10, 

fig. 4a-e. 

Streptelasma divaricans-angustatum Foerste, 1909, p. 308, pl. 9, 

fig. 6a, 6b. 

Streptelasma cf. divaricans (Nicholson). Foerste, 1917-18, p. 99, pl. 4, 

fig. 2. 

Streptelasma divaricans (Nicholson). Foerste, 1924, p. 67, pl. 2, 

fig. 5a-d. 

Streptelasma divaricans (Nicholson). Elias, 1982, p. 53-56, pl. 1, 

figs. 1.:_41; pl. 2, figs. 1-16; pl. 3, figs. 1-23. 

Lectotype (designated by Elias, 1982, p. 53).-FMNH 

UC413, HCincinnati Group, Cincinnati, Ohio", U. P. 

James collection (Nicholson, 1875b, pl. 22, fig. 10; Elias, 

1982, pl.· 3, figs. 1, 2). 

Occurrences.-S. divaricans is a Late Ordovician 

(Richmondian) species. It is known from: Dillsboro Formation, Rowland, Bardstown, Preachersville, and 

Saluda Dolomite Members of the Drakes Formation, 

and Whitewater Formation, Cincinnati Arch region, 

Kentucky-Indiana-Ohio (fig. 1); ttMeaford" and HKagawong" beds, upper member, Georgian Bay Formation, 

Manitoulin Island, Ontario; Bay de Noc Member, Stonington Formation, s Delta County, Mich. 

Description.-S. divaricans is a relatively small species. Maximum lengths and diameters are slightly 

8

Stonington beds and the Bay de Noc member of Hussey (1926) herein adopted 

as Stonington Formation and its basal Bay de Noc Member for U.S. Geological 

Survey usage. 
N10 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

more than 30 and 15 mm, respectively. External form 

is typically ceratoid, and curvature is usually slight 

(pl. 2, fig. 24). A base of attachment is present on the 

cardinal side (pl. 2, figs. 16, 17). Coralla generally occur 

individually, but 26 percent of 189 specimens consist of 

two or more in lateral contact (pl. 2, figs. 20, 29-33). 

The greatest number seen in a single group is 13 

(Foerste, 1909, pl. 10, fig. 4e). Most of these clusters 

represent pseudocolonies in which the corals grew into 

lateral contact or were attached one to another. True 

coloniality resulting from lateral and peripheral 

asexual increase is rare. 

The septa are generally nondilated throughout 

ontogeny. In early stages the major septa extend to or 

almost to the axis (pl. 2, figs. 21, 25). In late stages the 

nature of the axial region varies considerably among 

corals. There is complete gradation from moderately 

complex axial structu:r:es of septal lobes and lamellae 

(pl. 2, fig. 19), to simple structures having septal lobes 

only (pl. 2, fig. 23), to major septa extending to the axis 

without forming a structure, to septa withdrawn from 

the axis leaving an open axial region (pl. 2, fig. 28). 

Specimens with major septa extending to the axis are 

most frequent. A calicular boss, if developed, is slightly 

convex. The major septa are generally wavy and sometimes twist in a counterclockwise direction. They often 

meet in several groups at the axis. The cardinal septum 

cannot be distinguished from the other major septa, 

and a fossula is not developed. Minor septa are confined 

to or extend a short distance beyond the stereozone, 

which is generally narrow. 

. Tabulae appear in very early stages and are mostly 

complete and moderately convex upward (pl. 2, fig. 29). 

Discussion.-This species was placed in the genus 

Palaeophyllum by Nicholson (1875b) and White (1882) 

and in Streptelasma by Cumings (1908) and Foerste 

(1909). The assignment to Streptelasma Hall, 1847, is 

retained because the species is generally solitary and 

has slightly dilated major septa that usually extend to 

the axis without forming a structure. Foerste (1909) 

distinguished S. divaricans-angustatum on the basis of 

its cylindrical form. However, external and internal 

characters of his type specimens (USNM 84868) lie 

within the range of variability inS. divaricans (Nicholson, 1875b). 

LOCALITY REGISTER 

The coordinate system used herein and the descriptive 

format for the Middle Ordovician locality follow Pojeta 

(1979, p. 19). The stratigraphic positions of Upper 

Ordovician localities are shown in Elias (1982, fig. 3). 

