Carbonate Fades and the 

Lithostrotionid Corals of the 

Mississippian Kogruk Formation, 

DeLong Mountains, 

Northwestern Alaska

GEOLOGICAL SURVEY PROFESSIONAL PAPER 664
CARBONATE FACIES AND THE LITHOSTROTIONID CORALS OF THE

MISSISSIPPIAN KOGRUK FORMATION, 

DELONG MOUNTAINS, NORTHWESTERN ALASKA
Panoramic view eastward from a helicopter above a cirque in August 1968, showing section 62C-31 and parts of the

DeLong Mountains.
Carbonate Fades and the 

Lithostrotionid Corals of the 

Mississippian Kogruk Formation, 

DeLong Mountains, 

Northwestern Alaska

By AUGUSTUS K. ARMSTRONG

GEOLOGICAL SURVEY PROFESSIONAL PAPER 664

Systematic pahontologic studies of the lithostrotionid 

corals from four sectio?is of carbonate rocks in the 

Mississippian Kogruk Formation, DeLong 

Mountains, Brooks Range, northwestern Alaska

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1970
UNITED STATES DEPARTMENT OF THE INTERIOR 

WALTER J. HICKEL, Secretary

GEOLOGICAL SURVEY 

William T. Pecora, Director

Library of Congress catalog card No. 76-606745

For sale by the Superintendent of Documents, U.S. Government Printing Office 

Washington, D.C. 20402 - Price $1.00 (paper cover)
CONTENTS

Abstract- ___________--____--_________-_--__--_______

Introduction.. . _____________________________________

Acknowledgments _ _ ________________________________

Regional setting and previous work ___ _______________

Environments of deposition and carbonate facies_________

Characteristic carbonate rock types ____________________

Marine lime mudstones to echinoderm-bryozoan 

wackestones __________________________________

Echinoderm-bryozoan wackestones to packstones___ 

Ooid to oolitic grainstones _ ______________________

Echinoderm-bryozoan grainstones _ _________________

Calcitic dolomites and dolomites. __________________

Age and correlation of the lithostrotionid coral faunas____

Systematic paleontology. __-__-___-_____-__-_--____--_

Family Lithostrotionidae d'Orbigny, 1851__--_--___- 

Genus Lithostrotion Fleming, 1 S28___ ___________

Subgenus Siphonodendron McCoy, 1849_____

Lithostrotion (Siphonodendron) sinuosum

Lithostrotion (Siphonodendron) aff. L.

(S.) sinuosum (Kelly) _ ____________

Lithostrotion (Siphondendron) warreni

Nelson________ _______ ____________

Lithostrotion (Siphonodendron) sp. A___

Page 

1 

1

1

2

3

6

6

7

7

8

8

8

9

9

9

9

9

12

13

15

Systematic paleontology Continued Page

Family Lonsdaleiidae Chapman, 1893_____________ 16

Genus Lithostrotionella Yabe and Hayasaka,

1915___-----------------__-____-___-__ 16

Lithostrotionella banffensis (Warren)_______ 16

Lithostrotionella aff. L. banffensis (Warren) __ 19

Lithostrotionella birdi Armstrong._________ 20

Lithostrotionella mdareni (Sutherland) _____ 21

Lithostrotionella macouni (Lambe)_________ 23

Lithostrotionella sp. A__________________ 25

Lithostrotionella sp. B_____-_-----_-_---__ 26

Genus Thysanophyllum Nicholson and Thomson,

1876_______ -__- _- - ------ 26

Thysanophyllum orientale Thomson________ 27

Thysanophyllum astraeiforme (Warren).___ 28

Thysanophyllum sp. A___________________ 30

Genus Sciophyllum Harker and McLaren, 1950_ 30

Sciophyllum lambarti Harker and McLaren. 31

Sciophyllum alaskaensis Armstrong._______ 32

Sciophyllum sp. A___ ____________________ 33

Selected references.______________-___-_---------_--- 34

Index.____________-___-_--___-----__--_----------- 37

ILLUSTRATIONS

[Plates follow index]

PLATE 1. Lithostrotion (Siphonodendron) sinuosum (Kelly) and Lithostrotion (Siphonodendrori) warreni Nelson.

2. Lithostrotion (Siphonodendrori) warreni Nelson and Lithostrotion (Siphonodendrori) sp. A.

3. Lithostrotion (Siphonodendrori) aff. L. (/S.) sinuosum (Kelly), Lithostrotion (Siphonodendrori) sinuosm (Kelly), 

and Lithostrotionella banffensis (Warren).

4. Lithostrotionella banffensis (Warren), Lithostrotionella aff. L. banffensis (Warren), and Lithostrotionella birdi 

Armstrong.

5. Lithostrotionella birdi Armstrong and Lithostrotionella mdareni (Sutherland).

6. Lithostrotionella mdareni (Sutherland) and Sciophyllum lambarti Harker and McLaren.

7. Lithostrotionella sp. A and Lithostrotionella sp. B.

8. Thysanophyllum orientale Thomson.

9. Thysanophyllum astraeiforme (Warren).

10. Lithostrotionella banffensis (Warren) and Sciophyllum alaskaensis Armstrong.

11. Thysanophyllum sp. A and Sciophyllum sp. A.

12. Lithostrotionella macouni (Lambe) syntype.

13. Photomicrographs of carbonate rock types, sections 62C-15, 62C-31.

14. Photomicrographs of carbonate rock types, sections 62C-31, 60A-400 403, 62C-34.

FRONTISPIECE. Panorama of DeLong Mountains and location of measured section 62C-31.
VI CONTENTS

Page 

FIGURE 1. Index map of northwestern Alaska showing general location of measured sections described in this report___ 2

2. Diagram showing lithologic and paleontologic symbols used in this report-______________________________ 3

3. Columnar section showing carbonate stratigraphy and coral distribution, section 62C-15_--_-_-___________ 4

4. Index map showing location of section 62C-15______-___-_____--____---_-_-_-_____-_------_-____-___ 4

5. Columnar section showing carbonate stratigraphy and coral distribution, section 62C-31_________________ 5

6. Index map showing location of section 62C-31 _______-_____------_-_---_----_--___--_--_______-_____ 6

7. Columnar section showing carbonate stratigraphy and coral distribution, section 60A-400 403____________ 6

8. Index map showing location of section 60A-400 403___---_-_-__-_------_---_________________________ 7

9. Columnar section showing carbonate stratigraphy and coral distribution, section 62C-34__________________ 7

10. Index map showing location of section 62C-34_______________________________________________________ 7

11. Graphs showing corallite diameter and number of major septa in Lithostrotion (Siphonodendron) sinuosvm

(Kelly)_____________________________________________________________________________________ 11

12. Longitudinal and transverse section of Lithostrotion (Siphonodendron) sinuosum (Kelly)__________________ 12

13. Graph showing corallite diameter and number of major septa in Lithostrotion (Siphonodendron) aff. L. (S.~)

sinuosum (Kelly)_____________________________________________________________________________ 12

14. Transverse section of Lithostrotion (Siphonodendron) aff. L. (S.) sinuosum (Kelly)__________________________ 13

15. Graph showing corallite diameter and number of major septa in Lithostrotion (Siphonodendron) warreni

Nelson____________________________________________________________________________________ 13

16. Longitudinal and transverse sections of Lithostrotion (Siphonodendron) warreni Nelson_ _____________________ 13

17. Graph showing corallite diameter and number of major septa in Lithostrotion (Siphonodendron) sp. A_________ 15

18. Longitudinal and transverse section of Lithostrotion (Siphonodendron) sp. A________________________________ 15

19. Graph showing corallite diameter and number of major septa in Lithostrotionella banffensis (Warren) and

Lithostrotionella aff. L. banffensis (Warren)_______________________________________________________ 17

20. Longitudinal and transverse section of Lithostrotionella banffensis (Warren) _______________________________ 17

21. Longitudinal and transverse sections of Lithostrotionella aff. L. banffensis (Warren)_________________________ 19

22. Graphs showing corallite diameter and number of major septa in Lithostrotionella birdi Armstrong-________ 20

23. Longitudinal and transverse sections of Lithostrotionella birdi Armstrong-_______________________________ 20

24. Graph showing corallite diameter and number of major septa in Lithostrotionella mclareni (Sutherland)______ 23

25. Longitudinal and transverse sections of Lithostrotionella mclareni (Sutherland)___________________________ 23

26. Graph showing corallite diameter and number of major septa in Lithostrotionella macouni (Lambe), Lithostrotionella sp. A, and Lithostrotionella sp. B______-__-_____-_-_-__-__-_________-_-____-___------- 24

27. Longitudinal and transverse sections of Lithostrotionella macouni (Lambe)_______________________________ 24

28. Longitudinal and transverse sections of Lithostrotionella sp. A__________________________________________ 25

29. Longitudinal and transverse sections of Lithostrotionella sp. B_ ________________________________________ 26

30. Graph showing corallite diameter and number of major septa in Thysanophyllum orientale Thomson..______ 27

31. Longitudinal and transverse section of Thysanophyllum orientale Thomson_______________________________ 28

32. Graph showing corallite diameter and number of major septa in Thysanophyllum astraeiforme (Warren) and

Thysanophyllum sp. A________________________________________________________________________ 29

33. Longitudinal and transverse sections of Thysanophyllum astraeiforme (Warren)___________________________ 29

34. Longitudinal and transverse section of Thysanophyllum sp. A__________________________________________ 30

35. Longitudinal and transverse sections of Sciophyllum lambarti Marker and McLaren_______________________ 31

36. Longitudinal and transverse sections of Sciophyllum alaskaensis Armstrong._____________________________ 32

37. Longitudinal and transverse section of Sciophyllum sp. A_____________________________________________ 34

TABLE

TABLE 1. Classification of carbonate rocks according to depositional texture (Dunham, 1962).

Page
CARBONATE FACIES AND THE LITHOSTROTIONID CORALS

OF THE MISSISSIPPIAN KOGRUK FORMATION, 

DELONG MOUNTAINS, NORTHWESTERN ALASKA

By AUGUSTUS K. ARMSTRONG

ABSTRACT

The Kogruk Formation of the Lisburne Group is 1,500-2,000 

feet thick and is composed of marine carbonate rocks deposited 

in normal-marine to shoaling-water environments. Carbonate 

rock types are typically bryozoan-echinoderm packstones and 

wackestone and lesser amounts of lime mudstones and ooid 

grainstones and packstones. Extensive dolomitization, dolomites, 

and carbonate sedimentary features characteristic of intertidal 

and supratidal environments are absent in the sections studied. 

The Kogruk Formation was deposited in an open marine environment on a subsiding shelf on which carbonate deposition 

and subsidence were near equilibrium. Only minor oscillations in 

environments of deposition are seen in a typical section. Lithostrotionid coral faunas are best developed adjacent to the shoaling-water facies.

Two major coral faunas are recognized and described. The 

older, 200-600 feet above the base of the Kogruk Formation, 

consists of Lithostrotion (Siphonodendron) sinuosum (Kelly), 

L. (8.) warreni Nelson, Litliostrotionella mclareni (Sutherland), 

Lithostrotionella aff. L. banffcnsis (Warren), ThysanopliyUum 

astraeifonne (AVarren), Tliysanopliyllutn orientate Thomson, 

and Sciophyllum Jambarti Harker and McLaren. This fauna is 

of middle Meramec age. The younger coral fauna is found in the 

highest 600-800 feet of the Kogruk Formation and contains many 

of the species of lithostrotionids from lower beds, plus LitlwstrotioneUa- sp. A, L. sp. B, L. banffensis (AVarren), Lithostrotionella. bird! Armstrong, Tliysanopliyllum sp. A, Sciopliyllum 

alaskaensis Armstrong, and Faberopliylliim spp. This fauna is 

of late Meramec age. The youngest coral fauna in the Kogruk 

Formation contains Tliysanopliyllum orientate Thomson and 

Lithostrotionella birdi Armstrong and is of very late Meramec 

age.

Lithostrotionid corals, collected from the Nasorak Formation 

near Cape Thompson, described and compared to the Kogruk 

Formation coral fauna, are Lithostrotlon (8iphono(lendron) 

siniiosuni (Kelly), L. (#.) warreni Nelson, Litliostrotion (Niphon-odendron) sp. A, LitliostrotioneUa banffensis (AVarren), 

Tht/sanophyllitm astraeifonne (Warren), Sciophyllum lambarti 

Harker and McLaren, and Sciophyllum sp. A.

INTRODUCTION

The material for this study was collected in northwestern Alaska by Shell Oil Co. personnel during two 

field seasons (fig;. 1). In 1960 Dr. Sigmund Snelson

measured and collected from the thick section of the 

Kogruk Formation at Trail Creek (60A-400-403) and 

from the section near Cape Thompson. In a field party 

led by Dr. Snelson in 1962, the writer and Dr. Kenneth 

Bird collected from two sections of the Kogruk Formation (62C-15 and 62C-31) in the DeLong Mountains 

and from one section (62C-34) in the Lisburne Hills 

by the Kukpuk River.

The stratigraphic sections described in this report 

were measured with Jacob's staff and tape. Rock and 

Foraminifera samples were collected every 5-10 fe?t. 

Brachiopod and coral collections were made throughout the sections. Petrographic thin sections were made 

for carbonate microfacies and microfauna (Foraminifera) studies. The corals collected were studied by 

means of 2-iuch by 3-inch oriented thin sections.

Dunham's (1962) classification of carbonate rocks is 

used in this report. This system of describing carbonrte 

rocks is based on a terminology that indicates particle 

type and texture. Table 1 is Dunham's classification. 

The lithologic and paleontologic symbols used in the 

present report are shown in figure 2.

ACKNOWLEDGMENTS

The excellent stratigraphic collection which forms the 

basis for this study is from the Shell Oil Co. collections. 

The material was made available to the U.S. Geological 

Survey for study by R. E. McAdams and G. E. Burton, 

vice presidents, J. C. Threet, exploration manager, Pacific Coast Area, and Quey C. Hebrew, Northwest Division manager, Shell Oil Co.

Dr. Bernard L. Mamet, University of Montreal, 

studied the Foraminifera in petrographic thin sections 

made from stratigraphic collection samples.

Duplicate sets of thin sections were cut from the coral 

samples by Robert Shely, and the photographs were 

made by Kenji Sakamoto, both of the U.S. Geological 

Survey.
CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA 

TABLE 1. Classification of carbonate rocks according to depositional texture (Dunham, 1962, p. 117)

Depositional texture recognizable

Original components not bound together during deposition

Contains mud (particles of clay and fine silt size)

Mud-supported

Less than 10 percent 

grains

Mudstone

More than 10 percent 

grains

Wackestone

Grain-supported 

Packstone

Lacks mud and is 

grain-supported

Qrainstone

Original components were bound together during deposition * * * as 

shown by intergrown skeletal matter, lamination contrary to gravity, 

or sediment-floored cavities that are 

roofed over by organic or questionably organic matter and are too 

large to be interstices

Boundstone

Depositional terture not 

recognizable

Crystalline carbonate.

(Subdivide according to 

classifications designed to 

bear on physical texture 

or diagenesis.)

Special thanks are clue J. T. Dutro, Jr., W. A. Oliver, 

Jr., W. J. Sanclo, and E. W. Bamber for their help during preparation of the manuscript and for their critical 

review of the manuscript.

The author is grateful to E. W. Bamber and T. E. 

Bolton of the Geological Survey of Canada for the loan 

of a type specimen.

REGIONAL SETTING AND PREVIOUS WORK

The rock sequences which form the DeLong Mountains, northwest Brooks Range, are tentatively grouped 

by Snelson and Tailleur (1968, p. 567) into five tectonic 

units, each of which is characterized by northward 

thrusting of a distinctive rock unit. The light-gray 

shallow-marine carbonate rocks that contain the lithostrotionid corals discussed in this report belong to the 

middle tectonic unit (Sequence III, Kelly subunit B). 

All the stratigraphic sections described in this report 

are in imbricated, rootless thrust sheets which are many 

tens of miles north of the original sites of deposition. 

The Kogruk Formation, together with the other Mississippian formations of the DeLong Mountains, was 

named by Sable and Dutro (1961, p. 592) for outcrops 

on Tupik Mountain. The Kogruk Formation is 520- 

1,500 feet thick and is composed of cliff-forming lightgray- to bluish-gray-weathering limestone (Sable and 

Dutro, 1961, p. 590). It is underlain by the LTtukok Formation of Early Mississippian age; the Utuko1^ is some 

2,500 feet thick at the type locality and consists of ferruginous sandy limestone, calcareous and ouartzitic

FIGURE 1. General location of measured sections described in this report.
ENVIRONMENTS OF DEPOSITION AND CARBONATE FACIES

Composition, in percent

10 50 100 Dolomite Carbonate particles other than fossils

I I I

, I I I

L I L ^

y y y

y y y

y y y

/ /

/ /

/ /

30 90 50 10 C 

Limestone Dolomitic Calcitic dolomite Dolomite

0 Limestone

Dolomit 

limestone

Texture

mdst 

Lime mudstone

wkst 

Wackestone

pkst 

Packstone

gnst 

Grainstone

Size mm Mud

Silt

 0. 

Sand

 2

Granule

Pebble

*

4>

0 

0

0 

<D>

Coated particles

One layer More than one layer

Superficial 

ooid 

-O

Oolite 

®

Pisoid

©

Shale Sandstone 

Nodular chert

Symbols for fossil particles

& ^

Foraminifera Echinoderms 

Gastropods

Brachiopods Ostracodes 

^? >» 

Algae

o

Corals

Bryozoans 

FIGURE 2. Lithologic and paleontologic symbols used in this report.

sandstone, and calcareous shale. The contact between 

the Utukok and Kogruk Formations is conformable and 

gradational. The Tupik Formation, 135-700 feet thick, 

of Late Mississippian age overlies the Kogruk Formation with apparent conformity, but the lithologic change 

at the contact is abrupt. The Tupik Formation in outcrop is thin bedded, contains abundant bedded chert, 

and weathers to a dark gray.

The sections studied in this report do not include the 

type section of the Kogruk Formation. The locations 

of the sections are shown in figure 1.

ENVIRONMENTS OF DEPOSITION AND 

CARBONATE FACIES

The four sections of the Kogruk Formation described 

in this report are as much as 1,920 feet thick and are 

composed of carbonate rock deposited in normal-marine 

to shoaling-water environments; the location of each 

section is shown in figures 4, 6, 8, and 10. In outcrop the 

Kogruk Formation is medium- to massive-bedded 

light-olive-gray to medium-gray limestone and in places 

is cliff forming. It contains nodular to lenticular lightgray to dark-gray chert. The amount of chert, varies 

markedly at different horizons (figs. 3, 5, 7, 9).

The contact between the Utukok Formation and 

Kogruk Formation is gradational (Sable and Dutro, 

1961). The contact is generally obscured by talus and 

rubble but was well exposed in section 62C-15 (fig. 3). 

The silty fine-grained sandstones, shales, and arenaceous 

limestones of the Utukok Formation grade into the

378-461 O 70 2

Kogruk Formation carbonates within a stratigraphic 

distance of 100 feet. In section 62C-15 (fig. 3) tilie brsal 

360 feet of carbonates in the Kogruk Formation contain relatively high-energy current-deposited grginstones and packstones. These are ooid-to-oolitic echinoderm grainstones and packstones, carbonate rock types 

that indicate deposition in shoaling-water and tidalchannel environments.

The most common rock types within the Kogruk 

Formation are bryozoaii-echinoderm wackestones and 

packstones. These carbonate rock types are similar lithologically and petrographically to the nondolomitized 

wackestones and packstones from the lower member of 

the Mississippian Turner Valley Formation of Alberta, 

Canada, described by Murray and Lucia (1967). Murray and Lucia believe these carbonate rock types are 

noncurrent deposits because of the presence of lime mud, 

numerous large bryozoan fronds, and articulated crinoid stems.

Ooid grainstones are present at various levels some 

250-400 feet below the top of section 620-31 (fig. 5). 

The coating on these particles is not well developed, 

and the ooids tend to be less than 500 microns in diameter. The carbonate rocks of these four sections are in 

general only slightly dolomitized: the foryozoan-echinoderm wackestone-packstone facies commonly has lime 

mud containing small amounts (1-15 percent) of floating dolomite rhombs which range in size from 40-150 

microns, but the only beds of dolomite known are in 

the upper 350 feet, of section 62C-31 (fig. 5).
CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

STRATIGRAPHY

SYSTEM

MISSISSIPPIAN

CO

u

E 

u

Upper Mississippian

o3 

|

GROUP

aujnqsn dnojg 

z

0

1-

cr 

0

L.