MIDDLE ORDOVICIAN LOCALITY 

Collection number -------

Geographic location------

Coordinates ------------

Formation--------------

Stratigraphic position ----

Silicified ---------------

Quadrangle name -------

Section name -----------

USGS 6034-CO. 

Roadcut on New Watts Mill Rd., 

0.16 km SW. of intersection with 

State Route 39. 

Base of section at 260 mm east, 

346 mm north. 

Tyrone Limestone. 

About 8 m below Pencil Cave bentonite of drillers, which is about 7 m 

below the top of the Tyrone; 37 m 

above base of the section. 

Yes (1468 lbs). 

Little Hickman, Ky. 

Little Hickman A. 

UPPER ORDOVICIAN LOCALITIES 

Locality 1 a. Orangeburg and Maysville East quadrangles, Mason 

Co., Ky. Coordinates: 426 mm east, 558 mm north (Orangeburg quadrangle) to 411 mm east, 10 mm north (Maysville East quadrangle). 

Bull Fork Formation (type section); Preachersville Member, Drakes 

Formation. Roadcuts on east side ofHwy. 1443, 1.45 to 2.3 km north 

of junction with Hwy. 984, 3 km east of Springdale. 

Locality lb. Manchester Islands quadrangle, Adams Co., Ohio. 

Coordinates: 68 mm east, 497 mm north. Bull Fork Formation. 

Streamcut in Isaacs Creek just west of Hwy. 136, 1.8 km south of 

intersection with Hwy. 41 at Bentonville. 

Locality lc. West Union quadrangle, Adams Co., Ohio. Coordinates: 

430 mm east, 360 mm north. Preachersville Member, Drakes Formation. Roadcut on west side ofHwy. 41, 5.45 km northeast of junction 

with Hwy. 247N in West Union. 

Locality 2. Bedford quadrangle, Trimble Co., Ky. Coordinates: 

365 mm east, 466 mm north to 336 mm east, 446 mm north. Bull 

Fork Formation; Rowland, Bardstown, and Saluda Dolomite Members, Drakes Formation. Roadcuts on north and south sides of 

Hwy. 42, 3.5 to 4.4 km east of Bedford. 

Locality 3. Jeffersontown quadrangle, Jefferson Co., Ky. Coordinates: 338 mm east, 51 mm north to 325 mm east, 52 mm north. Rowland, Bardstown, and Saluda Dolomite Members, Drakes Formation. 

Roadcuts and quarry on north side of Brush Run Road, 0.25 to 0.65 

km east of junction with Hwy. 1819, about 1.5 km west-northwest of 

Seatonville. 

Locality 4. Maud quadrangle, Nelson Co., Ky. Coordinates: 70 mm 

east, 81 mm north to 59 mm east, 108 mm north. Gilbert Member, 

Ashlock Formation; Grant Lake Limestone; Rowland, Bardstown 

(type section), and Saluda Dolomite Members, Drakes Formation. 

Roadcut on west side ofHwy. 150, 1.15 to 1.9 km northwest of bridge 

over Beech Fork River, about 2 km northwest of Fredericktown. 

Locality 5a. Whitcomb quadrangle, Franklin Co., Ind. Coordinates: 

24 mm east, 285 mm north to 42 mm east, 289 mm north. Dillsboro 

Formation. Roadcut on north side ofHwy. 101 at Bon Well Hill about 

2 km northeast of Brookville. 

Locality 5b. Whitcomb quadrangle, Franklin Co., Ind. Coordinates: 

183 mm east, 508 mm north to 183 mm east, 532 mm north. Dillsboro 

Formation; Whitewater Formation, including Saluda Dolomite 

Member. Roadcuts on both sides ofHwy. 101 about 9.5 km northeast 

of Brookville. 