C 

0

"ro 

E 

o

LJ3

M 

O

E 

u_

o

3

D

Thickness, feet,m measured fromtop of ridge 

down

 -0-

100- 

200- 

300- 

400- 

500- 

600- 

700- 

800- 

900- 

1000-

1100-

1200- 

1300- 

1400- 

1500- 

1600- 

1700- 

1800-

1900- 

2000-

and microfacies Rocktype fromield observations 

thin-section andstudies

CM^,

S^fL^-L

\-« -1 -t

 'f'^ ^

^ ^ ^

 1 I

J- >.

^ i

~i «t

 1 V

-1 IV

*- t I' 1 J»

Jf -^ If

^^^

U * L L

^ I ^

^^t ' i ; ^ i *

1 ! 1

1 > - U

* \, 1 -<- 1

J 1 1-

s^^^t-

> i * i

i -vi .

^ i ,-.- i

-» i'i

 i -^ 1

-1 i i i

i Y i

^ !, ! [ f J

«' 1 -1 + *

| ^» t-| H ^

= ='='= =

Carbonate rock from types 

thin-section studies

wkst 

pkst

pkst 

wkst

_wkst 

pkst

pkst 

pkst

pkst 

pkst

wkst 

pkst

mdst

mdst

pkst 

gnst

pkst

gnst 

gnst

Photomicrographs of carrock bonate types.

fig. 1

^Pl- 13, 

fig 2

^Pl 13, 

fig 3

^PL 13, 

fig 4

^Pl. 13, 

fig 5

^Pl 13, 

fig 6

RUGOSE CORALS

2 > 2 "5

'S .s

3 ;

 

rotlonella Lithost banffensix 

(Warren)

Lithostrotionelln mdtiren 

(Sutherland)

^^

host Litionella birdirot 

Armstrong

^ 1

a

a.

0

1

cs 

-2

"5 M 

~ c

* 0

jl

a 

a at

a, 

p

-o

 

FIGURE 3. Carbonate stratigraphy and coral distribution, section 62C-15, USGS loc. M1019. Samples from this section have 

prefix 620-15.

R 20 W 163°W' R 19 W

10

0 it

62C-15

11 

1930 it

14'

FIGURE 4. Location of section 62C-15. Map base from U.S. 

Geological Survey, 1: 63,360, DeLong Mountains, A-2, A-3, 

1955.

Sedimentary structures which would indicate intertid'al and supratidal sedimentary facies, such as birdseye structures, stromatolites, chips, and mud cracks, 

were not found in any of the measured sections of the 

Kogruk Formation.

Within the four sections measured, no sedimentary 

features or microfacies indicative of carbonate deposition on bank slope to baisinal environments, such as 

those defined by McDaniel and Pray (1967, p. 474) and 

Wilson (1967a, p. 485, 486; 1969), were observed in the 

field or during petrographic studies of the Kokruk 

Formation.

Carbonate depositional cycles such as were described 

by Armstrong (1967) from the Mississippian of northern New Mexico or by Wilson (1967b) from the upper 

Pennsylvania!! Virgil Series of southern New Mexico 

or by Wilson (1967c) from the Upper Devonian Duperow Formation of western Canada appear to be. absent 

within the Kogruk Formation.

Field and laboratory studies of carbonate microf acies 

strongly suggest the Kogruk Formation was deposited 

in an open marine environment on a subsiding shelf on 

which carbonate deposition and subsidence were in near 

equilibrium. During deposition of the Kogruk Formation, only minor oscillations in environments of deposition are recorded in the 'sections studied.

Field studies and the petrographic examination of 

the suites of stratigraphic lithologic samples from each 

measured Kogruk Formation section clearly si ow the 

corals are most abundant in certain carbonate rock
ENVIRONMENTS OF DEPOSITION AND CARBONATE FACIE S

STRATIGRAPHY

SYSTEM

MISSISSIPPIAN

SERIES

c 

m

Upper Mississippi

GROUP

Q. 

O

0>

c

.Q

FORMATION

Kogruk Formation

Thickness, in feet, measured from oftp ridge 

down

0

100-

200-

300 

400- 

500-

600-

700-

800-

900-

1000- 

1100- 

1200-

1300-

1400-

1500-

1600-

1700- 

i Qnn

Rock and microfacies typ fromield observations and thin-section studies

Top of ridge, 

surface

 -" 4- .

' 4 * ^,

L ^* L L

^i I- 4- ^

1 ^ L * 1 « » | ^^ 

^x:

1 * L--4

 -M -

1 - 1 -M

,^«» *

? " ,' 1

i- . ,v | -^

^ ^ Dfl | «k

1 - 1 

I"P «r| V, 1-

^ 1 ^- K

J- 

 -* I v - l

r" ^ * L

- K 4 -

 t- - L L

 H , 1

«) ^ | i ^ |

, L i..«.

, L L v h

L- "'L- -^ I

 -4 [

L i>L 4 t-

- L J 1 -

1 * -t-

 1 ' -1 -

-I - 1 >f'

4 1 r 

-1 -t 1 L I.

1 IN 4 +

^ H , 1-

 - 1

l-i j

L -t -i-fc.

 * LV'-T

, 1 if L

^'^ »

» ^- L" 1 ^

^ ^ vn

r ^ ''v 1 ^

" [ , 

 l - l -

ir'l l 

| i. , -f

L . . 4 I

J.l - L ^ L

i L - I -

I L p* ^

^B 1 '

«UpJtof^-

^^^S1 ^ -t- ]^^f±

Carbonate rock types from 

studies thin-section 

dolo 

wkst

wkst 

gnst

dolo

gnst

dolo 

gnst

mdst 

wkst 

mdst 

wksf

wkst 

pkst

pkst 

pkst

wkst 

pkst

wkst 

wkst

pkst 

pkst

pkst

pkst

wksf 

"pRsF

mdst 

wkst

wkst

pkst 

_wkst_ 

wkst 

pkst

Photomicrographs of carbonate rock types

^Pl. 13 

fig 7

PI. 13, 

"fig. 8

^Pl 14, 

"fig 1

PI 14, 

"fig. 2

PI. 14,

RUGOSE CORALS

(Siphonoden- Lithostrotiuti dron) tinuogum (Kelly)

mm

m?m

mm

mm 

 

|l

mm

^M

mm

Lithnstriitiui/t'lla banffetiAifS 

(Warren)

Lithostrotionellit L. aff. 

banffensif! (Warren)

mm

LitkoRtrotiunella mclo reni

(Sutherland)

mm

mm

 2

mm

Th noph ylluastraei- ysn m

furme (Warren)

mm

Thy iiophyllu orientnie sit m

Thomson

mm

Scioph yll1 brtiumit HIa

Marker and Melaren

mm

Sciophyllu alaskuettsis m 

Armstrong

mm 

mm

D. 

D.

"a 

"a,

1

Talus slope 

Top of Utukok Formation 

believed to be 300-400 feet 

below base of measured section

FIGURE 5. Carbonate stratigraphy and coral distribution, section 62C-31, USGS 

loc. M1020. Samples from this section have prefix 62C-31.
6 CARBONATE FACIES AND CORALS, KOGRTTK FORMATION, BROOKS RANGE, ALASKA

FIGURE 6. Location of section 62C-31. Map base from U.S. 

Geological Survey 1: 250,000 DeLong Mountains, 1955.

types. The lithostrotionid corals are common in 

bryozoan-echinoderm packstones and ooid packstones 

adjacent to oolitic grainstone and well-sorted crinoid 

grainstone facies. These grainstones are interpreted to 

represent shoaling-water environments. A similar relationship was observed by Armstrong (1970) in the 

Mississippian Peratrovich Formation, Prince of Wales, 

Island, southeastern Alaska.

CHARACTERISTIC CARBONATE ROCK TYPES

MARINE LIME MUDSTONES TO ECHINODERMBRYOZOAN WACKESTONES

The lime mudstones (pi. 14, fig. 2) are typically composed of clotted pellets, which range in size from 50 to 

200 microns, and some pellets are more distinct and 

darker in color than others. Commonly present are 

larger size pellets or mud clasts which are generally 

ellipsoidal and which may contain fossil fragments. 

These larger pellets are interpreted as aggregates of 

muddy lime sediments whose exact mode of origin is 

uncertain. Wilson (1967io, p. 238) believes that small 

lithoclasts of this type in Devonian carbonates are derived from pieces of "previously deposited lime mud, 

partially lithified which were torn up and re-incorporated in the bottom sediments." Within the lime mudstones and wackestones, the dominant fossil fragments 

are echinoderm and bryozoan debris. Commonly present 

are fragments of Foraminifera, Ostracoda, and unidentified remains of sticklike or spicular organic fragments. 

Generally all fossil fragments are less than 1 mm in 

size. The fossil particles and pellets have undergone 

intense mixing and comminution, which probably indicates extensive burrowing of organisms into the 

sediments. The fauna of these rocks is considered representative of a marine environment of normal salinity.

FIGURE 7. Carbonate stratigraphy and coral distribution, section 

60A-400-403, USGS loc. M1021. Samples from this section 

have prefix 60A-400 to 60A-403.
CHARACTERICTIC CARBONATE ROCK TYPES

68°30' 

T 11 S

)Copter R 40 W I I P 39 W. 

Peak \ ^ '^ \

FIGURE 8. Location of section 60A-400 403. Map base from 

U.S. Geological Survey 1: 250,000, Misheguk Mountain, 1936.

STRATIGRAPHY

SYSTEM

MISSISSIPPIAN I 

SERIES

| i Upper Mississippian

GROUP

| Lisburne Group i

FORMATION

'| Kogruk Formation 1 

ckness, ifeet, measred bank cut on river 

I-

- - 0 

100-

200-

soa400-

500-

600-

700-

:k type and microfacles field observations om 

thin-section nd studies

cc

Covered 

slope

i,"1 v l-

-Th

1 J,

k

± -4 ,/

\i' f 1

Jf

i s- '-;

^ t 30

!' *. -i «P

1 ^

 -, 4-

± -^

rt f

 ^ i- 4 jf

1- ( f

 Jf. ^

-1

^ j- vn ^

^ ( n

r ' » -*-

t

^ V "~\

^ J

 i,--l

4 v

^ j1

'' ^

j 1

^ » ,?'

^ i

-i j.

Covered 

slope

bonate rck from types 

him-section studies

ro *" 

O

pkst

gnst T~ r

- 

pkst

pkst 

wkst

pkst

wkst 

pkst

pkst 

pkst

Dtomicrographs of carrock onate types

0.

PI. 14

fig./ 

^Pl. 14,

RUGOSE 

CORALS

hostrotionella mrln reni 

Sutherland)

3

 

Q.

in

 2 

£

^

 

Q.

a

at

& 

1

FIGURE 9. Carbonate stratigraphy and coral distribution, section 62C-34, USGS loc. M1022. 

Samples from this section have prefix 62O34.

FIGURE 10. Location of section 62C-34. Map base from U.S. 

Geological Survey 1: 63,360, Point Hope B-2, 1955.

ECHINODERM-BRYOZOAN WACKESTONES TO 

PACKSTONES

Echinoderm-bryozo'an wackestones to packstones are 

the most abundant rock types within the measured sections of the Kogruk Formation (pi. 13, figs. 1-4, 8; pi. 

14, figs. 1, 3-5). The majority of the fossils are broken 

and abraded fragments of crinoids and bryozoans, but 

there are lesser amounts of brachiopods, foraminifers, 

ostracodes, and calcareous algae. Dolomite makes up 

typically 1-15 percent of the rock. It occurs as scattered 

rhombs, ranging in size from 40 to 150 microns, within 

the lime mud or as rhombs impinging on larger crinoid 

fragments. These rocks are believed to be low-energy, 

possibly noil-current-deposited, open marine sediments.

OOID TO OOLITIC GRAINSTONES

The ooid grainstones (pi. 13, figs. 6, 7) are composed 

of rounded fossil fragments, which are generally less 

than 500 microns in size, and these fragments typically 

have one layer of oolitic coating. The fragments are 

broken skeletal remains of bryozoans, ecliinoderms, 

ostracodes, foraminifers, and calcispheres. Pellets of 

lime mudstone with oolitic coating are common. This 

carbonate rock type is only a small percentage of a Irogruk Formation section. These rocks are interpreted as 

shoaling-water sediments.
CARBONATE FACIES AND CORALS, KOGRTJK FORMATION, BROOKS RANGE, ALASKA

ECHINODERM-BRYOZOAN GRAINSTONES

The echinoderm-bryozoan grainstones fonn a relatively small percentage of the carbonates in the Kogruk 

Formation (pi. 13, fig. 5; pi. 14, fig. 7). The grainstones 

are composed of rather large, relatively poorly sorted 

angular fragments of crinoids, varying amounts of 

bryozoan fragments, and lesser amounts of calcareous 

algae and brachiopods. These grainstones are believed 

to be current-deposited sediments of shoaling-water or 

tidal-channel environments.

CALCITIC DOLOMITES AND DOLOMITES

Dolomites are relatively rare within the four measured 

sections of the Kogruk Formation. The only thick unit 

of dolomite found was the highest 100 feet of section 

62C-31 (fig. 5). Here the dolomite is typically composed 

of 60-100 percent dolomite rhombs 150-200 microns in 

size, less than 5 percent silt-size rounded quartz grains, 

and 0-40 percent residual unaltered lime mud and 

crinoid fragments. The dolomites were originally lime 

mudstones and crinoid wackestones. In all samples 

studied, the crinoid fragments are still calcite, but dolomite crystals impinge on the outside of the crinoid 

fragments.

AGE AND CORRELATION OF THE 

LITHOSTROTIONID CORAL FAUNAS

Coral zonation of thick Mississippian carbonate sections has been used in the northern Cordilleran region 

of the United States by Parks (1951), Saiido and Dutro 

(1960), Dutro and Sando (1963a, b), Sando (1967a, 

b), and Sando, Mamet and Dutro (1969). In the Cordilleran region of western Canada, Sutherland (1958), 

Nelson (1960, 1961), and Macqueen and Bamber (1967, 

1968) have utilized rugose corals for zonation and correlation of thick Mississippian carbonate sequences.

Detailed collecting from the three thicker sections of 

the Kogruk Formation in the DeLong Mountains indicates that fasciculate lithostrotionids are apparently 

absent in the lower 200-600 feet of the Kogruk Formation and that cerioicl lithostrotionids are absent from 

the lower 400-800 feet of these sections (figs. 3, 5, 7). 

Dutro (in Sable and Dutro, 1961, p. 592) states that 

fossil brachiopods in the lower part of the Kogruk Formation indicate an Early Mississippian (probable 

Osage) age in some places.

At a stratigraphic level about 1,800 feet below the top 

of section 62C-31 (fig. 5) and 900 feet below the top 

section 62C-15 (fig. 3), the first lithostrotionid corals 

were found. The fauna consists of Lithostrotion (Siphonodendron} slnuosunn (Kelly),Z. (8.} warreni Nelson, 

LithosfrotioneHa mclareni (Sutherland), Lithostrotionella. aff. Z. 'banffemis (Warren), Thysanophyllutn 

astraeiforme (Warren), Thysanophylluni or'entale 

Thomson, and Sciophylhun lanibarti Harker and 

McLaren.

The writer has collected from Bowsher and Dutro's 

(1957) type section of the Alapah Limestone (shaly 

limestone and dark limestone member) at Shainin Lake 

the following species: Lithostrotion (Siphonodendron} 

simwswm (Kelly), L. (8.) warreni Nelson, Lithostrotionella. mclareni (Sutherland), and Thysanophyllum 

axtraei forme (Warren).

The lower lithostrotionid coral fauna of the Kogruk 

Formation appears to be Meramec in age in the measured sections of this report and is possibly equivalent to 

the lower part of the Alapah Limestone, Lisburne 

Group, at Shainin Lake, Endicott Mountains, central 

Brooks Range.

This fauna may be in part equivalent to assemblage 

2 of Macqueen and Bamber s (1968, p. 261-264, figs. 7, 

8) from the Mount Head Formation of southwestern 

Alberta.

The youngest lithostrotionid coral fauna, found in 

the higher 600-800 feet of the Kogruk Formation, also 

contains elements of the lower fauna, Lithostrotionella 

melareni (Sutherland) and Thysanophyllwn orientale 

Thomson, but is characterized by the species Lithostrotionella birdi Armstrong, L. banffen-sls (Warren], L. 

sp. A, L. sp. B, and Sdophyllum, alaskaensis Armstrong. This fauna is found in association with the O _

solitary coral Faberophyllum- spp. Above the Fdberophyllum spp. are found Thysanophyllwn orientals 

Thomson and Lithostrotionella birdi Armstrong in association with latest Meramec age Foraminifera (B. L. 

Mamet, oral cominun., December 1969).

Armstrong (1970) reports Lithostrotwnella birdi 

Armstrong, L. aff. L. wiclareni (Sutherland), L. banffensis (Warren). Sdophyllum, alaskaemis Armstrong, 

and Faberophyttum girtyi Armstrong, and a. large 

fauna of microfossils of late Meramec age from the 

upper beds of the limestone and chert member, Peratrovich Formation, northwest coast of Prince of Wales 

Island, southeastern Alaska.

Nelson (1960,1961) reports Thysanophyllum astraeifonne. (Warren), Lithostrotionella banffensis (Warren), Lithostrotion (Siphonodendron) warreni Nelson, 

Z. (S.) sinuosum (Kelly), and FaberophyHum leathemanense Parks from the Mount Head Formation of 

British Columbia.

The younger Kogruk Formation coral fauna is probably equivalent to assemblage 3 of Macqueen and Bamber's (1968, p. 259-266, figs. 7, 8) from the Mount Head 

Formation of southwestern Alberta. The common 

species there are Thysanophylhini astraeiforme (War-
SYSTEMATIC PALEONTOLOGY 9

ren), possibly Lithostrotionella mdareni (Sutherland), 

and Faberophytfwn spp.

In southeastern Idaho, Dutro and Sando (1963a, p. 

B94, fig. 23.2; 1963b, p. 1974) found Fdberophyllum 

in the Chesterfield Range Group in their f aunal zone F. 

They stated that "Fnberophyllum-rich. strata are common throughout the Great Basin region in the Great 

Blue Limestone and correlative stratigraphic units. 

They are present also in the upper Mount Head Formation of western Canada. Zone F is certainly of Meramec 

age, in part, but may include correlatives of the lower 

Chester as well."

The youngest lithostrotionid coral fauna of the 

Kogruk Formation is believed to be late Meramec in age.

More recent work by Sando, Mamet, and Dutro 

(1969) indicates that the top of the FaberopJiyllum 

zone coincides with the top of the Meramec Series (W. 

J. Sando, written commun., 1969) and that the zone is 

exclusively late Meramec.

The Kogruk lithostrotionid coral fauna has many 

species which occur in the coral fauna from the upper 

part of the limestone and chert member of the Peratrovich Formation, on Prince of Wales Island, southeastern 

Alaska, and from the Mount Head Formation of British 

Columbia and Alberta, Canada. Significant aspects of 

these, two boreal faunas are apparently absent from the 

arctic Kogruk faunas. LithostrotioneWa pennsylraniea 

(Shinier), a common element to these boreal faunas, has 

not been found in the Kogruk Formation. Furthermore, 

fasciculate acolumellate corals have not been found as 

yet by the writer in the Kogruk Formation of the DeLong Mountains. Diphyphyllum. aff. D. M-airockensis 

Armstrong is abundant in latest Meramec and earliest 

Chester carbonates of the Lisburne Group in the Cape 

Lewis, Niak Creek sections, northwestern Alaska. It is 

also found in the Lisburne Group outcrops near the 

headwaters of the Hulahula River. Romanzof Mountains, northeastern Alaska, The Peratrovich Formation 

has two species of DiphyphyHum, D. Mairockensis Armstrong and DiphyphyUum venosum Armstrong. E. W. 

Bamber (oral commun., 1967) has found corals which 

possibly belong to the genus DipJiyphyflum to be rather 

common in the Mount Head Formation.

SYSTEMATIC PALEONTOLOGY

In the systematic study of this coral fauna, no new 

species are described. Most species in this collection are 

represented by only a few specimens from a given horizon in any one section. Oliver (1968, p. 27) considers 

that for Paleozoic corals, samples of 20 corallites adequately characterize a corallum and that a sample of 

20 coralla may be a representative sample of a local

population from one environment over a limited area. 

Collections of this nature were not available from the 

Kogruk Formation.

Morphological terminology follows that of Hill 

(1956, p. 34-251).

Conventional treatment has been followed in the taxonomic hierarchy above of the species level. The classification is generally that of Hill (1956), but there are some 

minor changes. The terminology of the microstruct'ire 

. is that of Kato (1963).

Phylum COELENTERATA

Class ANTHOZOA

Order RUGOSA Milne-Edwards and Haime, 1850 

Family LITHOSTROTIONIDAE d'Orbigny, 1851

Genus LITHOSTROTION Fleming, 1828 

LitJiostrotion Fleming, 1828, A history of British Animals,

Edinburgh, p. 508.

LitJiostrotion Fleming. Hill, 1956, in Moore, R. C., ed., Treatise 

on invertebrate paleontology, Part F, Geol. Soc. America, 

p. F282.

Type species. (Opinion 117, International Commission of Zoological Nomenclature) LitJiostrotion striaturn Fleming. Lower Carboniferous, British Isles.

For detailed synonymy of the genus see Hill (1940, 

p. 165-166; 1956, p. F282).

Diagnosis. Phaceloid or cerioid; typically with 

columella, long major septa, and large conical tabulae, 

generally supplemented by outer, smaller, nearly horizontal tabulae; dissepiments absent in very small forr^is, 

normal and well developed in large f orms; increase nonparricidal; diphymorphs common (Hill, 1956, p. F282).

Submenus SIPHONODENDRON McCoy, 1849 

SipJionodendron. McCoy, 1849, Annals and Mag. Nat. History,

p. 127. 

Siphonodendron McCoy. Sando, 1963, Jour. Paleontology, v. 37,

no. 5, p. 1075.

Type species. LitJiostrotion pmiciradialis (McCoy), 

Carboniferous, Ireland.

Diagnosis. Same internal features as LitJiostrotian 

except the growth form of the corallum is fasciculate. 

Lithostrotion (Siphonodendron) sinuosum (Kelly)

Plate 1, figures 1-7; plate 3, figures 3, 4

Lithostrotian flexuosuni Warren, 1927, Canada Geol. Surrey 

Bull. 42, p. 47-48, pi. 3, fig. 7, pi. 4, fig. 2. [Not, LitJiostrotion 

flexuosum Trautschold, 1879, p. 37, pi. 5, figs. 7a-b.]

Diphyphyllum sinuosum Kelly, 1942, Jour. Paleontology, v. 16, 

p. 358.

LitJiostrotion cf. pauciradiale (McCoy). Sutherland, 1958, Canada Geol. Survey Mem. 295, p. 92-93, pi. 32, figs. 1, 2, 3a, c.

Lithostrotion sinuosum (Kelly). Nelson, 1960, Jour. Paleortology, v. 34, p. 121, pi. 24, figs. 4-10.

LitJiostrotion sinuosum (Kelly). Nelson, 1961, Geol. Assoc. Canada Spec. Paper 2, pi. 11, figs. 1-7.

Lithostrotion (SipJionodendron) sinuosum (Kelly), Bamber, 

1966, Canada Geol. Survey Bull. 135, p. 7, 8, pi. 1, figs. 3, 4<*-i.
10 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

Litliostrotion (Siphonoilendron) sinuosum (Kelly). Bamber. 

1967, Canada Geol. Survey Paper 67-47, pi. 1, figs, lla-c, 

12a, b.

Material. Fragments of nine colonies, each fragment 

of which was about 8 by 8 by 10 cm, were available for 

study. Specimen USNM 160988 was studied in five 

transverse and three longitudinal thin sections. Typically five transverse and three longitudinal thin sections 

were made from each corallum.

Description. The specimen USNM 160989 (pi. 1, 

figs. 1, 2) from the measured section 62C-15, DeLong 

Mountains, has a dendroid fasciculate corallum and offsets that arise by lateral increase. In transverse thin 

section the corallites are 0.5 4 mm apart, and they are 

2.7-3.7 mm in diameter and have 16-18 major septa 

(figs. 11, 12). The major septa are 0.7-1.2 mm long and 

in some corallites reach the columella. This latter condition is noted in random thin sections which transact 

some corallites at a level at which the major septa reach 

the columella on the surface of tabulae. The minor septa 

are always present and are short, 0.3-0.5 mm long. The 

epitheca is 80-100 microns thick. The major septa at 

their bases are 150-180 microns thick and taper to their 

distal ends. The original microstructure of the corallum 

has been extensively affected by calcite neomorphism 

(Folk 1965) (pi. 3, figs. 3, -1). The epitheca appears to 

have been composed of calcite crystals that have their 

long axes perpendicular to the exterior. The septa are 

composed of 8-15-micron calcite crystals. The columella 

is lens shaped, 0.35-0.5 mm wide and 0.5-0.8 mm long, 

and has short, projections which are ridges made by the 

axial edges of septa on the surface of the upsloping 

tabulae. The columella has a median plate about 50 

microns thick which is in the plane of the cardinalcounter septa. The composition of the columella is interlocking crystals of calcite, ranging from 8-15 microns 

in size, and the columella appears to have the same 

microstructure as the septa.

In longitudinal section, the tabulae are generally 

complete and slope away from the columella for a distance of approximately 1 mm at angle of 20°-25° before 

bending downward to angles of 45°-60° near the dissepimentarium. Some 9-12 tabulae occur in a distance 

of 5 mm. The dissepimentarium is composed of a single 

row of globose dissepiments of which 12-16 occur in 

5 mm. The walls of the tabulae and dissepiments are 

20-30 microns thick and are formed by crystals of calcite which range in size from 8 to 15 microns. Microscopic examination of the junction of tabulae to the 

columella clearly indicates the tabulae do not contribute 

to the structure of the columella.

Occurrence. Specimen USNM 160989, described in 

detail above, and specimen USNM 160988 (pi. 1, figs.

3-5) were collected at 690 and 620 feet respectively 

below the top of measured section 62C-15, Kogruk Formation, DeLong Mountains. They were found in association with Lithostrotio-nella banff&mis (Warr?n), L. 

mclareni (Sutherland), and Faberoplvyllum spp. (fig. 

3). Specimens USNM 160982 and 160983 were collected 

by the writer in 1962 from the lower half of Campbell's 

(1967, p. 49) Cape Thompson Member of the Nasorak 

Formation, south of Nasorak Creek, near Cape Thompson. Other corals from the same bed are Litliostrotion 

(Siphonodendron) wa.rreni Nelson, Thysanophyllum 

axtraei.forme (Warren), and Sciophyllum sp. A. 

Litliostrotion (8.) sinuosum (Kelly), USNM 161032, 

was collected from 30 feet above the base of th?. Cape 

Thompson Member of the Nasorak Formation, r,t Cape 

Thompson (Campbell, 1967, pi. 2A). From measured 

section 62C-31 (fig. 5), Kogruk Formation, DeLong 

Mountains, the following specimens of Z. (&'.) sinuosum 

(Kelly) were collected at the indicated level below the 

top of the section: USNM 160987 at 870 feet (pi. 1, figs. 

6,7), USNM 160985 at 1,490 feet, USNM 161014 at 1,790 

feet, and USNM 160986 at 1,810 feet. The specimens 

occur with Lithostrotion (Siphonodendron] warreni 

Nelson, Sciophyllum lamb art i Harker and McLaren, 

and Lithostrotionella aff. L. banffensis (Warren).

Z. (S.) sinuosum (Kelly), USNM 160998, was found 

in association with Lithostrotio>nella. mclareni (Sutherland) in section 60A tOO 103, Kogruk Formation in 

the DeLong Mountains (fig. 7).

Bamber (1966, p. 7) states that Lithostrotion (8iphanodendron^) sinuosum (Kelly) is found in the 

Prophet Formation north of the Peace River in British 

Columbia and in the upper 400 feet of the Livingstone 

Formation and the basal Mount Head Formation, 

Rocky Mountains of southern British Columbia and 

Alberta.

Macqueen and Bamber (1967, p. 12, figs. 7, 8) found 

that Z. (S.) sinuosum. in the Mississippian rocks of 

southwestern Alberta ranges from Osage into Meramec 

age rocks, through most of the Livingstone Formation 

and into the overlying Mount Head Formation. In 

Alberta it normally occurs below the lithostrotionid 

species it is found associated with in the Kogruk Formation of Alaska.

Rem-arks. The coralla, assigned to the species Lithostrotion (Siphonodendron) sinuosum (Kelly) from 

the Lisburne Group of northwestern Alaska, rgree in 

corallite diameter, number, and development of septa, 

tabulae, dissepiments, and columella with ?Telson's 

(1960, pi. 24, figs. 4-10) illustration of the holotype 

from the basal Mount Head Formation and with 

Bamber's (1966, pi. 1, figs. 3,4a-i) illustrations of a syntype and a hypotype. Specimen USNM 160986 was col-
SYSTEMATIC PALEONTOLOGY

4

11

EXPLANATION

Q60A-402+10; USNM 160998

 60A-429 + 70; USNM 160982

 60A-429 + 80A; USNM 160983

A

13 14 15 16 17 

NUMBER OF MAJOR SEPTA

18

EXPLANATION

 62C-31 + 1810; USNM 160986

 62C-31 + 1490; USNM 160985 

o 62C-45 + 530; USNM 161032

c

15 16 17 18

NUMBER OF MAJOR SEPTA

378-461 O 70 3

19

Q 1

T I

EXPLANATION

 62C-15+690; USNM 160989

 62C-15+620; USNM 160988 

o 62C-31+870; USNM 160987

B

12 13 14 15 16 17 18 

NUMBER OF MAJOR SEPTA

19 20

FIGURE 11. Corallite diameter and number of major septa in 

Lithostrotion (Siphonodendron) sinuosum (Kelly). Eac1! unnumbered sym'bol represents a single corallite. If more than 

one corallite shows the same diameter and number of septa, 

the number of similar eorallites is shown.

lected from a bed at a level approximately 300-500 feet 

above the base of the Kogruk Formation in the DeLong 

Mountains in section 62C-31 (fig. 5). This specimen 

differs from the stratigraphically higher Kogruk examples of the species because its corallites have irajor 

septa which are 0.2-0.3 mm shorter and because they 

have thin columellae. These differences are not considered to be of specific or subspecific significance. L. ($.) 

sinuosum (Kelly), specimen USNM 160987, collected 

870 feet below the top of section 62C-31, at about the 

middle of the Kogruk Formation, is characterizei by 

longer major septa which generally join the colunella 

intransverse section. Other specimens, which have long 

major septa, were collected in stratigraphically younger 

beds of the Kogruk Formation at section 62C-15 and 

section 62C-31.

The Kogruk Formation specimens of L. (S.) sinuosum (Kelly) suggest a trend in this species towards 

septal elongation and thicker columellae in stratigraphically younger coralla.

Specimen USNM 160997, Lithostrotion (Siphoncdendron) aff. L. (8.) sinuosuvn (Kelly) (pi. 1, fig. 8; pi. 3, 

figs. 1,2), is the stratigraphically lowest specimen of the 

subgenus in this collection from the Lisbume Group, 

DeLong Mountains. It was collected by Dr. Sigmund 

Snelson 540 feet below the top of the Utukok Formation. 

It differs from typical examples of L. (/&'.) sinuosum by
12 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

FIGURE 12. Sections of LitJiostrotion (RipJwnodendron) sinuosum (Kelly), USNM 160989.

having corallites in which the minor septa are usually 

absent and in which the major septa are short and are 

withdrawn from the axial region.

Lithostrotion (Siphonodendron) oculimum Saiido 

(1963) is readily distinguished from L. (8.} sinuoswni 

(Kelly) by its larger corallites; they range in diameter 

from 4 to 6 mm and have 20 to 25 major septa. Another 

distinguishing feature is its tabulae, which near the 

periphery of the tabularium are reflexed downward 

about 50°-70° and then are reflexed to nearly horizontal 

just before they contact the dissepimentarium.

Morphologically similar in some respects to L. (8.} 

sinuosum. (Kelly) from the Lisburne Group is Dobroljubova's (1958, p. 153-155, pi. 22, figs, la, b, 2a, b) Lithostrotion volkovae Dobroljubova from the lower Carboniferous of the Russian Platform. Its corallites have 

a diameter of 4-5 mm; they have 17-18 long major septa 

and well-developed columelae. The minor septa are 

about one-third the length of the major septa. It differs from L. (S.} sinuosum (Kelly) by having tabulae 

which tend to be incomplete and a well-developed double 

to triple row of dissepiments.

The lectotype of Lithostrotion paucimdiale (McCoy), 

chosen by Hill (1940, p. 169, pi. 9, figs. 1, 2) specimens 

at the National Museum of Ireland, has 18-22 major 

septa per corallite and a corallite diameter of 4-5.5 mm. 

The species has a slightly larger corallite diameter, a 

higher number of septa, and a more pronounced tendency towards incomplete tabulae than does L. (S.} 

sinuosum (Kelly).

Yii's (1933, pi. 19, figs. 4, 4a-d; pi. 20, figs. 1, la-c) 

illustration of Lithostrotion. (8'i.pho-nodendron) irregidare (Phillips) var. aniatica Yabe and Hayasaka 

from China shows specimens which closely resemble

some specimens of L. (S.) sinuosum (Kelly) fr:nn the 

Kogruk Formation, in particular USNM 160987, from, 

the middle of the formation, section 62C-31.

Lithostrotion (Siphonodendron) aff. L. (S.) sinuosum (Felly)

Plate 1, figure 8; plate 3, figures 1, 2

Material. A fragment approximately 8 by 10 by 15 

cm of a corallum was collected. The corallum is preserved as calcite in a partially dolomitized arenaceous 

crinoidal wackestone. Two transverse and three longitudinal thin sections were available for study. Transverse sections of 65 corallites were studied.

Description. The specimen, USNM 160997, has a 

fasciculate corallum and offsets that arise by lateral increase. In transverse thin section, corallites are 0.5-7 mm 

apart, are 3-4.5 mm in diameter, and have 15-lf major 

septa (figs. 13,14). The major septa are 0.7-1.3 mm. long 

and in the thin section studied do not reach the columella (pi. 1, fig. 8; pi. 3, fig. 2). In most of the corallites, 

minor septa are absent, but where present they are less 

than 0.1 mm long. The calcite of the internal strictures 

has been recrystallized, and most of the original microstructure has been destroyed. The interiors of the corallites are filled with sparry calcite, and the columella 

has been extensively recry&tallized (pi. 3, figs 1, 2). 

The epitheca is 90-100 microns thick, and the major 

septa 'at their bases are 70-100 microns thick. T1XQ, columella is lens shaped, 0.5-0.7 mm long and 0.1-0.2 mm 

wide.

In this section all longitudinal sections of corallites 

are crushed and distorted (pi. 4, fig. 2). Reconstruction 

of individual corallites suggests they had complete

14 15 16 17 

NUMBER OF MAJOR SEPTA

18 19

FIGURE 13. Corallite diameter and number of major septa in 

Lithostrotion (Siphonodendron) aff. L. (8.) sinuosum 

(Kelly). Each unnumbered symbol represents a single corallite. If more than one corallite shows the same diameter and 

number of septa, the number of similar corallites if shown. 

Specimens from section 60A-303+410; USNM 160997.
SYSTEMATIC PALEONTOLOGY 13

FIGURE 14. Section of Lithostrotion (Siphonodendron) aff. 

L. <»SY .) sinuosum (Kelly), USNM 160997.

tabulae which sloped 15°-25° away from the columella 

for a distance of approximately 1 mm before bending 

downward to angles of 40 C -50° near the dissepimentarium. In a distance of 5 mm, there are 5-8 tabulae. The 

globose dissepiments are not persistent and occur as a 

discontinuous single row in which 8-10 dissepiments are 

present in 5 mm.

Occurrence. Specimen USNM 160997 was collected 

by Dr. Sigmund Snelson about 540 feet below the top of 

the Utukok Formation at the headwaters of Nunaviksok 

Creek, sec. 36, T. 10 S., R. 41 W. This specimen is the 

stratigraphicially lowest example of the sufogenus Siphonodendron collected by Shell Oil Co. geologists from 

the Lisburne Group, DeLong Mountains.

Remarks. L.(8.} aff. L. (8.) sinuosum (Kelly) differs from L. (8.} sinuosum. (Kelly) by having corallites in which the minor septa may be absent or only 

weakly developed, the major septa are withdrawn from 

the axial region, and the dissepiments are not continuous in the corallites. (See remarks under L. (8.} sinuosum.} Kelly (1942, p. 358) describes the holotype of the 

Lower Mississippian species of Lithostrotion (Siphonodendron)mutabile (Kelly) as having corallites with a 

diameter of 4.0-6.5 mm and 24 major septa and long 

minor septa. In transverse section this species differs 

from L. (3.) aff. L. (/S.) sinuosum (Kelly) by having 

larger corallites and more numerous and much longer 

minor septa.

Lithostrotion (Siphonodendron) warreni Nelson 

Plate 1, figures 9,10; Plate 2, figures 1-4

Lithostrotion (DiphyphyUitm) sp. A. Sutherland, 1958, Canada 

Geol. Survey Mem. 295, p. 98, pi. 32, figs. 4a-d.

Lithostrotion warreni Nelson, I960, Jour. Paleontology, v. 34,

p. 121,122, pi. 24, figs. 11-14. 

Lithostrotion ivarreni Nelson, Nelson, 1961, Geol. Assoc. Canada

Spec. Paper 2, pi. 13, figs. 4-8. 

Lithostrotion (Siphonodendron) warreni Nelsion, Bamber, 1966,

Canada Geol. Survey Bull. 135, pi. 1, fig. 2. 

Llthostro'tion (Siphonodendron) warreni Nelson, Armstrong,

1970, U.S. Geol. Survey Prof. Paper 534, p. 18-20, p1 . 4,

figs. 1-6.

Material. Fragments of four colonies were collected 

from measured stratigraphic sections. The specimens 

are typically 8 by 8 by 10 cm and are preserved as calcite 

in a matrix of limestone or dolomitic limestone. Four 

transverse and two longitudinal thin sections were made 

of each colony.

Description. Specimen USNM 160990 (pi. 2, figs. 1, 

2), from measured section 62C-31 in the DeLong Mountains, has a dendroid corallum and offsets that arise- by 

lateral increase. In transverse thin section, corallites 

are 0.5-5 mm apart and are 4.0-5.5 mm in diameter; 

they hiave 21-23 major septa (figs. 15, 16). The mr.jor

C/)

LJ 6

,- 4

< 3

Q

EXPLANATION

 62C-45 + 510, USNM 161033

 62C-31 + 1310, USNM 160990 

O 62C-31 + 1425. USNM 160991 

A60A-429+10; USNM 160993

18 19 20 21 22 23

NUMBER OF MAJOR SEPTA

24 25

FIGUEE 15. Corallite diameter and number of major septr in 

Lithostrotion (Siphonodendron) warreni Nelson.

FIGURE 16. Sections of Lithostrotion (Siphonodendron) war 

rent Nelson; A, USNM 160993; B, C, D, USNM 160990.
14 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

septa are 0.8-1.3 mm long; the minor septa are 0.3-0.4 

mm long. The major septa at their bases are 70-100 

microns thick, and the epitheca appears to be in excess 

of 100 microns thick. The epitheca and septa, along with 

all internal structures, have undergone calcite neomorphism and are composed of interlocking calcite crystals 

ranging in size from 20 to 80 microns (pi. 1, fig. 10). 

The columella is elongated in the plane of the cardinalcounter septa. The septa, in the thin section studied, 

generally do not reach the columella. The columellae 

range in size from 0.5 to 1 mm long and 0.1 to 0.2 mm 

wide and generally have short radiating projections 

formed by the septa wT hich are low ridges on the surface 

of the upsloping tabulae.

A median plate, 20-40 microns thick, is present in the 

columella and is preserved as a dark-colored band (pi. 

1, fig. 10).

In longitudinal section (pi. 1, fig. 9; pi. 2, fig. 2) the 

tabulae are complete and slope peripherally from the 

columella at angles of 25°-35° in the axial region, then 

are deflected downward 50°-65° near the periphery of 

the tabularium. A few tabulae near the periphery of 

the tabularium are reflexed to a near-horizontal plane, 

but the vast majority of tabulae join the dissepimentarium at angles of 50°-65°. The tabulae are 50-70 microns 

thick. In a distance of 5 mm there are 5-7 tabulae. The 

columella (pi. 1, fig. 9) is a continuous, straight -axial 

plate to which the tabulae are fused, but the tabulae do 

not 'contribute to its structure.

In all corallites studies the dissepimentarium is present and is a single row of regular dissepiments of 

relatively uniform globose shape; the dissepiments are 

typically 0.5 mm long and 0.2-0.3 mm wide and have a 

wall that is 20-30 microns thick.