Locality 5c. Brookville quadrangle, Franklin Co., Ind. Coordinates: 

424 mm east, 292 mm north to 423 mm east, 305 mm north. Dillsboro 

Formation. Cut at Brookville Dam Spillway about 2 km north of 

Brookville. 
MIDDLE AND LATE ORDOVICIAN SOLITARY RUGOSE CORALS OF CINCINNATI ARCH REGION Nll 

Locality 6a. Lancaster quadrangle, Lincoln Co., Ky. Coordinates: 

55 mm east, 358 mm north. Terrill and Reba Members, Ashlock Formation (type section). Roadcuts on both sides ofHwy. 27, 1 km north 

of Dix River, about 5.5 km southwest of Lancaster. 

Locality 6b. Paint Lick quadrangle, Garrard Co., Ky. Coordinates: 

13 mm east, 152 mm north. Rowland Member, Drakes Formation 

(type section). Roadcuts about 0.4 km south of East Fork, Drakes 

Creek, on east side of road leading northwest from Vanhock Cemetery, about 3 km east of Preachersville. 

Locality 6c. Lancaster and Crab Orchard quadrangles, Lincoln Co., 

Ky. Coordinates: 405 mm east, 7 mm north (Lancaster quadrangle) 

to 410 mm east, 574 mm north (Crab Orchard quadrangle). Preachersville Member (type section), Drakes Formation. Roadcuts on east side 

of Hwy. 39, 3.7 to 3.95 km southeast of Preachersville. 

Locality 7a. Union City quadrangle, Madison Co., Ky. Coordinates: 

232 mm east, 244 mm north to 218 mm east, 235 mm north. Rowland 

and Preachersville Members, Drakes Formation. Roadcuts on both 

sides of Hwy. 974, 0.8 to 1.25 km northeast of Union City. 

Locality 7b. Union City quadrangle, Madison Co., Ky. Coordinates: 

52 mm east, 200 mm north to 38 mm east, 186 mm north. Rowland 

and Preachersville Members, Drakes Formation. Roadcut on east 

side of road, 0.8 to 1.3 km northeast of junction with Hwy. 974, about 

3.5 km west of Union City. 

Locality 8. Moberly quadrangle, Madison Co., Ky. Coordinates: 

4 mm east, 537 mm north to 43 mm east, 521 mm north. Terrill and 

Reba Members (type section), Ashlock Formation; Rowland and 

Preachersville Members, Drakes Formation. Roadcuts on both sides 

of Hwy. 52, about 3 km east of Richmond. 

Locality 9. Hedges quadrangle, Clark Co., Ky. Coordinates: 140 mm 

east, 175 mm north to 152 mm east, 139 mm north. Terrill and Reba 

Members, Ashlock Formation; Rowland and Preachersville Members, 

Drakes Formation. Railroad cuts on Louisville and Nashville Railroad, 1.4 to 2.4 km north of Howard Creek, 0.2 to 1.2 km southeast of 

Agawam. 

Locality lOa. Hillsboro quadrangle, Fleming Co., Ky. Coordinates: 

159 mm east, 194 mm north. Sunset Member, Bull Fork Formation. 

Roadcut on east side of road along Buttermilk Branch, 1.6 km northwest of Sunset. 

Locality JOb. Hillsboro quadrangle, Fleming Co., Ky. Coordinates: 

179 mm east, 187 mm north. Bull Fork Formation. Roadcut on east 

side of road along Buttermilk Branch, 1.1 km northwest of Sunset. 

Locality JOe. Hillsboro quadrangle, Fleming Co., Ky. Coordinates: 

168 mm east, 246 mm north. Bull Fork Formation. Roadcut on north 

side of road 1.5 km south of junction of Locust Creek and Hillsboro 

Branch, 4 km west-northwest of Hillsboro. 

Locality JOd. Hillsboro quadrangle, Fleming Co., Ky. Coordinates: 

290 mm east, 240 mm north. Bull Fork Formation. Stream cut in 

tributary just south of road on north side of Hillsboro Branch, 1.35 km 

northwest of Hillsboro. 

Locality JOe. Hillsboro quadrangle, Fleming Co., Ky. Coordinates: 

227 mm east, 310 mm north. Bull Fork Formation. Roadcut on north 

side of road 0.6 km south of Locust Creek, 3.6 km northwest of 

Hillsboro. 