Occurrence. Specimens USNM 160990 and 160991 

were collected in the Kogruk Formation at 1,310 and 

1,425 feet below the top of measured section 62C-31, 

DeLong Mountains, in association with a coral fauna of 

Lithostrotion (Siphonodendron} sinuos-wn (Kelly), 

Thysanophyll/um. astraeifornw (Warren), T. orientate 

Thomson, 8ciophyllwn lambarti Harker and McLaren, 

8. alaskaemsix Armstrong, Lithostrotionella aff. L. banffensis (Warren), and L. mclareni (Sutherland) (fig. 5).

Specimen USNM 160993 (pi. 2, figs. 3,4) was collected 

in association with Thysanophyllum astraeiforme 

(Warren) and Sciophylhim sp. A. in the lower half of 

the Cape Thompson Member (Campbell, 1967, p. 49, 

pi. 2B) of the Nasorak Formation south of Nasorak 

Creek, near Cape Thompson.

L. (8.)icarreni Nelson USNM 161033, was collected 

10 feet above the base of the Cape Thompson Member 

of the Nasorak Formation at Cape Thompson.

L. (xS'.) ivttrrenl Nelson has been found in the Jower 20

feet of Bowsher and Dutro's (1957) dark limestone 

member of the Alapah Formation, Lisburne Group, at 

Shainin Lake. It occurs here with a large fauna of 

Meramec lithostrotionid corals and Foraminifc^a.

Armstrong (1970, p. 19) reports L. (S.) warreni 

Nelson with Lithostrotionella birdi Armstrong, L. 

pennsylvanica (Shinier), and a Foraminiferr, microfauna of Meramec age from the limestone and chert 

member of the Peratrovich Formation, northwest coast, 

Prince of Wales Island, Alaska.

Nelson (1960, p. 121) reports L. (8.) warreni Nelson 

in Alberta from the "Lower Mount Head Formation, 

ranging from the lower to upper Lithoxtrotionella beds."

Macqueen and Bamber (1968, p. 261-262) found Z. 

(8.} warreni Nelson in their Meramec age faunal assemblages 1 and 2 from the Mount Head Foriration of 

southwestern Alberta.

Remarks. Lithostrotion, (Siphonodendron ) warreni 

Nelson (1960, p. 121-122, pi. 24, figs. 11-14) from the 

lower Mount Head Formation, Alberta, arid Lithostrotion, (Siphonodendrori) 0cw7mwm, Sando (1963, p.1075- 

1076, pi. 145, figs. 1-5) from the Red wall Limestone, 

Arizona, are similar in diameter of the corallites, the 

number of major septa, and development of the columellae. They differ, however, in that L. (8.) cculinum, 

Sando has slightly longer minor septa and in particular 

has, in longitudinal section, tabulae that are sharply 

deflected downward near the periphery of the tabularium but that are bent to nearly a horizontal plane adjacent to the dissepimentarium. Furthermore, in L. ($.) 

ocuUnum, Sando (p. 1075) rare tabulae are so sharply 

deflected at the tabular shoulder that they rest upon the 

underlying tabulae. In contrast, the tabularium of L. 

(8.) warreni Nelson has tabulae which are generally 

flatter and lack well-defined shoulders.

In the transverse sections the specimens of L. (8.) 

warreni Nelson from the Kogruk Formation compare 

closely with Bamber's (1966, pi. 1, fig. 2) illustration of 

a transverse section of the holotype. Some parts of an 

individual corallite within one colony may shew a few 

tabulae whose configuration is suggestive of some of the 

characteristics of L. (S.) ociilinum Sando. But among 

all the Kogruk Formation specimens, not one corallite 

or any one colony has well-developed or consistent characteristics typical of L. (8.) ocidimimS&ndo.

Lithostrotion, (SipJi onodendron) sp. A, which occurs 

in the Lisburne Group in the same beds as L. (8.) 

warreni, can be distinguished from the latter by its 

tabulae which slope peripherally from the columella to 

the dissepimentarium at angle 50°-65°.

Lithostrotion (Siphonodendron) sinuosum (Kelly), 

which also occurs in the Lisburne Group with L. (8.) 

warreni. differs from the latter by having corallites with
SYSTEMATIC PALEONTOLOGY 15

a diameter of only 3-4.5 mm and longer major septa 

that may extend across the tabularium and join with 

the columella.

Lithostrotion (Siphonodendron) oregonensis Merriam (1942, p. 379, pi. 57, figs. 1-8), from the Mississippian Coffee Creek Formation of Oregon, is closely related to and has a corallite diameter similar to Z. (S.) 

waweni. L. (S.) oregonensis differs by having 17-20 

major septa which are always thickened in the dissepimentarium and tabulae that are commonly discontinuous.

Lithostrotion (Siphonodendron) sp. A 

Plate 2, figures 5-9

Material. Specimen USNM 160992 was collected 

from a measured section of the Nasorak Formation at 

Cape Thompson. Specimen USNM 160996 was collected 

from the dark limestone member of the Alapah Limestone at Shainin Lake, central Brooks Eange. Both 

specimens are fragments about 6 cm square and contain 

coralla which are preserved as calcite in a limestone 

matrix. Two transverse and three longitudinal thin 

sections have been made from specimen USNM 160992. 

Approximately 62 corallites were studied in transverse 

section, and 25 in longitudinal section. The specimen 

from the Shainin Lake section, USNM 160996, was 

studied in one longitudinal and three transverse thin 

sections; 72 corallites in the transverse sections, and 10 

in the longitudinal section.

Description. Specimen USNM 160992 (pi. 2, figs. 

5-9) from the type locality of the Cape Thompson 

Member of the Nasorak Formation has a dendroid coral - 

lum and offsets that arise by lateral increase. In 

transverse thin section, corallites are 0.5-6 mm apart 

and have a diameter of 3 1.5 mm; they have 20-26 major 

septa, which are 0.7-1.0 mm long and which are 100 

microns thick at their bases (figs. 17, 18). Minor septa 

are always present and are 0.3-0.4 mm long. The epitheca is 50-70 microns thick. The colmnellae are lens 

shaped, 0.7-1.2 mm long, 0.3-0.5 mm wide, and in some 

corallites are attached to the counter septum. The major 

septa extend to the columella as low ridges on the surfaces of the tabulae. A few corallites were cut on the 

plane at which the tabulae joined the columella.

In longitudinal section, the tabularium is well defined 

and regular. The tabulae (pi. 2, figs. 5-8) slope downward from the columella at angles of 50°-65° across the 

tabularium to join the dissepimentarium. Some tabulae are reflexed to slopes of 20°-30° before reaching 

the dissepimentarium. There are 5-6 tabulae in 5 mm. 

In all corallites studied, the dissepimentarium is present 

and is a single row of uniform globose-shaped dissepiments, 0.4-0.6 mm long, 0.2-0.3 mm wide. The walls of 

both dissepiments and tabulae are 50-70 microns thick.

EXPLANATION

60A-429 + 36; USNM 160992 

W-105Z; USNM 160996

16 17 18 19 20 21 22 23 24 25 26 

NUMBER OF MAJOR SEPTA

27

FIGURE 17. Corallite diameter and number of major septa in 

Lithostrotion (Siphonodendron) sp. A. Each unnumbered 

symbol represents a single corallite. If more than one corallite shows the same diameter and number of septa, the number of similar corallites is shown.

Specimen USNM 160996 collected from the dark 

limestone member of the Alapah Limestone of the 

Lisbume Group, near Shainin Lake, central Brooks 

Eange, is similar to specimen 160992 in its development 

of the tabulae, dissepiments, columellae, and septa, but 

does differ by having corallites of a slightly smaller diameter and with fewer major septa. In specimen USFM 

160996, the corallites are typically 3.5 LO mm in diameter and have 18-19 major septa.

Occurrence. Specimen USNM 160922 was collected 

from the Cape Thompson Member of the Nasorak 

Formation, south of Nasorak Creek, near Cape Thompson, Alaska (Campbell, 1967, pi. 2B). It occurs with a 

Meramec coral fauna of Lithostrotion (Siphonodendron) warreni Nelson, Thysanophyllwn astraeiforme 

(Warren), and Sciophyllum sp. A. Specimen USI TM 

160996 was collected in the lower 20 feet of Bowsher

FIGURE 18. Sections of Lithostrotion (Siphonodendron) sp. 

A, USNM 160992.
16 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

and Dutro's (1957) dark limestone member of their 

type section of the Alapah Limestone, Shainin Lake, 

Alaska. It occurs with a large fauna of Meramec Foraminifera and cerioid Lithostrotiotlella corals.

Remarks. The most distinctive feature of Lithostrotion (Siphonodendron) sp. A is the tabulae which slope 

peripherally from the columella to the dissepimentarium at angle's of 50°-65°. This is in marked contrast 

to Lithostrotion (SipJionodendron} warreni Nelson (in 

which tabulae slope away from the columella at angles 

of 25°-35° and then are reflexed downward at an angle 

of 50°-65°. In Litllostrotion (Siphonodendron} oculinmn Sando the tabulae are reflexed even more sharply; 

furthermore, they are frequently reflexed to a 

nearly horizontal plane just before joining the 

dissepimentarium.

In size of the corallite diameter, number of major 

septa, development of the dissepimentarium, and type 

of columella, L. (S.} sp. A, L. (S.) warreni Nelson, and 

L. (8.} oculinuni Sando are very similar.

Family LONSDALEIIDAE Chapman, 1893 

Genus LITHOSTROTIONELLA Yabe and Hayasaka, 1915

Lithostrottonella. Yabe and Hayasaka, 1915, Geol. Soc. Tokyo

Jour., v. 22, p. 94. 

Lithostrotionella Yabe and Hayasaka. Hayasaka, 1936, Taihoku

Imp. Univ., Formosa, v. 13, no. 5, p. 47-58. 

Lithostrotionella Yabe and Hayasaka. Hill, 1956, in Moore, R. C.,

eel., Treatise on invertebrate paleontology, Part F, Geol. Soc.

America, p. F306-307.

Type species. Lithostrotionella iniicum- Yabe and 

Hayasaka, 1915, Permian, Chihsia Limestone, Yun-nan, 

South China.

Diagnosis. Cerioid corallum, primatic corallites, 

columella a persistent vertical lath frequently continuous with counter and cardinal septa. Lonsdaleoid dissepiments. All major septa intermittently reach the wall 

along the tops of the dissepiments. Minor septa short. 

Tabulae frequently complete, conical. (Summarized 

from Yabe and Hayasaka, 1915, p. 94.)

Lithostrotionella banffensis (Warren) 

Plate 3, figures 5-8; plate 4, figures 1-4; plate 10, figure 1

Litllostrotion banffense Warren, 1927, Canada Geol. Survey Bull. 

42, p. 46-47, pi. 3, figs. 5, 6, pi. 5.

Lithostrotionella floriformis Hayasaka, 1936, Taihoku Imperial 

University Memoirs Faculty of Science and Agriculture, 

v. 13, no. 5, p. 64-65, pi. 17, figs. la. b.

LitJwstrotionella vesioularis Hayasaka, 1936, Taihoku Imperial 

University, Memoirs Faculty of Science and Agriculture, 

v. 13, no. 5, p. 68-69, pi. 14, figs. 3a, b.

Lithostrotionella, banffensis (Warren). Kelly, 1942, Jour. Paleontology, v. 16, p. 354-356.

Lithostrotionella, banffense (Warren). Nelson, 1960, Jour. Paleontology, v. 34, p. 119, pi. 23, figs. 4, 5.

Lithostrotionella banffense (Warren). Nelson, 1961, Geol. Assoc.

Canada Spec. Paper 2, pi. 17, figs. 1, 2. 

Lithostrotionella. banffensis (Warren). Bamber, 1966, Canada

Geol. Survey Bull. 135, p. 17-19, pi. 3, fig. 5. 

Lithostrotionella- banffensis (Warren). Armstrong, 1970, U.S.

Geol. Survey Prof. Paper 534, p. 29-31, pi. 10, figs. 1-8, pi. 13,

figs. 1-7.

Material. Fragments of three coralla, USNM 

161011,161012, and 161013, each about 5 by 10 by 10 cm, 

were collected from the Lisburne Group in 1962. The 

specimens are from measured stratigraphic sections. Internal features were studied by eight transverse and 12 

longitudinal thin sections. The coralla are preserved as 

calcite with some minor silicification. The preservation 

of the microstructure in the specimens is generally poor, 

owing to calcite neomorphism.

Description. Specimen USNM 161011 is cerioid. In 

transverse section (pi. 3, figs. 5, 8) the corallites are 8- 

10.5 mm in diameter and have 21-25 major septa (fig. 

19). The major and minor septa are discontinuous and 

poorly developed in the dissepimentarium and are 

short ridges less than 0.5 mm long on the corallite wall. 

The major septa are well developed in the tabnlarium 

and extend to the columella as ridges on the surfaces of 

the tabulae. In the dissepimentarium, the majo^ septa 

are short and discontinuous. The minor septa reappear 

near the tabularium wall and penetrate it; they are 

short, generally less than 1 mm in length. The dissepiments are lonsdaleoid and show considerable variation 

in size in a given corallite and between corallites. The 

columella is generally continuous with the counter septum; it is typically 1-1.5 mm long and 0.25 mm wide.

In longitudinal section (pi. 3, figs. 6, Y) the dissepimentarium consists of 3-6 rows of dissepiments which 

are inclined upward at angles of 25°-35°. In a corallite 

10 mm wide, the tabularium is approximately 5 rnm 

wide. The tabulae are normally incomplete and slope 

away from the columella at angles of 30°^tO°. The interior of the corallum is filled with sparry calcite. These 

calcite crystals are in the 0.5-2 mm size range ard have 

by grain growth engulfed, penetrated, or in some cases 

destroyed the smaller (5-30 microns in size) calcite 

crystals which form the internal structures of the 

corallum.

The corallite walls are 100-125 microns thick and 

have a central dark band of calcite 10-20 microns thick. 

The major septa in the tabularium are 150 microns thick 

and also have a central dark band on which fibrous calcite is deposited. The tabulae and dissepiments have 

walls that are 20-40 microns thick and that ar^ composed of interlocking crystals of calcite which range in 

size from 4 to 10 microns (pi. 3, fig. Y).

Specimen USNM 161012 is cerioid (pi. 4, figs, 1, 2). 

In transverse section the corallites are 5.6-7.0 mm in
SYSTEMATIC PALEONTOLOGY 17

12

11

10

5 6 -

5 -

4 -

EXPLANATION

Lithostrotioitelln aff i. 

biinffetixiis (Warren)

 62C-31 + 1260.USNM 161010

Litliostrutiiintlla bn nffe n s /

(Warren) 

O 60A-425+150;USNM 161011

 62C-15 + 570;USNM 161012 

A62C-31 + 335, USNM 161013

D Bamber's (1966, p. 17-18) 

lectotype for L. bantfensis 

(Warren)

14 15 16 17 18 19 20 21

NUMBER OF MAJOR SEPTA

22 23 24 25 26

FIGURE 19. Corallite diameter and number of major septa in Bamber's (1966, p. 17-18) lectotype of Lith&strotfonella 

banffensis (Warren) ; three specimens of Lithostroti&nella banffensis (Warren) and Lithostrotionella aff. L. 

banffensis (Warren) from the Lisburne Group. Bach unnumbered symbol represents a single corallite; if more 

than one corallite shows the same diameter and number of septa, the number of similar eorallites is shown.

diameter and have 18-21 major septa (figs. 19, 20). The 

dissepiments are lonsdaleoid. The major and minor 

septa occur in the dissepimentarium as short ridges on 

the epitheca and as projections on the outer wall of the 

taTbularium. Minor septa are present in the tabularium 

and may project into the dissepimentarium. The tabulariuin is from 3.5-4.5 mm wide. Major septa extend onehalf to two-thirds the distance from the tabularium wall 

to the center of the corallite. Major septa are commonly 

curved or sinuous, are thickened in the peripheral part 

of the tabularium, and are thinner toward the axis and 

in to the dissepimentarium. The septa are radially arranged. The columellae are typically 1-1.5 mm long and 

0.2-0.3 mm wide, lens shaped, and frequently attached 

to the cardinal-counter septa. The edges of the columella 

have small projections which are formed by the major 

septa on the surfaces of the tabulae.

A longitudinal section (pi. 4, fig. 2) of a 4-mm wide

FIGURE 20. Sections of LithostrotioneUa banffensis (Warren), 

USNM 161012.
18 'CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

corallite shows the dissepimentarimn to be composed of 

1-2 rows of swollen, globose dissepiments. Dissepiments 

have considerable size variation. Tabulae are generally 

incomplete. Tabulae slope away from the columella at 

angles of 15°-40° and, within 0.7-0.4 mm of the dissepiments, are reflexed to 15°-25°.

The columella is clearly formed by the axial ends of 

the cardinal and counter septa plus the axial edges of 

other septa which reach the columella as ridges on the 

surface of the tabulae.

The preservation of the corallum is poor (pi. 10, fig. 

1). The calcite crystals ranging in size from 40 to 150 

microns, which fill the interior of the corallites have, by 

grain growth, penetrated and replaced much of the 

calcite which forms the internal structures of the 

corallites.

The corallite walls are typically 150-200 microns thick 

(pi. 10, fig. 1). A central dark band 20-30 microns 

thick is present in the corallite walls. The walls are 

composed of long fibrous calcite which was deposited 

normal to the dark bands. The discontinuous major septa 

which project from the wall into the dissepimentariuni 

appear to have a composition similar to the epitheca. 

Near the tabularium wall, the major septa are formed 

by interlocking crystals of calcite which range in size 

from 20 to 40 microns. The septal microstructure suggests that septa were made of divergent fibers of calcite with a central trabeculae band.

Specimen USNM 161013 (pi. 4, figs. 3, 4) is cerioid, 

and in transverse section the corallites are 4.9-7 mm in 

diameter and have 18-21 major septa (fig. 19). The dissepiments are lonsdaleoid. Minor septa are present and 

am one-half to two-thirds the length of the major septa. 

Major septa reach the columella as low ridges on the 

upper surfaces of tabulae. Major and minor septa are 

slightly sinuous, are thickened in the peripheral part of 

the tabularium, and become thinner towards the axis 

and into the dissepimentarium. The septa are radially 

arranged. Many columellae are continuous with cardinal 

and counter septa are typically lens shaped, 1.0-1.5 mm 

long, and have a maximum thickness of 0.2-0.3 mm. The 

major septa are generally discontinuous in the dissepimentarium. In all specimens they are present on the epitheca wall as ridges which project from 0.3 to 1 mm 

into the dissepimentarium. The discontinuous major 

septa are 60-80 microns thick at the tabularium wall and 

150 microns thick near the epitheca.

In longitudinal section, the dissepimentarium is composed of 3-5 rows of swollen dissepiments. The typical 

dissepiment is 1-1.5 mm long and 1-2 mm wide. The 

tabulae tend to be complete and slope away from the 

columella at angles of 30°-50°. Six to eight tabulae occur in 5 mm.

The microstructure of the corallum is affected l~y calcite neomorphism, which obscures many of the finer details. The wall is 150-200 microns thick, has a clearly 

defined central band of gray calcite 20--25 microns thick. 

The epitheca is composed of fibrous calcite deposited 

normal to the central gray band. The septa have an irregular central band of trabeculae from which divergent fibrous calcite radiates.

Occurrence. Near Cape Thompson south of Nasorak 

Creek, the writer in 1962 collected L. banffensis (Warren) from CampbelFs (1967, p. 44-45, pi. 2B) measured 

section of the upper member of the Nasorak Formation 

at his stratigraphic level of 950 feet, specimen USNM 

161011 (pi. 3, figs. 5-8), and at 690 feet, specimen 

USNM 161009. Associated with L. banffemis are Lithostrotionella mclareni (Sutherland) and Lithostrotion 

(Siphonodendron] warreni Nelson.

In the measured sections of the Kogruk Formation in 

the western DeLong Mountains, L. banffensis (USNM 

161012) was found in section 62C-15 at 570 feet below 

the top of the section with Lithostrotionella tjwlaareni 

(Sutherland), Lithostrotion (Siphonod-endron) sinuosiun (Kelly), Thysanophyllum sp. A, and Faberophylftwispp. (fig. 3).

At section 62C-31, L. banffensis (USNM 161013) was 

collected 335 feet below the top of the section with Lithostrotionella sp. B and Faberophyllmn sp. (fig. 5).

From the limestone and chert member of the Peratrovich Formation, Prince of Wales Island, southeastern 

Alaska, Armstrong (1970, p. 29) reports L. barffensis 

occurring with late Meramec Foraminifera micrifauna 

and a rugose coral fauna of Faberophyttutn girtyi Armstrong, F. wiUiam^i Armstrong, Lithostrotionella pen- 

'mylvanica ( Shimer), Thysanophylliim astraeiforme 

(Warren), Sciophyllum alaskaensis Armstrong, 8.lambarti Harker and McLaren, Diphyphyllum venosum 

Armstrong, and D. klaivockensis Armstrong.

The type material for L. banffensis, according to Warren (1927, p. 47), came from Alberta, Canada, "near 

the top of the Bundle Limestone on Stoney Mountain." 

Nelson (1960, p. 119) is of the opinion that "tin holotype was derived from the upper Lithostrotionella}^^ 

(lower Mount Head Formation)."

Remarks. Bamber's (1966, p. 17-18) description of 

the lectotype of L. banffensis (Warren) indicates that 

the corallites are 7-10 mm in diameter and have 18-23 

major septa. Minor septa are very short, but present. 

The dissepiments are lonsdaleoid. As Bamber (p. 23) 

redescribed L. pennsylvanica (Shimer) it differs from 

L. banffensis (Warren) by having flat-lying tabulae 

which are sharply reflexed upwards near the columella 

and which are better developed than those of L. banffen-
SYSTEMATIC PALEONTOLOGY 19

sis and by having larger lonsdaleoid dissepiments and 

larger corallites (average diameter 10-14 mm).

The writer's concept of Lithost rationed a ban-ffensis 

(Warren) is rather wide and embraces forms which 

show some variation from tho holotype in corallite 

diameter and development of the dissepimentarium.

The holotypes of Lithostrotionella vesicularis 

Hayasaka (1936) and Lithostrotionella flo?*ifon?iis 

Hayasaka (1936) from the Mississippian Peratrovich 

Formation, Prince of Wales Island, southeastern Alaska 

are considered by Armstrong (1970) to be junior synonyms of L. bcmffensis (Warren).

The diameter of the corallites and number of major 

septa in the coralla assigned to this species are graphically compared to Bamber's (1966) lectotype of the 

species in figure 19.

Specimen USNM161013, as figure 19, shows has corallites which are more uniform in size and typically 1-2 

mm smaller than Bamber's (1966) lectotype of the 

species. Specimen USNM 161013 also has smaller dissepiments, in which the lonsdaleoid trait is not as welJ 

developed as in the lectotype.

Specimen USNM 161012, from 570 feet below the top 

of section 62C-15, also has corallites with diameters 

1-2 mm less than those in Bamber's lectotype of L. ban- 

 ffensis (fig. 19). The major and minor septa are more 

strongly developed and more persistent in the dissepimentarium, but the lonsdaleoid dissepiments are similar 

to those of the lectotype.

Some of the corallites in specimen USNM 161011 have 

a slightly larger diameter, 1-2 more major septa, and 

larger lonsdaleoid dissepiments than Bamber's lectotype 

of L. ban-ffensis. Specimen USNM 161011 from the Lisburne Group compares closely with examples of L. banff ens-is collected by the writer (1970) from carbonate 

rocks of Meramec age collected on the northwest side of 

Prince of Wales Island, southeastern Alaska.

Lithostrotionella aff. I. banffensis (Warren) 

Plate 4, figures 5, 6

Material. Specimen USNM 161010 is a 6 by 8 by 11 

cm fragment of a corallum collected from measured section 62C-31. Two longitudinal and three transverse 

thin sections were made. Thirty corallites were studied 

in transverse, and 11 in longitudinal thin section. The 

specimen is preserved as calcite in which much of the 

original microstructure is preserved.

Description. The corallum is cerioid. The corallites 

(pi. 4, fig. 5) are from 4.5 to 8.5 mm in diameter and 

have 16-20 major septa (fig. 19). In mature corallites, 

the major septa are discontinuous in the dissepimentarium, and the dissepiments are lonsdaleoid. Minor septa 

alternate with major septa, but in some corallites minor

378-461 O 70 4

septa may be absent between a few pair of the major 

septa. Major septa are generally withdrawn from the 

columella. Minor septa are one-thrid to one-half the 

length of major septa. Major septa are 75-150 microns 

thick near the tabularium wall. Septa of both classes 

taper from the tabularium wall towards the axis and 

into the dissepimentarium (fig. 21).

The columella, simple is present in all corallites, and 

is lens shaped. It is typically 0.6-0.8 mm long and 0.2- 

0.3 mm wide. The columella commonly shows projections 

which are the ridges formed by the major septa on the 

surface of the tabulae. The columella appears to be the 

result of axial thickening of the counter septum.

In transverse section (pi. 4, fig. 6) the dissepimentarium consists of 1-3 rows of dissepiments which are inflated and strongly arched upward. There are 7-9 

dissepiments in 5 mm. In mature corallites the dissopimentarium occupies about half the diameter. The 

tabulae are generally complete and slope upward from 

the dissepimentarium at 20°-35° before meeting the 

slightly sinuous columella. There are 8-11 tabulae, in 

10 mm.

The corallite walls are 250-300 microns thick and 

contain a well-developed central band of dark-gray 

calcite 20-25 microns thick. The corallite walls are 

composed of fibrous calcite crystals with their long &xes 

normal to the central band. The major and minor septa 

are composed of fibrous calcite crystals similar to those 

in the corallite walls. The septa have a central band of 

trabeculae. The microstructure of the tabulae and dissepiments is now composed of interlocking calcite crystals which range in size from 10 to 20 microns.

FIGURE 21. Sections of LithostrotioneUa aff. L. banffensis 

(Warren) ; USNM 161010.
20 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

Occurrence. The single sample of Lithostrotionella

aff. L. ~banffensis was collected 1,260 feet below the top

of measured section 62C-31 in the Kogruk Formation,

western DeLong Mountains. It occurs with Lithostrotwn

(Siphonodendron) warreni Nelson, Lithostrotwn

(Siphonodendron) sinuosum (Kelly), and Lithostrotionella mclareni (Sutherland] (fig. 5).

Remarks. Lithostrotionella aff. L. banffensis, USNM 

161010, has close affinities to L. banffensis Warren. It 

differs from Bamber's (1966) leototype (fig. 19) in that 

its corallites are generally 2 mm smaller in diameter but 

they typically have 18-20 major septa. It also differs by 

having longer and consistently better developed minor 

septa. The major and minor septa are also more persistent and better developed in the dissepimentarium.

Specimen USNM 161012 was collected 570 feet below 

the top of measured section 62C-15 and is placed with 

L. ~ban-ffensls. (See remarks under that species.) In 

diameter of the corallites, it resembles Lithostrotian&ll'a 

aff. L. ~banffensis but differs by having larger, better 

developed lonsdaleoid dissepiments and 1-8 additional 

major septa per corallite.

Lithostrotionella birdi Armstrong 

Plate 4, figure 7; plate 5, figures 1-3, 5, 6

LitJiostrotioneUa birdi Armstrong, 1970, U.S. Geol. Survey Prof. 

Paper 534, p. 32-35, pi. 7, fig. 1-4, pi. 8, figs. 1-7.

Material. Specimen USNM 161024 is an 8 by 8 by 10 

cm fragment, of a corallum, and specimen USNM 

161031 is a 5 by 6 by 8 cm fragment of a corallum. These 

were collected from measured section 60A 400-403 by 

Dr. Sigmund Snefeon in 1960. Sample USNM 161024 

was studied in six transverse thin sections and three 

longitudinal thin sections, and USNM 161031 in one 

transverse thin section 'and two longitudinal thin sections. Specimen USNM 161023 is a 10 by 10 by 12 cm 

fragment of a corallum collected from measured section 

62C-15. This sample was studied by four transverse and 

four longitudinal thin sections.

Description. The corallum is cerioid. Specimen 

USNM 161024 in transverse thin section (pi. 4, fig. 7) 

has mature corallites which are 3.5-6.5 mm in diameter 

and which have 15-19 slightly sinuous major septa (figs. 

22, 23). The major septa may be weakly dilated in the 

tabularium, and they extend two-thirds or more the distance to the axis. Major septa are generally discontinuous in the dissepimentarium. Minor septa are 

inconsistently developed. In some corallites minor septa 

are short, ridges on the epitheca or are absent. In some 

corallites most of the major and minor septa are continuous through the dissepimentarium. The dissepiments 

may be arranged in a herringbone pattern in many specimens but generally are lonsdaleoid, and interrupt from

u 7

LU

EXPLANATION

 60A-401; USNM 161024

 60A-400+105- USNM 161031 

° 62C-15 + 49; USNM 161023

 Holotype of Lithostrotionella 

birdi; USNM 160487; 

from Armstrong (1970)

11 12 13 14 15 16 17 18 19 

NUMBER OF MAJOR SEPTA

20 21

FIGURE 22. Corallite diameter and number of major septa in 

Lithostrotionella birdi Armstrong. Each symbol renresents 

a single corallite.

FIGURE 23. Sections of LitJiostrotioneUa birdi Armstrong, 

USNM 161024.

2 to 8 major septa. Columellae are present in the majority of corallites and vary in their development. Most 

are lens shaped, and many are connected to the counter 

septa (pi. 5, fig. 6). A typical columella is 1 mm long 

and 0.2 mm wide. Many columellae have short projections which are formed by axial ends of the major 

septa as ridges on the upper surfaces of the tabulae.

In longitudinal section (pi. 5, figs. 3, 5), the dissepiment arium is 1-2 and in a few examines 3 rows of
SYSTEMATIC PALEONTOLOGY 21

inflated and inclined dissepiments. There are 7-10 dissepiments in 5 mm. The majority of tabulae are complete and convex, sloping upAvards at angles of 35° i5° 

from their junction with the dissepiment to their apex 

at the columella. The columella is thin, nonpersistent, 

and sinuous.

'The internal structures of the corallites are preserved 

by neomorphic calcite ranging in size from 50 to 150 

microns and much of the original microstructure has 

been destroyed. The internal voids of the collallum are 

filled with chalcedony (pi. 5, fig. 5).

Specimen USNM 161031 (not illustrated) does not 

differ in any significant way from the above specimen.

Specimen USNM 161023 (pi. 5, figs. 1, 2) is similar 

to the above specimens but has corallites that are typically 4.5-7.5 mm in diameter and that have 15-17 major 

septa. Within the corallum, the typical corallite. tends 

to have larger, well developed lonsclaleoid dissepiments, 

and the septa are amplexoid. In general the typical 

corallites show a stronger trend toward the characteristics of the genus ThysanophyUum-. The internal preservation of this specimen is similar to that described for 

specimen USNM 161024 above.

Occurrence. L. birdi specimens, USNM 161031 and 

161024, were collected 105 and 180 feet respectively below the top of measured section 60A-400 i03 (fig. 7), 

near Trail Creek, DeLong Mountains. They were found 

with a Foraminifera fauna of earliest Chester age, 

equivalent to Mamet's (1968) and Maniet and Mason's 

1968) microfaimal assemblage zone 16i (B. L. Mamet, 

oral commun., March 1969). L. lirdi, USNM 161023, 

was also collected in the Kogruk Formation at 49 feet 

from the top of stratigraphic section 62C-15, USGS loc. 

M1019 in the DeLong Mountains (fig. 3). This specimen was found in association with Faberophyllwn spp. 

and Lithostrotionella mclareni (Sutherland).

The holotype and paratypes of L. ~birdi are reported 

by Armstrong (1970) from the chert and limestone 

member of the Peratrovich Formation, Prince of Wales 

Island, southeastern Alaska. Here L. birdi occurs with 

a late Meramec fauna of Foraminifera and a coral 

fauna characterized by Fdberophyllum. girtyi Armstrong, F. williamsi Armstrong, Lithostrotionella 

banffensis (Warren), L. pennsylvanica (Shinier), 

Thysanophyllum astraeiforme (Warren), and Sciophyllum alaskaensis Armstrong.

Remarks. L. ~birdi as defined by Armstrong (1970) 

has a consistent ratio of the diameter of mature corallite 

to the number of major septa. Serial transverse sections 

of corallites reveal that a given corallite may shoAv considerable variation in the organization of its internal 

structures. Variation in its vertical length is particularly pronounced in the clissepimentariimi, where the

dissepiments and septa may show a wide range of fcnns 

and shapes. At the levels at which a corallite has herringbone dissepiments it will also have persistent major 

septa in the dissepiment arium. At another level the 

corallites may have discontinuous septa in the disrepimentarmm and large lonsdaleoid dissepiments. An individual corallite and the majority of corallites within a 

corallum may have the characteristics of the genus 

Lithostrotionella, but also can be acolumellate and have 

the traits of the genus Thysanophyllum. A few corallites 

may display a columella and persistent continuous major septa that join the wall and have the traits of the 

genus Lithostrotion. The same type of corallite variation or plasticity exists in the closely related species of 

Lithostrotionella mclareni (Sutherland). (See Sutherland, 1958, and McLaren and Sutherland, 1949.)

Lithostrotionella birdi Armstrong is distinguished 

from L. mclareni (Sutherland) by L. mclareni'} s smaller 

corallites, which have a diameter of 3-4 mm and which 

have only 12-14 major septa and, typically, by L. tnclarentfs dissepimentarium, in which lonsdaleoid dissepiments are not as well developed.

On any given transverse thin section, 80 percert of 

the corallites of specimen USNM 161024 have internal 

structures characteristic of the genus Lithostrotionella. 

Some corallites have persistent septa in the dissepimentarium and are suggestive of cerioicl Lithostrotion. Only 

20 percent of the corallites have the traits of the g^nus 

Thysanophyllum, and none were found that have the 

traits of Sciophyllum.

Specimen USNM 161023 (pi. 5, figs. 1, 2) from section 62C-15 has slightly more than half of its corallites 

with the characteristics of Lithostrotionella. Corallites 

characteristic of Sciophyllwn make up about 20 percent 

of the corallites. (See remarks under Sciophyllum 

alasTcaensis Armstrong.)

Lithostrotionella mclareni (Sutherland) 

Plate 5, figures 4, 7, 8-10; plate 6, figures 1, 2, 7-9

Lithostrotion sp. McLaren and Sutherland, 1949, Jour. Paleontology, v. 23, p. 631, pi. 103, figs. 1-9, text figs. 2-4.

Lithostrotion [Lithostrotionella'] [Thysanophyllum] mclareni 

Sutherland, 1958, Canada Geol. Survey Mem. 295, p. £5, 96, 

pi. 33, fig. la-g.

Material. Fragments of eight coralla were collected 

from three measured sections of the Kogruk Formation 

in the DeLong Mountains.

The internal features of the specimens from the DeLoiig Mountains are preserved as crystals of neomorphic 

calcite, which range in size from 10 to 20 microns, embedded in chalcedony which fills the internal ^oids 

within the corals. The majority of specimens aA^ailable 

for study had some of the voids within the corallites
22 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

filled with sparry calcite. In these corallites, vestiges of 

the original microstructure are preserved.

The specimens were studied as shown in the tabulation below:

USNMNo.

160999

161000

161001

161002

161003

161004

161016

161030

Number of

transverse

thin sections

3

3

3

2

2

2

1

3

Numbt

coralli

95

185

225

90

160

100

32

190

Number of 

longitudinal 

thin sections

1

2

4

2

2

3

3

5

Number of

corallites

7

27

30

18

20

38

26

50

Description. Specimen TJSNM 160999 is a cerioid 

corallum and in transverse section (pi. 5, fig. 10) has 

mature corallites which are 3.5-4.4 mm in diameter and 

have 13-15 slightly sinuous major septa (fig. 24). Corallites have common walls which average about 150-200 

microns thick and which are now composed of crystals 

of calcite ranging in size from 10 to 20 microns. The 

centers of the walls have a dark-gray calcite band 12-15 

microns thick. Near the epitheca the major septa are 

40-50 microns thick. In the tabularium the major septa 

are dilated and are 60-70 microns thick and taper to 

their distal ends. They do not reach the columella, and 

many are discontinuous in the dissepimentarium. The 

minor septa are inconsistently developed, are generally 

short spikes on the epitheca wall, and only a few appear 

on the inside of the tabularium wall. Most of the corallites have lonsdaleoid dissepiments, and some corallites 

have herringbone dissepiments. Many columellae are 

swollen extensions of the counter septum and are typically 0.5-1.0 mm long and 0.1-0.2 mm wide. The columella is thin, persistent, and slightly sinuous.

In longitudinal section (pi. 5, figs. 4, 9) the dissepimentarium is a single to double row of inflated and 

inclined dissepiments. There are 10-13 dissepiments in 

5 mm. Many tabulae are incomplete. They are convex 

upward, sloping away from the columella at angles of 

10°-30° to their junction with the dissepimentarium.

Occurrence. Lithostrotianella mclareni (Sutherland) is common in the Kogruk Formation of the DeLong Mountains. In section 62C-15, it is found below the 

top of the measured section at 49 feet, TJSNM 161000; 

150 feet, TJSNM 161001; 250 feet, USNM 161002; 510 

feet, USNM 161003 (pi. 6, figs. 1, 2) and 161004. In this 

section the species occurs with Faberophyllum spp., 

Lithostrotionella banffemis (Warren), Thysanophyllum sp. A, and Sciophyllum alaskaensis Armstrong. L. 

mclareni (TJSNM 160999) was found at 1,065 feet, and 

(TJSNM 161016) at 1,390 feet, below the top of section 

62C-31 (fig. 5). Here it also occurs in association with 

a large fauna of lithostrotionid corals (fig. 3).

L. mclareni, USNM 161030 (pi. 6, figs. 8, 9), was collected 1,100 feet from the top of section 60A-400-403 in

the Kogruk Formation by Dr. Sigmimd Snelson in 1960. 

It occurs with a foraminiferal fauna of Meramec age 

(fig. 7).

In the Kogruk Formation L. mclareni occurs with a 

coral fauna of Meramec age. The holotype of the species, 

according to McLaren and Sutherland (1949, p. 633; 

Sutherland, 1958, p. 96), was found 4 feet from the top 

of the Prophet Formation, in beds of Middle Mississippian age, near the headwaters of Bull Creek, British 

Columbia.

Macqueen and Bamber (1968, p. 261, fig. 7) found a 

few specimens of L. mclareni (Sutherland) in their 

faunal assemblage 2, Meramec Mount Head Formation, 

southwestern Alberta. Bamber, Taylor, and Proctor 

(1968, p. 8) report the holotype was collected from 

member C of the Prophet Formation and th^ associated coral fauna is middle to late Meramec in age.

Remarks. The holotype of Lithostrotionella mclareni (Sutherland), as described by McLaren and Sutherland (1949) and Sutherland (1958), has ccrallites 

with the internal structures which are typically developed in genera of Lithostrotion, LithostrotioneUa* and 

Th ysan oph yllmn.

The specimens assigned to Z. mclareni from tl °i Kogruk Formation display, within a single colony, cc rallites 

which have the generic characteristics of three different 

genera (fig. 25). Thin section studies of the coralla indicate corallites characteristic of a particular generic 

type tend to group together within one part of a corallum with transitional types occurring between two 

distinct generic types. Within the coralla, the Lithostrotionella type of corallite is the most common and 

the rarest configuration is the Lithostrotion type of 

corallite.

Specimen USNM 161003, which is assigned to this 

species, has the greatest deviation from the holotype. 

It occurs 520 feet below the top of section 62C-15 and 

was collected from the same bed and a few fe^t from 

typical specimens of L. mclareni (Sutherland). Any one 

of the serial thin sections shows a predominance of 

corallites of the Thysanophyllum and Sciophyllum 

type, but also contains many corallites witv welldeveloped columellae typical of Lithostrotionella and 

in particular of L. mclareni. Within the corallum of 

specimen USNM 161003, the cluster of corallite? which 

have the structure of Sciophyllum are morphologically 

identical to the corallites of Sciophyllum lambarti 

Harker and McLaren. This latter species also has the 

same general stratigraphic range in the Kogruk Formation as L. mclareni. Specimen USNM 161003 strongly 

suggests S. lambarti was derived from L. mclareni 

through the degeneration and amplification of structure 

towards large lonsdaleoid dissepiments, peripheral
SYSTEMATIC PALEONTOLOGY 

6

23

tr

LJI- 2

LJ

EXPLANATION

 62C-31 + 1065;USNM 160999 

O 62C-L5 + 150, USNM 161001 

I________I________I

 62C-15 + 49;USNM 161000 

D 60A-402+195,USNM 161030 

__J_______I________I

COtr

LJ 

LJ 4

2

EXPLANATION

 62C-15 + 250.USNM 161002

 62C-15f 510A.USNM 161003 

O 62C-15+510B;USNM Ibl004 

O 62C-31 +1390, USNM 161016

10 11 12 13 14

NUMBER OF MAJOR SEPTA

15 16 10 11 12 13 14 15 

NUMBER OF MAJOR SEPTA

16

FIGURE 24. Corallite diameter and number of major septa in LithostrotioneUa mclareni (Sutherland). Each unnumbered symbol represents a single corallite; if more than one corrallite shows the same diameter and number of septa, the number of 

similar corallites is shown.

withdrawal of the septa, and elimination of the 

columella.