Locality 10{ Hillsboro quadrangle, Fleming Co., Ky. Coordinates: 

319 mm east, 320 mm north. Preachersville Member, Drakes Formation. Roadcut on east side of Hwy. 111, 3 km north of Hillsboro. 

Locality lla. Milan quadrangle, Ripley Co., Ind. Coordinates: 

16 mm east, 305 mm north to 0 mm east, 308 mm north. Dillsboro 

Formation; Whitewater Formation, including Saluda Dolomite 

Member. Roadcuts on east and west sides of Hwy. 50, 1.1 to 1.5 km 

west of Laughery Creek at Versailles. 

Locality llb. Milan quadrangle, Ripley Co., Ind. Coordinates: 

80 mm east, 372 mm north, 103 mm east, 379 mm north, and 108 mm 

east, 390 mm north. Dillsboro Formation. Stream cuts on Falling 

Timber Creek, 0.4, 1.15, and 1.45 km upstream from Laughery 

Creek, about 2.3 to 3.1 km northeast of Versailles. 

Locality 12a. Richmond quadrangle, Wayne Co., Ind. Coordinates: 

364 mm east, 448 mm north. Whitewater Formation. Stream cut at 

Thistlewaite Falls on West Fork of Whitewater River just south of 

bridge in Spring Grove. 

Locality 12b. Richmond and New Paris quadrangles, Wayne Co., 

Ind. Coordinates: 392 mm east, 103 mm north (Richmond quadrangle) 

to 37 mm east, 134 mm north (New Paris quadrangle). Whitewater 

Formation. Stream cuts along Elkhorn Creek between Straight Line 

Road and Hwy. 227, about 6 km south of Richmond. 

Locality 12c. Richmond quadrangle, Wayne Co., Ind. Coordinates: 

175 mm east, 156 mm north. Dillsboro Formation. Stream cuts at 

Blue Clay Falls on creek just south of Hunt Road, 0.55 km west of 

Salisbury Road, about 7 km southwest of Richmond. 

Locality 12d. Liberty quadrangle, Wayne Co., Ind. Coordinates: 

148 mm east, 496 mm north to 152 mm east, 501 mm north. Dillsboro 

Formation. Roadcut on east side of Smithfield Road, 0.1 to 0.25 km 

north of intersection with Potter Shop Road, 0.4 km east of Abington. 

Locality 13a. Fairborn quadrangle, Greene Co., Ohio. Coordinates: 

128 'mm east, 211 mm north. Whitewater Formation. Railroad cuts 

primarily on south side of New York Central Railroad, 0.1 km north 

of WrigJtt Brothers Memorial, about 6 km southwest of Fairborn. 

Locality 13b. Fairborn quadrangle, Greene Co., Ohio. Coordinates: 

119 mm east, 215 mm north. Dillsboro and Whitewater Formations. 

Cut on south bank of Mad River, 0.1 km southwest of Huffman Dam, 

about 6 km southwest of Fairborn. 

Locality 14a. Clarksville quadrangle, Clinton Co., Ohio. Coordinates: 253 mm east, 83 mm north to 263 mm east, 65 mm north. 

Dillsboro and Whitewater Formations. Cut on north side of Cowan 

Creek, 0.2 to 0.75 km downstream from Cowan Lake spillway, about 

4. 7 km east-southeast of Clarksville. 

Locality 14b. Oregonia quadrangle, Warren Co., Ohio. Coordinates: 

70 mm east, 195 mm north to 63 mm east, 184 mm north. Dillsboro 

Formation. Roadcuts primarily on west side of road just south of 

Hwy. l-71leading to picnic area on Little Miami River, about 1.7 km 

northwest of Fort Ancient State Memorial. 

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no. 1, p. 275-283. 

Billings, E., 1858, Report for the year 1857: Geological Survey of 

Canada, Report of Progress (1857), p. 14 7-192. 

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Bolton, T. E., and Copeland, M. J., 1972, Manitoulin Island regionOrdovician and Silurian fossils, in Robertson, J. A., and Card, 

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p. 54-61. 