Lithostrotio'nellatnclareni (Sutherland) is closely related to Lithostrotionella. birdi Armstrong, both of 

which are characterized by coralla with individual 

corallites that have structural arrangements of the genera LithostrotioneUa, Lithostrotion, and Sciophyllum. 

L. birdi consistently has larger corallites, which are 4.5- 

6.5 mm in diameter and which have 17-20 slightly 

sinuous major septa, and the corallites typically have 

well-developed lonsdaleoid dissepiments.

FIGURE 25. Sections of Litliostrotionella mclareni (Sutherland), USNM 161003.

lithostrotionella macouni (Lambe) 

Plate 12, figures 1-6

Lithostrotion macouni Lambe, 1899, Ottawa Naturalist, v. 12,

p. 220. 

LitJlostrotion macouni Lambe. Lambe, 1901, Canada Geol. ?nrvey, Contr. Canadian Paleontology, v. 4, pt. 2, p. 176, 177,

pi. 14, figs. 11, lla, lib. 

Lithostrotionl macouni Lambe. Nelson, 1960, Jour. Paleontology,

v. 34, p. 122,123, pi. 23, figs. 1, 2.

Description of syntype. Geological Survey of Canada No. 4327. The material available for study consists 

of one transverse and one longitudinal thin section erch 

on a 27 mm by 48 mm slide. The transverse thin section 

(pi. 12, fig. 4) had about 30 complete corallite sections 

available for study. In longitudinal thin section, sections of five corallites are present (pi. 2, fig. 3). The 

corallum is preserved as calcite, and the voids within 

the corallites have been filled by sparry calcite. The two 

thin sections are the same material on which Nelson 

(1960, p. 122-123) based, in part, his redescription of 

Lambe's 1899 species.

Description. In transverse section the corallites are 

1.9-2.8 mm in diameter and have 9^-11 major septa which 

generally extend to the axial region and fuse with the 

columella (figs. 26, 27). In about half of the corallites 

studied, one or more major septa are discontinuous 

within the dissepimentarium (pi. 12, fig. 1). The major 

septa are 60-80 microns thick at their junction with the 

corallite wall and progressively taper towards the cchimellae. In the tabularium they are typically only 20-40
24 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

o:

UJ

h 2

1 -

EXPLANATION

LithostrotioHella macouni (Lambe)

 Geological Survey Canada 4327 

syntype

Lithostrvtionelln sp. A

 62C-34 + 395; USNM 161027

Lithostrotionella sp. B

o 62C-31+365; USNM 161028

10 11 12 13 

NUMBER OF MAJOR SEPTA

14 15

FIGURE 26. Corallite diameter and number of major septa in 

Lithostrotionella ma-count (Lambe), syntype; Lithostrotionella sp. A and Lithostrotionella sp. B. Each unnumbered symbol represents a single corallite; if more than one 

corallite shows the same diameter and number of septa, the 

number of similar corallites is shown.

microns thick. Minor septa are inconsistently developed; 

they are generally only 0.2-0.5 mm long and in many 

corallites are absent between the major septa. The corallite walls are 100-150 microns thick and have a central 

dark band of calcite 20-30 microns thick. The walls are 

composed of fibrous calcite crystals deposited normal to 

the dark band (pi. 12, fig. 2). The columella is an extension of the counter septum to which the cardinal septum 

is generally fused. One or all of the other major septa 

may reach the columella. The majority of the dissepiments are regular but almost half the corallites have 

lonsdaleoid dissepiments.

In longitudinal thin section the tabulae are generally 

complete and about 30-40 microns thick. As was pointed 

out by Nelson (1960, p. 122), this longitudinal section 

is apparently off center, and the exact relationship of 

the tabulae to the columella is not clear. About 12-15 

tabulae occur in 5 mm. One section of a corallite suggests the presence of a columella. The tabulae are bent

FIGURE 27. Sections of Lithostrotionetta macomii (Lambe), 

syntype GSC No. -4327.

upwards 20°-25°. The dissepimentarium consists of a 

single row of globose dissepiments, 9-12 occurring in 5 

mm.

Occurrence. According to Lambe (1901, p. T.TT) the 

specimen, GSC No. 4327, was collected at "Fossil Point, 

Peace Kiver, British Columbia" by J. Macoun in 1875. 

Dr. E. W. Bamber of the Geological Survey of Canada 

reports (written commun., May 1968) "as far as I know 

L. macouni is late Meramecian in age and I have found 

it only in the lower range of Fdberophyll/um, and 

slightly below; never in the upper part of the Fdberophyllmn zone, or in the overlying Chesterian buds."

Remarks. Lithostrotionella macouni is dist;nguishable from the late Kinderhook and early Osage corals 

Lithostrotionella micra Kelly (1942, p. 357, pi. 50, fig. 

7) and Lithostrotionella lochmanae Armstrong (1962, 

p. 38-39, pi. 4, figs. 6-8, which have similar corallite 

diameters, by its smaller lonsdaleoid dissepiments. It is 

separated from Lithostrotionella nwlareni (Sutherland) by its better developed major septa ard welldeveloped columella.

Within the Kogruk Formation, two forms of Lithostrotionella were collected which appear to be morphologically similar and possibly even conspecific with the 

syntype of L. macoum. Because each form h represented by only a few specimens, their taxonomic relationship to L. macouni is somewhat uncertain. Accordingly they have been designated Lithostrotionella sp. A 

and Lithostrotionella sp. B. The morphological relationships of these two forms with each other and with 

L. macouni are discussed in this study within the "Remarks" of L. sp. A and L. sp. B.

Groot (1963, p. 49-52, pi. 6, figs. 1, 2) describes a 

cerioid, trimorphic coral, Lithostrotion trimorphum 

Groot from the Numurian age, Perapertu Formation of
SYSTEMATIC PALEONTOLOGY 25

Spain, which has corallites 4-5 mm in diameter that 

have 13-14 major septa, poorly developed minor septa, 

and a single row of steeply inclined dissepiments. L. ' 

trimorphum, (Groot, pi. 6, fig. la) shows strong similarity to the syntype of L. macouni (Lambe) and to 

Lithostrotionella sp. A and L. sp. B.

A species from eastern Asia which morphologically 

shows some relationship to the above species was described by Yli (1933, p. 91, pi. 18, figs. 2, 3; 1937, p. 42- 

43, pi. 11, figs. 1, 3) from the Viseaii of China. Lithostrotion mccoyanum Edwards and Haime var. 

mutungeme Yii has corallites that are 4-5 mm in diameter and that have 12-13 major septa. It differs from L. 

mavmmi, L. sp. A, and L. sp. B by having long minor 

septa and 2-3 rows of dissepiments.

Lithostrotionella sp. A 

Plate 7, figures 1-6

Material. Specimen USNM 161027 was collected 

from stratigraphic section 62C-34, 395 feet below the 

top, and is a fragment of a corallum 8 by 8 by 10 cm. 

It was studied in five transverse and five longitudinal 

thin sections. The specimen is preserved as calcite in a 

calcite matrix. The niicrostructure of the corallum is 

well preserved.

Description. Specimen USNM 161027 (pi. 7, figs. 1, 

2) is cerioid in transverse section and has uniform 

prismatic corallites which are typically 2.0-2.8 nim in 

diameter; the corallites have 13-14 major septa. The 

major septa are 0.4-0.7 mm long, and the minor septa 

are 0.15-0.3 mm long (figs. 26, 28). The major septa, 

with rare exceptions, are continuous through the dissepimentarium. The dissepiments are regular, and only 

in the larger diameter corallites have weakly developed 

lonsdaleoid dissepiments which may intercept 1-2 major 

septa. A columella is present in the majority of the 

corallites; it is lath to lens shaped and is apparently 

not connected to any septa. Serial sections show some 

corallites at various levels are acolumellate. Serial transverse thin sections reveal that the major septa extend 

one-fourth to three-fourths the distance to the axial region as short ridges on the upper surfaces of the tabulae. 

The cardinal-counter septa extend farther on the tabulae than the other septa. The adjacent lateral septa 

are weakly incurved to form poorly defined open 

fossulae.

In longitudinal section (pi. 7, figs. 3, 5, 6) the dissepimentarium is present generally throughout the 

length of mature corallites and consists of a single row 

of swollen, uparched dissepiments. The typical dissepinientarium is 0.5 mm wide and has 13-17 dissepiments 

in 5 mm. The tabulae are complete and dome shaped. 

They slope downward from the columella at angles of 

15°-30°. The tabulae within 0.5 mm of the dissepimenFIGXIRE 28. Sections of Lithostrotionella sp. A, USNM 161027.

tarimn are reflexed downward about 40°-50°, and adjacent to the dissepimentarium they are reflexed upward before joining to the dissepiments (pi. 7, figr,, 5, 

6). The columella is a rodlike vertical structure composed of calcite crystals arranged similarly if not icSntically to the septa. The tabulae abut against the 

columella (pi. 7, fig. 3) but do not contribute to the 

structure of the columella.

The corallite walls are typically 150 microns thick 

and contain at their center a band of dark-gray calcite 

20 microns thick (pi. 7, figs. 3, 4). The corallite walls 

are formed by fibers of calcite that have the long axis 

normal to the gray central band. The niicrostructure of 

the septa appears to be similar to the epitheca. The septa 

lack a central dark-gray band and are composed of 

fibrous calcite deposited parallel to the calcite of the 

epitheca (that is, in optical continuity). In transverse 

section the niicrostructure of the columellae appears to 

be similar to that of the septa.

Occurrence. Specimen USNM 161027 was collected 

395 feet below the top of section 62C-34, on a river cut 

bank exposure, west side of the Kukpuk River, in the 

Lisburne Hills (fig. 9). The specimen is preserved in 

echiiioderm-foraminiferal wackestone. The specimen 

was found in association with FaberophyUum sp.; (the 

genus indicates a late Meramec age.

Remarks. Lithostrotionella, sp. A shows close affinities to Lithostrotionella macouni (Lambe). LithostrotioneUa sp. A differs from L. macouni in a number 

of significant details, in possessing few lonsdaleoid dissepiments, better developed minor septa, major septa 

which are withdrawn from the axial region, and a
26 .CARBONATE FACIES AND CORALS, KOGRTJK FORMATION, BROOKS RANGE, ALASKA

thicker, better developed columella. Lithostrotionella sp. 

A differs from Lithostrotionella sp. B, in that the latter 

has major septa which extend to the columella, much 

longer minor septa, corallites which have a diameter 

1-2 mm larger, which have 1-2 less major septa, and 

which are more irregularly shaped.

Lithostrotionella sp. B

Plate 7, figures 7-9

Material. Specimen USNM 161028 is a fragment, 6 

by 6 by 8 cm, of a corallum collected 365 feet below the 

top of stratigraphic section 62C-31. The specimen was 

studied in two transverse and one longitudinal thin 

sections. The corallum retains much of the original 

microstructure and is preserved as calcite in a limestone 

matrix.

Description. Specimen USNM 161028 is cerioid. In 

transverse section it has somewhat uniform prismatic 

corallites that are 2.9-4.7 mm in diameter and that have 

9-12 major septa (figs. 26, 29). The major septa are 

typically 1.0-1.2 mm long, and many reach the columella. In all specimens minor septa are present between 

major septa and are 0.5-0.7 mm long. Dissepiments are 

regular to herringbone type with major and minor septa 

continuous from axial region to epitheca. Within some 

corallites a few lonsdaleoid dissepiments may be present 

at corners of the prismatic corallites. Lonsdaleoid dissepiments intercept 1-3 major septa. The columella is 

lens shaped, 1 mm long to 0.3 mm wide, and generally 

continuous with cardinal and counter septa. A few corallites are acolumellate with amplexoid septa. The septa 

are typically dilated in the tabularium.

FIGURE 29. Sections of Lithustrotionclla sp. B, USNM 161028.

In longitudinal section the dissepimentarium is 

about half the radius of the corallite and consists of 1, 

or rarely 2, rows of swollen and inflated dissepiments 

of which 9-13 occur in 5 mm. The tabulae are complete, 

dome shaped, and slope away from the colum°lla at 

angles of 20°-40°. The tabulae near the dissepimentarium may be reflexed to nearly horizontal before joining the dissepiments.

The microstructure of the corallum is similar to that 

of specimen USNM 161027.

Occurrence. Specimen USNM 161028 was collected 

365 feet below the top of measured section 62C-31 from 

the Kogruk Formation in the DeLong Mountains. 

Lithostrotionella sp. B is found in association with 

Faberophyllum spp., Lithostrotionella banffetms 

(Warren), and Sciophyllum cdaskaensis Armstrong 

(fig. 5). This association is late Meramec in age.

Coralla conspecific with Lithostrotwnetta sp. B have 

been collected, some 250 stratigraphic feet below the contact of the Lisburne Group with the Permian Siksikpuk 

Formation in a measured section at Skimo Creel- in the 

Endicott Mountains. At the Skimo Creek locality, 

Lithostrotionella sp. B is found in association with 

Chester age Foraminifera (B. L. Mamet oral comniun., 

March 1969).

Remarks. Lithostrotionella sp. B is very similar to 

Lithostrotionella macouni (Lambe). L. sp. B in comparison with the syntype of L. tnacouni (Lambe) has longer 

minor septa, septa that are more persistent in the dissepimentarium, major septa that are dilated in the 

tabularium, and a dissepimentarium which is commonly 

formed by a double row of dissepiments.

Lithostrotion mccoyanum Edwards and Haime var. 

mutungense Yii from the Visean of China Yii (1933, 

p. 91, pi. 18, figs. 3a-b) is similar to Lithostrotionella 

sp. B except for the presence of 2-3 rows of dissepiments in the dissepimentarium.

For a comparison of Lithostrotionella sp. B with 

Lithostrotionella sp. A, see discussion under the latter 

species.

Genus THYSANOPHYLLUM Nicholson and Thomson, 1876

Thysanophyllutn Nicholson and Thomson, 1876, Royal Soc.

Edinburgh Proc., v. 9, no. 95, p. 150. 

ThysanopJiyllitm Nicholson and Thomson. Thomson, 1880, Royal

Philos. Soc. Glasgow Proc., v. 12, p. 255. 

Thysanophyllum Nicholson and Thomson. Thomson, 18^3, Royal

Philos. Soc. Glasgow Proc., v. 14, p. 387. 

Thysanophyllum Nicholson and Thomson. Thomson, 192", Annals

and Mag. Nat. History, v. 18, p. 148. 

Lithostrotion Fleming, genornorph [Diphystrotion Smith and

Lang], 1930, Annals and Mag. Nat. History, v. 5, p. 184. 

ThysanophylluHi Nicholson and Thomson. Hill, 1940, Palaeontographical Soc., p. 160-162.
SYSTEMATIC PALEONTOLOGY 27

Tliysanophyllum Nicholson and Thomson. Hill, 1940, in Moore, 

R. C., ed., Treatise on invertebrate paleontology, Part F, 

Geol. Soc. America, p. 306.

Type species. Thysanophyllum orientale Thomson, 

1876, lower Carboniferous, Visean; Scotland.

Diagnosis. Compound rugose corals with a lonsdaleoid dissepimentarium; the septa are withdrawn 

from the axis except for the counter septum which may 

be very long, particularly in young stages; the tabulae 

are complete; typically they consist of flat-topped 

domes, but sometimes may be slightly sagging (Hill, 

1940, p. 161).

Thysanophyllum orientale Thomson 

Plate 8, figures 1-5

Tliysanophyllum orientale Thomson, 1880, Royal Philos. Soc.

Glasgow Proc., p. 257, text fig. 4, pi. 3, figs. 11, lla, 14, 14a. 

Tliysanophyllum orientale Thomson. Hill, 1940, Paleontographical Soc. Mon., p. 162,163, pi. 8, figs. 26-32. 

Thysanophyllum orientale Thomson. Jtill, 1967, Paleontological

Assoc., v. 10, pt. 4, text fig. 5, pi. 102, figs. 5a-b.

Material Specimen USNM 161018 is a 7 by 8 by 

12 cm fragment of a corallum collected by the writer 

within measured section 62C-31. Three transverse and 

four longitudinal thin sections were made. Specimen 

USNM 161019 was collected by Dr. Sigmund Snelson 

near Trail Creek, DeLong Mountains, from stratigraphic section 60A-400-403. This specimen is a 6 by 6 

by 10 cm fragment of a corallum. It has been cut into 

one transverse and one longitudinal thin section. Both 

specimens are preserved as calcite which has retained 

some of the original microstructure.

Description. Specimen USNM 161018 is a fragment 

of a cerioid corallum. In transverse thin section (pi. 8, 

fig. 2) the corallites are 9-19 mm in diameter and have 

23-28 major septa (fig. 30). Within the dissepimentarium the major septa are short, extending 1 mm or less 

from the epitheca. Minor septa are very short, poorly 

developed, and found between the major septa in only 

a few corallites. The major septa reappear near the 

tabularium wall, are 1.4-1.7 mm long, 200-300 microns 

thick near the wall, and taper both toward the axis and 

into the dissepimentarium. Minor septa are absent in 

the tabularium. Major septa are withdrawn from the 

axis. Dissepiments are lonsdaleoid and vary in size; the 

dissepiments typically intercept 2-1 septa. Columellae 

are rare and occur as small, 0.5-mm-long lathlike rods 

in the axial region.

In longitudinal section (pi. 8, fig. 3) the dissepimentarium consists of 2-5 rows of swollen uparched dissepiments of varying size. The dissepimentarium 

makes up about half the radius of the corallite. Tabulae 

are broad flat domes, which are bent downward 30°-45°

378-461 O 70 5

20

19

18

17

16 

CO 

LU 15

Id 

14

11

10

9

8 - 

7 -

EXPLANATION

 62C-31+1105; USNM 161018

 60A-401+0; USNM 161019

20 21 22 23 24 25 26 27 28 

NUMBER OF MAJOR SEPTA

29 30

FIGURE 30. Corallite diameter and number of major septa in 

Thysanophyllum orientale Thomson. Each symbol represents 

a single corallite.

within a distance of 1-1.5 mm from the dissepiir^ntarium.

The corallite wall is typically 200-300 microns thick, 

with a central dark-gray calcite band, 20 microns thick, 

normal to which fibrous calcite has been deposited (pi. 

8, fig. 1). The septa in the tabularium are composed of 

fibrous calcite. The dissepiments and tabulae are 20-30 

microns thick and composed of calcite crystals wHch 

range in size from 15-20 microns. An immature corallite some 10 mm in diameter has an isolated columella, 

1 mm long and 150 microns wide, that appears to be 

made of fibrous calcite crystals similar to the m?,jor 

septa.

Specimen USNM 161019 (pi. 8, figs. 4, 5; text fig. 31) 

differs from the above description by having typically 

26-29 major septa per corallite and few minor septa.

Occurrence. Thysanophyllum orientale Thomson, 

USNM 161018, was collected in about the middle of 

the Kogruk Formation, section 62C-31, DeLong Mountains (fig. 5). The specimen was found 1,105 feet below 

the top of the section in poorly sorted crinoid-bryozoan
28 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

FIGURE 31. Sections of Thysanophyllum orientate Thomson, 

USNM 161019.

wackestones. It is associated with Lithostrotion (Siph&nodendron) sinuosum (Kelly), Lithostrotion (Siplwnodendron} warreni Nelson, Lith-ostrotioneUa 

mclareni (Sutherland), and Sciophyllum Iwribarti 

Harker and McLaren.

T. one.ntale (USNM 161018) was also found in the 

Kogruk Fomiation near Trail Creek, DeLong Mountains, in section 60A-400-403 (fig. 7). This section is a 

continuous exposure of the Kogruk Formation about 

1,900 stratigraphic feet thick. The specimen was found 

about 70 feet below the top, in association with LithostrotioneUa birdi Armstrong.

The type species of T. orieMcH-e Thomson occurs in 

the shales of coral zone 3 age at Aberlady Bay, Scotland (Jull, 1967, p. 623; Hill, 1940, p. 162). Jull (p. 623- 

624) has collected and illustrated additional topotype 

material from this location.

Remarks. The Kogruk Formation specimens of 

ThysanophyUum orieniale Thomson compare closely 

to Hill's (1940, pi. 8, figs. 26, 27) illustrations of the 

lectotype from the Lower Limestone Series of Scotland 

(lower Carboniferous).

Thysanophyllum astraeiforme (Warren) 

Plate 9, figures 1-6

Diphyphyllum astraeiforme Warren, 1927, Canada Geol. Survey

Mem. 153, p. 44-45, pi. 3, figs. 2, 3; pi. 4, fig. 1. 

Lithostrotionella astraeiformis (Warren). Kelly, 1942, Jour.