Browne, R. G., 1964, The coral horizons and stratigraphy of the 

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fossils: American Zoologist, v. 9, no. 3, ed. 2, p. 689-703, 1 pl. 
N12 CONTRIBUTIONS TO THE ORDOVICIAN PALEONTOLOGY OF KENTUCKY AND NEARBY STATES 

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Copper, P., 1978, Paleoenvironments and paleocommunities in the 

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the road log to the Michigan Basin Geological Society field trip 

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Cumings, E. R., 1908, The stratigraphy and paleontology of the 

Cincinnati Series of Indiana: Indiana Department of Geology and 

Natural Resources, Annual Report, v. 32, p. 605-1188, 55 pls. 

Dennison, J. M., 1976, Appalachian Queenston delta related to 

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Proceedings of a Palaeontological Association symposium, Birmingham, September 1974: Cardiff, University of Wales Press 

and National Museum of Wales, p. 107-120. 

Dybowski, W., 1873, Monographie der Zoantharia sclerodermata 

rugosa aus der Silurformation Estlands/Nord-Livlands und der 

Insel Gotland: Archiv fur die Naturkunde Liv-, Ehst- und Kurlands, ser. I, v. 5, no. 3, p. 257~414, pls. 1, 2. 

Elias, R. J., 1980, Borings in solitary rugose corals of the Selkirk 

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southern Manitoba: Canadian Journal of Earth Sciences, v. 17, 

no. 2, p. 272-277. 

____ 1981, Solitary rugose corals of the Selkirk Member, Red 

River Formation (late Middle or Upper Ordovician), southern 

Manitoba: Geological Survey of Canada Bulletin 344, 53 p., 11 pls. 

____ 1982, Latest Ordovician solitary rugose corals of eastern 

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no. 314, 116 p., 15 pls. 

____ 1983, Late Ordovician solitary rugose corals of the Stony 

Mountain Formation, southern Manitoba, and its equivalents: 

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v. 14, p. 289-333, pls. 7-11. 

____ 1917-18, The Richmond faunas of Little Bay de Noquette, 

in northern Michigan: Ottawa Naturalist, v. 31, no. 9 (1917), 

p. 97-103; no. 10 (1918), p. 121-127, pls. 4-6. 

____ 1924, Upper Ordovician faunas of Ontario and Quebec: 

Geological Survey of Canada Memoir 138, 255 p., 46 pls. 

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Survey of Canada, Report of Progress, 983 p. 

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338 p., 87 pls. 

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. Hill, Dorothy, 1961, On the Ordovician corals Palaeophyllum rugosum 

Billings and Nyctopora billingsii Nicholson: Geological Survey of 

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Geologicheskii Institut (VSEGEI), Trudy, novaya seriya, no. 12, 

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MIDDLE AND LATE ORDOVICIAN SOLITARY RUGOSE CORALS OF CINCINNATI ARCH REGION N13 

376-401, pls. 44-55. 

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of Minnesota, v. 3, pt. 1, Paleontology: Minneapolis, Minnesota 

Geological and Natural History Survey, chapter 3, p. 55-95. 
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 

[All specimens are whitened with ammonium chloride. Cardinal side faces down in all calicular views. All specimens are from about 8 m 

below Pencil Cave bentonite of drillers, which is about 7 m below the top ofTyrone Limestone, High Bridge Group, USGS locality 6034-CO.] 

FIGURES 1, 2. Lambeophyllum? sp. A (p. N7). USNM 334851. 

1. Alar view, cardinal side left, x 1.5. 

2. Calicular view, stereopair, x 2. 

3. Lambeophyllum? sp. A (p. N7). USNM 334852. 

Calicular view, stereopair, x 2.5. 

4, 5. Lambeophyllum? sp. A (p. N7). USNM 334853. 

4. Alar view, cardinal side left, x 2. 

5. Calicular view, stereopair, x 2.5. 

6, 7. Lambeophyllum? sp. A (p. N7). USNM 334854. 

6. Alar view, cardinal side right, x 3. 

7. Calicular view, stereopair, x 4. 

8. Lambeophyllum? sp. A (p. N7). USNM 334855. 

Calicular view, stereopair, x 7. 

9, 10. Lambeophyllum? sp. A (p. N7). USNM 334856. 