Paleontology, v. 16, p. 352, 354. 

Lithostrotionella (TliysanopJiyllum) astraeiformis (Warren).

Nelson, 1960, Jour. Paleontology, v. 34, p. 115-117, pi. 22,

figs. 7-10. 

Lithostrotionella astraeiformis (Warren). Nelson, 1961, Geol.

Assoc. Canada Spec. Paper No. 2, pi. 18, figs. 1-3. 

Thysanophyllmn astraeiforme (Warren). Bamber, 1966, Canada

Geol. Survey Bull. 135, p. 23-26, pi. 4, figs. 3, 4. 

Thysanophyllum. astraeiforme- (Warren). Armstrong, 1970, U.S.

Geol. Survey Prof. Paper 534, p. 37-38, pi. 11, figs. 5-8.

Material. Two specimens are available for study, 

both of which were collected from measured stratigraphic sections. They are preserved as calcite which 

has retained some of the original microstructure. Specimen USNM 161025 is a 5 by 7 by 7 cm fragment of a 

corallum from which two transverse and one longitudinal thin sections were made. Specimen USNM 161026 

is an 8 by 10 by 10 cm fragment of a corallmr from 

which three transverse and two longitudinal thin sections were made.

Description. Specimen USNM 161025 is cerioid, and 

the typical mature corallite is 3.1-6.5 mm in diameter 

and has 14-16 major septa (figs. 32, 33). In trarsverse 

section (pi. 9, fig. 1) the major septa extend one-tlird to 

one-half the distance from the inside of the tabularium 

wall to the axial region. In some corallites, very short 

(less than 0.2 mm long) minor septa occur between the 

major septa. Major and minor septa are not developed 

in the dissepimentarium in the majority of cor-rllites, 

and where present, they are short ridges on the epitheca 

wall or short ridges on the upper surfaces of the dissepiments. The dissepimentarium has large lonsc'aleoid 

dissepiments which intercept the loci of 2-8 major septa.

A columella is present in most corallites and is formed 

by axial ends of the counter and (or) cardinal septa.

In longitudinal section (pi. 9, fig. 3) the dissepimentarium is continuous, one-third to one-half the width 

of the radius of the corallite, and consists of 1-8 rows 

of steeply inclined, swollen dissepiments. There are 

7-10 dissepiments in 10 mm. Tabulae are inclined 20°- 

35° near the dissepiments, frequently are flat to sHghtly 

domed in the axial region, and in a few specimens are 

upturned to meet the columella.

Corallite walls are 200-250 microns thick and have 

a central dark band 20-30 microns thick (pi. 9, fig. 2). 

The walls are composed of fibrous calcite crystals 

normal to the central band.

At the tabularium wall the major septa are 50-80 

microns thick and are composed of fibers of calcite 

with a central dark band. The walls of the tabulae and 

dissepiments are 20-30 microns thick and are formed 

by crystals of calcite ranging in size from 8 to 12 

microns.

Specimens USNM 161026 (pi. 9, fig. 4-6) is cerioid 

and has corallites which are typically 4.5-6.5 mm in 

diameter and which have 19-21 major septa. The major 

septa are best developed within the tabularium, where 

short minor septa are generally present. Major septa 

reach one-half to two-thirds the distance to the axial 

region. A columella is generally present but is not 

attached to the septa. Major and minor septa are well 

developed as ridges or projections on epitheca walls, 

varying from 0.1 to 1 mm in length. The dissepimentarium contains large and numerous lonsdaleoid 

dissepiments.
SYSTEMATIC PALEONTOLOGY 29

10

cc 

LJ 

H 5

UJ

EXPLANATION

Thysanophyllum astraeiforme (Warren)

 62C-31 + 1200; USNM 161025

 60A-429+10; USNM 161026

Thysnnophyllum sp. A

o 62C-15 +520: USNM 161006

13 14 15 16 17 18 19 20 21 22 23

NUMBER OF MAJOR SEPTA

24 25 26 27 28 29

FIGURE 32. Corallite diameter and number of major septa in Thysanophyllum astraeiforme (Warren) and TJiysanopJiyllum 

sp. A. Each unnuniberetd symbol represents a single corallite; if more than one corallite shows the same diameter and 

number of septa, the number of similar corallites isi shown.

Ill longitudinal section the dissepimentarium is onethird to one-half the radius of corallite and consists 

generally of a single row of dissepiments which are 

large, subquadrate, strongly convex, and steeply inclined. There are 4-6 in 5 mm. Tabulae are complete, 

dome shaped, and may be slightly uparched near the 

columella.

Occurrence. Specimen USNM 161025 was collected 

1,200 feet below the top of measured section 62C-31, in 

the Kogruk Formation, DeLong Mountains. It occurs

FIGURE 33. Sections of Thysanophyllum astraeiforme (Warren), USNM 161025.

with Thysanophyllum orientate Thomson, Sciophyllum 

lambarti Harker and McLaren, S. alaskaensis Armstrong, Lithostrotionella mclareni (Sutherland), Lithostrotionella aff. L. banffensis (Warren), and Lltlwstrotion (Siplionodendron) icarreni (Nelson) (fig. 3).

Specimen USNM 161026 was collected in the Cape 

Thompson Member of the Nasorak Formation south of 

Nasorak Creek, near Cape Thompson. Here it was fonnd 

in association with Litliostrotion (Siph-onodendron] 

sinuosum (Kelly),Z. (S.} warreni (Nelson), and Soiophylhvm sp. A.

Armstrong (1970) reports T. astraeiforme from the 

limestone and chert member of the Peratrovich Formation, northwest coast of Prince of Wales Island, southeastern Alaska, in association with a fauna of Fabvrophyllutn spp., lithostrotionid corals, and Foraminifera 

of late Meramec age.

Bamber (1966) reports T. astraeiforme (Warren) 

from the Rmidle Group near Banff, Alberta, and in the 

upper Mount Head Formation of the Rocky Mountains 

of southern British Columbia and Alberta.

Macqueen and Bamber (1968, p. 264, figs. 7, 8) report 

T. astraeiforme (Warren) from their faunal zones 3 

and 4 in the Mount Head Formation, southwestern 

Alberta.

T. astraeiforme appears to be a common, widespread
30 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

index fossil to Meramec age rocks in western Canada 

and Alaska.

Remarks. Specimen USNM 161025 differs from the 

lectotype described by Bamber (1966, p. 23-24) by having some corallites which show, in longitudinal section, 

an additional row of dissepiments. In transverse section 

specimen USNM 161025 differs from the type specimens 

by having in corallites of equal diameter 3-4 additional 

major septa.

Specimen USNM 161026 is with some hesitation 

placed with the species ThysatwphyUum astraeiforrne 

(Warren). It differs from the type specimens of the 

species as described by Bamber (1966) by having in 

corallites of equal size 4-6 more major septa, by having 

major and minor septa which are relatively well 

developed and which are long projections from the 

epitheca, and by having much smaller and more abundant lonsdaleoid dissepiments.

Thysanophyllum sp. A 

Plate 11, figures 1-3

MaterM. Specimen USNM 161006 is a 7 by 9 by 

10 cm fragment of a corallum collected from 520 feet 

below the top of section 62C-15. The corallum is preserved as calcite in a limestone matrix. Within the corallum many corallites were crushed before lithification. 

The specimen was studied in three transverse and four 

longitudinal thin sections.

Description. Specimen USNM 161006 (pi. 11, figs. 

1-3) is cerioid. In transverse thin section, corallites are 

from 3.5 to 9.5 mm in diameter, and the dissepimentarium is from 1.5 to 3 mm wide. The major septa are 

essentially restricted to the tabularium and are 1.25-1.6 

mm long. Major septa where developed in the dissepimentarium are short, ridges on the epitheca. Minor septa 

are absent in all corallites studied. The dissepiments 

are lonsdaleoid.

The majority of corallites lack columellae. Where 

columellae are present, they are thin and lath shaped

FIGURE 34. Sections of Thysanophyllum sp. A, USNM 161006.

and generally not connected to the septa. A few corallites have lens-shaped columellae that are attached to 

the cardinal and the counter septa (fig. 34).

In longitudinal section, corallites with a columella 

have a dissepimentariuni composed (pi. 11, fig. 3) of 2-3 

rows of globose dissepiments of which 4-6 occur in 5 mm. 

Many tabulae are incomplete and dome shaped and are 

slightly reflexed upward near the columella. The tabulae 

in the axial region slope downward from the columella 

10°-20°, and with 0.5-1.0 mm of the dissepimentariuni 

they are reflexed downward 30°-45°. Corallites which 

are acolumellate have dome-shaped tabulae in the axial 

region with steeply inclined margins near the 

disse pimentarium.

The epitheca (pi. 11, fig. 1) is about 200-300 microns 

thick and contains a central dark-gray band 30-40 microns thick. The epitheca is composed of fibers of cr.lcite 

deposited with their long axes normal to the central 

dark-gray band. Within the tabularium the major septa 

are 150-170 microns thick at their bases and taper 

towards the axial region. The septa in transverse section 

are characterized by a central dark band 10-20 microns 

thick, on which fibrous calcite crystal are deposited at 

angles of 35°^0°.

Occurrence. Only one specimen of Th-ysanophyttum 

sp. A is known from the Lisburne Group of Alaska. It is 

represented by specimen USNM 161006, which was collected 520 feet below the top of section 62C-15, Kogruk 

Formation, DeLong Mountains (fig. 3). It is found in 

association with Lithostroti-onella banffensis (Warden), 

Lithastrotionella mclareni (Sutherland), and Faberophyllum sp. The coral fauna is of Meramec age.

Remarks. Thysa/nophyllum sp. A resembles Thysanophyllmn astraeiforme (Warren) in its development of the septa within the tabularium and in its 

lonsdaleoid dissepiments in the dissepimentariun. It 

differs from the latter species by having corallites which 

are typically 2-3 mm larger in diameter and which 

have 22-28 major septa (fig. 32).

ThysanopJiyUinn orientale Thomson differs from 

Thysanophyllum sp. A by having corallites of marly 

twice the diameter with well-deveoped minor septa.

The description of Thysanophylhim sp. A is based on 

a single fragment of a corallum in which many of the 

individual corallites were crushed before lithificg.tion. 

The material is considered inadequate for a detailed 

description of a new species.

Genus SCIOPHYLLUM Harker and McLaren, 1950

Sciophyllum Harker and McLaren, 1950, Canala Geol. Survey

Bull. 15, p. 31. 

Sciophyllum Harker and McLaren. Hill, 1956, in Moore, R. C.,

ed., Treatise on invertebrate paleontology, part F, Geol.

Soc. America, p. F307.
SYSTEMATIC PALEONTOLOGY 31

Sciophyllum Harker and McLaren. Sando, 1965, U.S. Geol. Survey Prof. Paper 503-E, p. E29.

Type species. Sciophyttum lambarti Harker and| 

McLaren (1950 p. 31-33, pi. 4), Mississippian, Canada.

Diagnosis. Cerioid rugose corals of basaltiform 

habit, without columella; complete corallum unknown; 

dissepimentarium of one or more series of dissepiments, 

the imier margin forming a well-marked inner wall; 

tabulae strong, well spaced and regular, flat or slightly 

arched; septa absent or reduced to fine vertical striations on the inner side of the epitheca or inside the inner 

wall; gemmation laterial (Harker and McLaren, 1950, 

p. 31).

Sciophyllum lambarti Harker and McLaren 

Plate 6, figures 3-6

Sciophyllum lambarti Harker and McLaren, 1950, Canada Geol. 

Survey Bull. 15, p. 31-33, pi. 4, figs. 1-4.

Material. Two specimens are available for study, 

and both are fragments approximately 8 by 8 by 10 cm, 

collected from two coralla found in measured stratigraphic sections. Specimen USNM 161015 was collected 

from a dolomitic packstone in section 62C-31. From 

this specimen two transverse thin sections with 94 

corallites and three longitudinal thin sections with 18 

corallites were made. Specimen USNM 161017 was collected from the measured section at Gape Thompson, 

and one transverse thin section with 40 corallites and 

one longitudinal thin, section with five corallites were 

made.

Description. Specimen USNM 161015 is cerioid and 

has prismatic corallites that are typically 3-4 mm in 

diameter. In transverse section (pi. 6, fig. 6) the traces 

of 1 or 2 large dissepiments are generally present. Some 

parts of various corallites are devoid of dissepiment. 

Where present, the dissepimentariimi occupies about 

one-half the radius of the corallites. Septa are poorly 

developed and vestigial and on the inside of the tabularium wall as short ridges less than 0.1 mm long 

(fig. 35).

In longitudinal section (pi. 6, fig. 5) some corallites 

have a dissepiment arium that consists of a single row 

of large inflated, steeply inclined dissepiments of which 

there are 5-8 in 5 mm. Tabulae are essentially flat, and 

there are 6-8 in 5 mm. In corallites without a dissepimentarium, the tabulae are flat and extend horizontally 

across the corallites, normal to the epitheca.

The corallite walls are 80-110 microns thick and 

have a median dark-gray calcite band 20 microns 

thick. The walls are composed of fibrous calcite 

deposited normal to the central band. The walls .of the 

dissepiments are thin, only some 15 microns thick, and 

are formed by very small (10 microns or less) crystals

FIGURE 35. Sections of Sciophyllum lambarti Harker and 

MeLaren, USNM 161015.

of interlocking calcite. The tabulae have thin walls, 

only 20-25 microns thick, and are made of crystals of 

calcite which range in size from 10 to 15 microns.

Specimen USNM 161017 (pi. 6, figs. 3, 4), from the 

upper member of the Nasorak Formation near Cape 

Thompson, in transverse section, has corallites which 

are typically 3 1.5 mm in diameter. The corallites have 

short septa on the epitheca and on the inside of the 

tabularium wall. All corallites studied have a dis^epimentarium composed of relatively small lonsdaleoid 

dissepiments. In longitudinal section the dissepimentarium is about half the radius, composed of a single 

to double row of swollen dissepiments of which 10-14 

occur in 5 mm. The tabulae are weakly convex near the 

dissepiments and nearly horizontal in the axial region, 

9-13 tabulae occurring in 5 mm. Microstructure is similar to specimen USNM 161015 which is decribed above.

Occurrence. 8. lambarti, in the Kogruk Formation 

of the DeLong Mountains and the Nasorak Formation 

near Cape Thompson, has been collected in beds which 

contain a diversified coral fauna of Meramec age. Specimen USNM 161015 was collected from the Kogruk 

Formation, western DeLong Mountains, 1,320 feet below 

the top of measured section 62C-31 (fig. 5). It occurs 

in association with LithostrotioneUa nwlareni (Sutherland), Llthostrotionella aff. L. banffensis (Warren), 

Tkysa-nophyllmn sp., Lithostrotion (tSiphonodendron) 

simiosum (Kelly), and Lithostrotion (Siphonodendron) warreni Nelson.

8. lambarti was collected by the writer in 1962 near 

Cape Thompson south of Nasorak Creek from the 

upper member of the Nasorak Formation as defined 

by Campbell (1967, p. 44-45, pi. 2B) and was found in
32 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

association with Lithostrotionella nwlareni (Sutherland) and Lithostrotionella banffetisis (Warren).

Harker and McLaren's (1950, p. 30-31) holotype of 

3. lambarti is described as having been collected "from 

the Carboniferous of the Yukon-Alaska boundary, long 

141° W., lat 68°48'40" N." They thought it possibly 

came "from a Mississippian horizon."

Remarks. Specimen USNM 161015 from section 

62C-31, Kogruk Formation, DeLong Mountains, differs 

from the illustration and description of the holotype of 

fS. lambarti Harker and McLaren (1950) by having a 

number of corallites which are devoid of dissepiments. 

Furthermore, in those corallites which have a dissepimentarium, the dissepiments are in only one series and 

are larger in size. The corallites are devoid of septa in 

the dissepimentarium and on the epitheca wall. This 

specimen does conform to the holotype in corallite 

diameter.

Specimen USNM 161017 from the Nasorak Formation resembles in most respects the holotype of Sciopliyllum lambarti as defined by Harker and McLaren 

(1950).

Sando's (1965, p. E29-E31) description of the lectotype of SciophyUum adjunctivum (White) from the 

Upper Mississippian of southeastern Idaho mentions 

that corallites are as large as 9 mm in diameter and 

that most of the tabulae are concave or inclined. S. 

adjunctivum is characterized by a single row of large 

dissepiments and absence of septa in the dissepimentarium.

Lithostrotionella mclareni (Sutherland) from the 

Kogruk Formation is exemplified by specimens USNM 

161003 (pi. 6, figs. 1, 2) from 520 feet below the top 

of section 62C-15; USNM 161016 from 1,390 feet below 

the top of section 62C-31; and USNM 161030 (pi. 6, 

figs. 8, 9) from 1,100 feet below the top of section 60A400 103; these specimens have columellae in a majority 

of the corallites and have septa typical of the genus 

Lifhostrotionella. A few corallites within these coralla 

may have morphology of the genera Thysanophyllum 

and Sciophylfaim. Furthermore there are clusters of 

corallites within these coralla which have the morphology of Sciophyllum lambarti. Both L. mclareni and 

/$. lambarti have similar stratigraphic ranges within 

the Kogruk Formation.

The collection of L. mclareni from the Kogruk Formation suggests that 8. hunbarti was possibly derived 

from the, former by elimination of the columella, peripheral withdrawal of the septa, development of large 

lonsdaleoid dissepiments, and development of horizontal tabulae.

SciophyUum alaskaensis Armstrong 

Plate 10, figures 2-6

Sciophyttiini alaskaensis Armstrong, 1970, U.S. Geol. Survey 

Prof. Paper 534, p. 38, 39, pi. 11, figs. 1-4.

Material. Fragments of three coralla were collected 

from two measured sections of the Kogruk Formation 

in the DeLong Mountains. Each specimen was about 6 

by 8 by 8 cm. Three transverse thin sections were made 

from specimen USNM 161020 and showed 65 corallites. 

From specimen USNM 161021 the two transverse thin 

sections made showed 40 corallites, and the three longitudinal thin sections, seven corallites. From specimen 

USNM 161022 the, seven transverse thin sections made 

showed 43 corallites, and the five longitudinal thin sections, 18 corallites. All the specimens have the corallites 

preserved as calcite and the internal voids filled with 

sparry calcite and minor amounts of chalcedony. The 

microstructure has undergone calcite neomorphism and 

has also been affected by grain growth and penetrated 

by sparry calcite crystals.

Description. Specimen USNM 161020 (pi. 10, figs. 

4, 5) has a cerioid corallum. In transverse section the 

average mature corallite is from 6.0 to 8.7 mm in diameter. The dissepimentarium occupies 25-35 percent of 

the corallite diameter and consists of lonsdaleoid dissepiments which intercept from 2 to 5 major septa. 

Short major and minor septa project from the epitheca 

into the dissepimentarium (pi. 10, fig. 5). The discontinuous major and minor septa may reappear on the 

inner wall of the tabularium. Here they range in length 

from 0.1 to 0.5 mm. The development of the m?,jor and 

minor septa varies in different corallites. All corallites 

studied are devoid of columellae. Corallites with a diameter less than 4 mm have major septa which tend to 

be persistent in the dissepimentarium from the epitheca 

to the tabularium wall but which are withdrawn from 

the axial region of the corallite (fig. 36).

FIGURE 36. Sections of SciopJiyllum alaskaensis Armstrong: 

A, USNM 161020; B, C, USNM 161021.
SYSTEMATIC PALEONTOLOGY 33

In longitudinal section the dissepimentarinm is a 

single to double row of large, inflated and steeply inclined dissepiments of which there are 4-6 in 5 mm. 

The tabulae are complete, flat to slightly concave in the 

axial region; some are reflexed downward 10°-35° near 

the dissepimentarium.

Microstructure (pi. 10, fig. 5) is poorly preserved 

owing to extensive calcite neomorphism in particular, 

grain growth of the sparry calcite which fills the 

internal voids of the corallites. The corallite walls are 

150-200 microns thick and have a central band, 20 

microns thick, of dark-gray calcite. The epitheca is 

formed by fibrous calcite deposited at right angles to 

and on both sides of the dark-gray band. The septa 

appear to have been thin, less than 100 microns thick. 

In the tabularium the major septa are 100-120 microns 

thick and are composed of fibrous calcite. The tabulae 

and dissepiment walls have been affected by calcite 

neomorphism but appear to have been very thin, less 

than 40 microns thick (pi. 10, fig. 5).

Specimen USNM 161021 (pi. 10, figs. 2, 3) has corallites which are typically 4.5-6.5 mm. in diameter and 

has septa which are irregularly and inconsistently 

developed on the epitheca and on the inside of the tabularium wall. In other respects it is similar to specimen 

USNM 161020 (fig. 36).