9. Alar view, cardinal side right, x 8. 

10. Calicular view, stereopair, x 10. 

11, 12. Lambeophyllum? sp. B (p. N7). USNM 334857. 

11. Alar view, cardinal side left, x 3. 

12. Calicular view, stereopair, x 4. 

13. Lambeophyllum? sp. B (p. N7). USNM 334858. 

Calicular view, stereopair, x 10. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066 - N- PLATE 1 

2 

3 

10 

13 

LAMBEOPHYLLUM? 
PLATE 2 

[Exterior views are of specimens whitened with ammonium chloride. Transverse and longitudinal sections were prepared using thin sections 

as negatives in a photographic enlarger. Transverse sections are oriented as they appear looking from the top of the coral towards the tip. 

Locality information for specimens in figures 1-28 and 33 is given in Locality Register. Available information for specimens in figures 29-32 

is given in figure explanations below.] 

FIGURES 1-4. Grewingkia canadensis (Billings, 1862) (p. N8). 

UCGM 45390. Whitewater Formation, locality 12a. 

1. Exterior· alar view, cardinal side left, x 1. 

2-4. Transverse sections, cardinal side down, x 1.5. 

5-8. Grewingkia canadensis (Billings, 1862) (p. N8). 

UCGM 45193. Upper part of Bardstown Member or lower part of Saluda Dolomite Member, Drakes Formation, locality 2. 

5. Exterior alar view, cardinal side left, x 1. 

6-8. Transverse sections, cardinal side down, x 1.5. 

9-12. Grewingkia canadensis (Billings, 1862) (p. N8). 

UCGM 45183. Bull Fork Formation, locality 1a. 

9. Exterior alar view, cardinal side left, x 1. 

10-12. Transverse sections, cardinal side down, x 1.5. 

13-15. Grewingkia canadensis (Billings, 1862) (p. N8). 

UCGM 45446. Dillsboro Formation, locality 13b. 

13. Exterior alar view, cardinal side left, X 1. 

14, 15. Longitudinal sections, cardinal side left, x 1.5. 

16-19. Streptelasma divaricans (Nicholson, 1875b) (p. N9). 

UCGM 45072. Whitewater Formation, locality 12a. 

16. Exterior alar view, cardinal side left, x 1. 

17-19. Transverse sections, cardinal side down, x 3. 

20-23. Streptelasma divaricans (Nicholson, 1875b) (p. N9). 

UCGM 45084. Whitewater Formation, locality 12a. 

20. Exterior view, x 1. 

21-23. Transverse sections, x 3. 

24-28. Streptelasma divaricans (Nicholson, 1875b) (p. N9). 

UCGM 45086. Whitewater Formation, locality 12a. 

24. Exterior alar view, cardinal side left, x 1. 

25-28. Transverse sections, cardinal side down, x 3. 

29. Streptelasma divaricans (Nicholson, 1875b) (p. N9). 

UCGM 45145. Whitewater Formation, entrance to Hueston Woods Park, Oxford, Ohio. Longitudinal section, <:ardinal 

side left, x 3. 

30. Streptelasma divaricans (Nicholson, 1875b) (p. N9). 

USNM 311628. Dillsboro Formation, near Clarksville, Ohio. Coralla attached to ramose bryozoan, x 1. 

31. Streptelasma divaricans (Nicholson, 1875b) (p. N9). 

USNM 40086. Whitewater Formation, Oxford, Ohio. Coralla attached to Lepidocyclus? capax, x 1. 

32. Streptelasma divaricans (Nicholson, 1875b) (p. N9). 

USNM 135767. Whitewater Formation, Richmond, Indiana. Coralla attached to Rafinesquina alternata, x 1. 

33. Streptelasma divaricans (Nicholson, 1875b) (p. N9). 

UCGM 45121. Whitewater Formation, locality 13a. Bedding surface with coralla in growth position on brachiopod 

fragment (upper right) and on bryozoan (lower right), x 1. 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 1066 - N- PLATE 2 

22 

GREWINGKIA AND STREPTELASMA 

Elias-MIDDLE AND LATE ORDOVICIAN SOLITARY RUGOS£ CORALS OF CINCINNATI ARCH REGION-Geological Survey Profession