Specimen USNM 161022 (pi. 10, fig. 6), which is 

with reservation assigned to this species, has corallites 

which are 6-8.5 mm in diameter. Minor septa are absent, 

and the major septa are developed only on the epitheca 

or in the dissepimentarium of a few corallites. The septa 

in the tabularium are inconsistently developed on the 

tabularium wall. The dissepimentarium occupies about 

half the radius of the corallites, and the dissepiments 

are large and lonsdaleoid.

Occurrence. Sciophyllmn alaskaensis was found in 

the Kogruk Formation, DeLong Mountains, 515 feet 

(USNM 161020) and 1,075 feet (USNM 161021) below 

the top of stratigraphic section 62C-31 (fig. 5). In 

section 62C-15 it was found about 300 feet (USNM 

161022) below the top. S. alaskaensis is found in the 

Kogruk Formation in association with Faberopkyllum 

spp., fS. lanibarti Harker and McLaren, Litliostrotionella mclareni (Sutherland), Thysanophyllum, astraeiforme (Warren), Thysanophylliun orientale Thomson, 

and Lithostrotionella banffensis (Warren) (fig. 3).

The holotype (Armstrong, 1970) of S. alaskaensis 

was described from the limestone and chert member, 

Peratrovich Formation, northwest coast, Prince of 

Wales Island, southeastern Alaska. There the species 

occurs with Faberophyllum, g'trtyi Armstrong, Fdherophyllum witticunsi Armstrong, L. banffemis, and T.

astraeiforme, and a large fauna of Meramo-c 

Foraminifera.

Remarks. Sciophyllum alaskaensis, as defined by 

Armstrong (1970) from material collected from the 

Peratrovich Formation, northwest side Prince of Wales 

Island, southeastern Alaska, has a double row of dissepiments. It differs from S. adjunctivuin (White) as 

redescribed by Sando (1965, p. E29-E31) and the holotype of S. lambarti as described by Harker and 

McLaren (1950, p. 31-33), both of which have only a 

single row of dissepiments. Furthermore, 8. adjunctivum has tabulae which are concave and septa which 

are inconsistently present on the inner side of the tafrilarium wall and absent on the corallite wall. /S. lambarti 

is distinguished from S. alaskaensis by the former's 

smaller corallite diameter of only 4.6-5.0 mm and less 

developed septa.

The concept of S. alaskaensis is expanded in this 

study to cover a wider variation of septal degeneration 

and development of lonsdaleoid dissepiments. Specimen 

USNM 161020 closely resembles the holotype from 

southeastern Alaska. Specimen USNM 161021, found 

560 feet stratigraphically below specimen USNM 

161020 in the Kogruk Formation, is similar in mcst 

respects, but typical corallites are about 2 mm smaller 

in diameter, and the tabulae tend to sag or be concave.

Specimens USNM 161020 and 161021 may have been 

derived from a Tliymnophyllum astraeiforme (Warren) lineage, as the holotype of S. ala-skaensis may have 

been, by the elimination of the columella and further 

degeneration of the septa. The holotype and paratyp^s 

of the species from the Peratrovich Formation, Prince 

of Wales Island, southeastern Alaska, also strongly 

suggest T. astraeiforme lineage.

Specimen USNM 161022, from 300 feet below the 

top of section 61C-15 which is with considerable reservation assigned to this species probably is of a different phylogenic lineage. It is characterized by very 

degenerate major septa, large irregularly developed 

lonsdaleoid dissepiments and irregularly shaped corrllites. This specimen may possibly be derived from the 

Lithostrot'wnella birdi Armstrong lineage. An example 

of this latter species, specimen LTSNM 161023, has some 

corallites (pi. 5, figs. 1, 2) which are strongly suggestive of specimen USNM 161022. (See, remarks und^r 

L. lirdi.)

Sciophyllum sp. A

Plate 11, figures 4-7

Material. Specimen USNM 161029 is the only example of Sciophyllum sp. A collected by the writer from 

the Lisburne Group in Alaska. It is a 6 by 6 by 8 cm, 

fragment of a corallum.
34 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

A significant proportion of the corallites within the 

corallum were crushed before lithification. Thacorallum 

is preserved as calcite and is in a limestone matrix. Thin 

section studies were made on three transverse thin sections with 12 corallites and two longitudinal thin sections with 5 corallites. (See fig. 37 for transverse and 

longitudinal section).

Description. The corallum is cerioid. In transverse 

thin section (pi. 11, fig. 6) average mature corallites 

are 12-15 mm in diameter. The dissepimentarium occupies about 50 percent of the corallite diameter and is 

a series of tightly packed lonsdaleoid dissepiments. 

Major septa are absent on the epitheca of mature corallites. On the epitheca of corallites under 8 mm in diameter there may be short major septa that are ridges 

100-150 microns long. In some corallites major septa 

may occur on the inside of the tabularium wall as short 

spikes 100-200 microns long. As many as 20-24 major 

septa can be developed; minor septa are absent.

In longitudinal section the dissepimentarium is 2-4 

rows of inflated, steeply inclined dissepiments of which 

6-10 occur in 5 mm. Tabulae are complete, are flat to 

slightly convex, and have their greatest convexity near 

their junction with the dissepiments. There are ordinarily 12-15 tabulae in 5 mm (fig. 37).

The epitheca walls in transverse section (pi. 11, fig. 7) 

are between 350 and 450 microns thick and have a central dark band of calcite 50 microns thick. Fibrous calcite deposited at right angles to the central dark band 

forms the corallite walls. The spikelike septal ridges 

on the epitheca are formed by calcite which is in optical 

continuity with the fibrous calcite of the corallite wall. 

The short major septa on the inside of the tabularium 

where present, are also formed by fibrous calcite. In 

longitudinal section the walls of the dissepimentarium 

and tabulae are 20-30 microns thick and are composed of 

interlocking calcite crystals ranging in size from 10 to 

20 microns.

FIGURE 37. Sections of Sciophyllum sp. A, USNM 161029.

The voids within the corallum are filled with 0.2-0.4 

mm crystals of sparry calcite.

Occurrence. The only known example of Sciophyllum sp. A was collected in 1962 from the upp^r 50 feet 

of the lower member of the Nasorak Formation as defined by Campbell (1967, pi. 2B) south of Nasorak 

Creek near Cape Thompson. It occurs in association 

with Lithostrotion (Siphonodendron) sinuosum 

(Kelly), L. (S.) warreni Nelson, and Thysanophyllum astraeiforme (Warren), which indicate a Meramec 

age.

Remarks. Specimen 161029, on which the description 

of Sciophyllum sp. A is based, is the only example of 

this form of Sciophyllum known by the writer from the 

Lisburne Group, and it has many crushed cor<r.llites.

Sciophyllum lambarti Harker and McLaren, which 

occurs in the Lisburne Group, is easily dist;nguished 

from Sciophyllum sp. A by the former's smaller corallite diameter of 4.5-5 mm and single row of large lonsdaleoid dissepiments.

Sciophyllum alaxkaensis Armstrong, wHch also 

occurs in the Lisburne Group of northwestern Alaska, 

is separated from Sciophyllum sp. A by the latter's 

smaller corallite diameter of 6.0-8.5 mm, narrower dissepimentarium, better developed and larger lonsdaleoid 

dissepiments.

Sciophyllum adjunctivum (White) as rede^cribed by 

Sando (1965, p. E29-E31) has concave tabulae, large 

lonsdaleoid dissepiments, and smaller corallite 

diameters.

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36 CARBONATE FACIES AND CORALS, KOGRUK FORMATION, BROOKS RANGE, ALASKA

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Mem. 153, 94 p., 7 pis. 

Wilson, J. L., 1967a, Microfacies and sedimentary structures in

deeper-water lime mudstones [abs.] : Am. Assoc. Petroleum

Geologists Bull., v. 51, no. 3, p. 485-486.

 IQGTb, Cyclic and reciprocal sedimentation in Virgilian 

strata of southern New Mexico: Geol. Soc. America Bull., 

v. 78, no. 7, p. 805-818,4 pis., 4 figs.

 1967c, Carbonate evaporite cycles in Lower Duperow Formation of Williston Basin: Canadian Petroleum Geology 

Bull., v. 15, no. 3, p. 230-312, 22 pis., 14 figs.

 1969, Microfacies and sedimentary structures in 

"deeper water" lime mudstones in Friedman, G. M., ed.,

Depositional environments in carbonate rocks: Toe. Bcon.

Paleontologists and Mineralogists Spec. Pub. 14, p. 4-17, 5

figs. 

Yabe, Hisakatsu, and Hayakawa. Ichiro, 1915, Palaeozoic corals

from Japan, Korea, and China: Jour. Geol. Soc. Tokyo, v.

22, no. 264, p. 98-109. 

Yii, C. C., 1933, Lower Carboniferous corals of Chira: China

Geol. Survey, Palaeontologica Sinica, ser. B, v. 12, pt. 3, 211

p., 24 pis. 

 1937, The Fenginian (lower Carboniferous) corals of

south China: Acad. Sinica, Inst. Geology and Paleontology,

Chi-K'an Mem., no. 16, 111 p., 13 pis.
INDEX

[Italic page numbers indicate both major references and descriptions]

Page 

Aberlady Bay___________....____ 28

Acknowledgments___..-..___.___. / 

adjunctivum, Sciophyllum.................. 32,33,34

Age and correlation...__................... 8

Alapah Limestone___-_..._....... 8,15,16

alaskaensis, Sciophyllum...................... 8,

14,18,21, 22, 26, 29, 32, 34; pi. 10 

Algae, calcareous....__________. 7,8

asiatica, Lithostrotion (Siphonodendron) irregulare............................. 12

astraeiforme, Diphyphyllum................... 28

Thysanophyttum.......................... 8,

10,14,15,18, 21,28,30,33,34; pi. 9 

astraeiformis, Lithostrotionella................. 28

Lithostrotionella (Thysanophyttum)........ 28

banffense, Lithostrotion........................ 16

banffensis, Lithostrotionella.................... 8,

10,14, 16,19, 21, 22,26, 29,30,31,32,33; pis.

3,4,10

birdi, Lithostrotionella..... 8,14,20,23,28,33; pis. 4,5 

Brachiopods___-...-__._._____ 8 

Brooks Range__.________....____ 8,15

Calcitic dolomites..________...____ 8

Cape Lewis. ____.________.____ 9

Cape Thompson....______________ 1,

10,14,15,18,29,31,34; pis. 2, 6,9,11 

Cape Thompson Member of the Nasarok Formation........... 10,14,15,29; pis. 2,9

Carbonate facies__....________.__ 3,4

C arbonate rocks, classification__. ___... l

types______.________.____ 6

Chester Range Group_________.__ 9

Coffee Creek Formation____ .___ 15

Coral faunas, lithostrotionid__ ___.__ 8, 9

Crinoid grainstone......_..--._--..._.. 6

Crinoid wackes tones...____..__..__ 8

Crinoid-bryozoan wackestones.. ___. __ 27

DeLong Mountains..._______.__.__ 1,

2, 8, 9, 10, 11, 13, 14, 18, 20, 21, 22, 26,

27, 28, 29, 30, 31, 32, 33; pis. 1, 2, 3, 4,

5,6, 7,8,9,10,11,13,14

Deposition environments.._._............ 3

Diphyphyllum................................ 9

astraeiforme............................... 28

klawockensti.............................. 9,18

sinuosum................................. 9

venosum.. ..----__--._ -.-...-... 9,18

(Diphyphyllum), Lithostrotion, sp. A..____ 13 

Dolomites.._..__._.................. 8

Duperow Formation..__._......._.._.. 4

Echinoderm-bryozoan grainstones -.-.-. _... 8 

packstones..__._______...____ 3,6,7 

wackestones._.................._..... 3,6,7

Echinoderm-foraminiferal wackestone. _. _ 25 

Endicott Mountains_-..._._._-------- 8,26

Faberophyllum................................ 9,24

girtyi................................ 8,18,21,33

leathamense............................... 8

williamsi.............................. 18,21,33

sp..................................... 18,25,30

spp.................... 8,9,10,18,21,22,26,29,33

Page

Facies, carbonate ______ . __ _____ . 3 

flexuosum, Lithostrotion. ..... .. .... . ..... ..... 9

floriformis, Lithostrotionella ..... .............. 16, 19

Foraminifera. . ____ ___ .... ___ ... 6,7,8,14

FossQ Point....... .................... 24; pi. 12

girtyi, FaberophyUum. ................... 8,18,21,33

Grainstones, crinoid ___ ... _ __ ___ ... 6

echinoderm-bryozoan...... _ _____ . 8

oaid................... .................... 3,7

oolitic-....-.---.-.--.--- . ..-- 6,7

Great Basin ________ . ___________ 9

Great Blue Limestone... -... __ . ___ . 9

Hulahula River. 9

Introduction......__________..... 1

irregulare, var. asiatica, Lithostrotion (Siphoncdendron).......................... 12

klawockensis, Diphyphyllum................... 9,18

Kogruk Formation__. ________.__. 1,

2, 3, 4, 7, 8, 9,10, 11, 12, 14,18, 20, 21,

22, 24, 26, 27, 28, 29, 30, 31, 32, 33; pis.

1,2,3,4,5,6,7,8,9,10,11,13,14

Kukpuk River....--.-.-_............... 1

lambarti, Sciophyllum......................... 8,

10,14,18,22,28,29, 31, 33,34; pi. 6 

leathamense, Faberophyllum___.....___ 8

Lisburne Group..-. 8, 9,11,12,13,14,15,16, 26,30,34 

Lisburne Hills.. ................ 1; pis. 7,14

Lithostrotion.......................... 9,21,22,23,26

banffense................................. 16

flexuosum................................. 9

macouni.................................. 23

mccoyanum mutungense................... 25,26

pauciradiale.............................. 9,12

pauciradialis.............................. 9

sinuosum................................. 9

striatum.................................. 9

trimorphum............................... 24,25

volkovae................................... 12

warreni................................... 13

sp..-..... - 21

(Diphyphyllum) sp. A........ .... 13

[Lithostrotionella] [Thysanophyttum] mclareni............. ................ 21

(Siphonodendron) irregulare var. asiatica... 12 

mutabile.. .......................... 13

oculinum.......................... 12,14,16

oregonensis........................... 15

sinuosum............................. 8,

9, IS, 14,18,20, 28,29,31,34; pis. 1,3 

warreni............................... 8.

10, IS, 15,16,18,20, 28,29,31,34; pis. 1, 2 

sp. A . 14,/5;pl, 2

Lithostrotionella............. 14, 18, 18,21, 22, 23,34,32

astraeiformis............................ 28

banffense................................. 16

banffensis................................. 8,

10, 14, 16, 19, 21, 22, 26, 29, 30, 31, 32, 

33; pis. 3,4,10 

birdi.................. 8,14, 20,23,28,33; pis.4,5

floriformis....... ......._._._..._. 16,19

Lithostrotionella Continued Page 

lochmanae................................ 24

macouni...................... 23, 25, 26; pi. 12

mclareni.................................. 8,

9,10,14,18,20,2/, 24, 28, 29, 30, 31, F2, 

33; pis. 5, 6 

micra..................................... 24

pennsylvanica........................ 9,14,18,21

unicum................................... 16

vesicularis................................ 16,19

sp. A.... .............. 8, 24, 25, 26; pi. 7

sp. B. .............. 8, 18, 24, 25, 26; pi. 7

(Thysanophyttum) astraeiformis........... 28

Lithostrotionid coral faunas. ____...__.. 8 9 

Lithostrotionidae....________.____ 9

Livingstone Formation_____....__.... 10

lochmanae, Lithostrotionella................... 24

Lonsdaleiidae....____. .. ... 16

Lower Limestone Series of Scotland. _ __. 28

macouni, Lithostrotion...........-.-...-..-... 23

Lithostrotionella................. 23, 25, 26; pi. 12

mccoyanum mutungense, Lithostrotion......... 25,26

mclareni, Lithostrotionella..................... 8,

9,10,14,18, 20,2/, 24, 28,29,30,31, 32,

33; pis. 5, 6 

micra, Lithostrotionella........................ 24

Mount Head Formation.-------- 8,9,10,14,22,29

Mudstones, marine lime. . 6 

mutabile, Lithostrotion (Siphonodendron)...... 13

mutungense, Lithostrotion mccoyanum......... 25,26

Nasorak Creek.... 10,14,15,18,29,31,34

Nasorak Formation. 15, 18, 31, 32; pis. 2, 3, 6, 11 

Nasarok Formation, Cape Thompson Member.-- - 10, 14, 15; pl.s 2, 9 

Niak Creek............ . . 9

Nunaviksok Creek... .... 13

oculinum, Lithostrotion (Siphonodendron)... 12,14,16

Ooid grainstones _.---. -... 3,7

Ooid packstones... - ...... - - 6

Oolitic grainstones------- - - f, 7

oregonensis, Lithostrotion (Siphonodendron).... 15

orientate, Thysanophyttum.. 8,14, 27, 29, 30, 33; pi 8

Ostracoda..._ - - -- f, 7

Packstones, echinoderm-bryozoan 3, e, 7

nondolomitized-__... -- 3 

ooid___._____..... ----- 6

pauciradiale, Lithostrotion..................... 9,12

pauciradialis, Lithostrotion.................... 9

Peace River. ------- 10, 24; pi. 12

pennsylvanica, Lithostrotionella........... 9,14,18,21

Perapertu Formation.. - 24

Peratrovich Formation........ 6,8,9,14,18,19,29,33

Previous work-._... .. . ........ 2

Prince of Wales Island......... 6,8,9,14,18,19,29,33

Prophet Formation..... . 10

Redwall Limestone-..-...-- --- - 14 

Regional setting-. . - * 

Romanzof Mountains.. . 9 

Rugosa.___ .--. - 9 

Rundle Group_...... -.... -------- 29

Rundle Limestone.. - -- 18

37
38 INDEX

Page 

Sclophyllum......................... 21,22,23,30,32

adjunctivum. ____.______.__ 32,33,34 

alaskaensis. 8, 14, 18, 21, 22, 26, 29, 32, 34; pi. 10 

lambarti... 8, 10,14,18, 22, 28, 29, 31, 33, 34; pi. 6 

sp. A... .............. 10,14,15, 29, 33; pi. 11

Shainin Lake .- . 8,15,16

Shell Oil Co-- ........................... 1

Siksikpuk Formation,-___.....______ 26

sinuosum,Diphyphyttum...................... 9

Lithostrotion.............................. 9

(Siphonodendron)......... _____-- 8,

9, 1%, 14,18, 20, 28, 29, 31, 34; pis. 1, 3 

Siphonodendron............................... 9, 13

(Siphonodendron) irregulare, Lithostrotion..... 12

mutabile, Lithostrotion........... __-- ._ 13

oculinum, Lithostrotion................. 12,14,16

oregonensis, Lithostrotion.................. 15

sinuosum, Lithostrotion................ ... 8,

9, Ut 14, 18, 20, 28, 29, 31, 34; pis. 1, 3

Page

(Siphonodendron) irregulare, Lithostrotion Con. 

warreni, Lithostrotion..................... 8,

10, 13, 15,16, 18, 20, 28, 29, 31, 34; pis.

1,2

sp. A, Lithostrotion................ 14, IB; pi. 2

Skimo Creek..______. ________- 26 

Stoney Mountain,____.__.__.-__ _-_. 18 

striatum, Lithostrotion......................... 9

Systematic paleontology ....--- 9

ThysanophyUum..................... 21,2z,, 26, 27,32

astraeiforme.... 8,10,14,15,18, 28, 30,33,34; pi. 9

orientate.. ........... 8,14, 27, 29, 30, 33; pi. 8

sp. A......................... 18, 22, 30; pi. 11

sp ........ . 31

(ThysanophyUum) astraeiformte, Lithostrotionella............................... 28

TrailCreek.. 1,27,28

trimorphum, Lithostrotion..................... 24,25

Tupik Formation.___._._______ 3

Tupik Mountain..... __ 

Turner Valley Formation.

Page

2

3

unicum, LithostrotioneHa... ________.-. 16 

Utukok Formation....... 2, 3,11, If; pis. 1, 3,13

venosum, DiphyphyUum....................... 9,18

vesicularis, Ltthostrotionetta.................. - 16,19

tolkovae, Lithostrotion......................... 12

Wackestones, crinoid..__ _ _._.-. 8 

crinoid-bryozoan. ___.-_..______. 27 

echinoderm-bryozoan_..________-- 3,5,7 

echinoderm-foraminiferal.---.-.-._ .. 25 

nondolomitized____.___......_- 3

warreni, Lithostrotion......................... 13

(Siphonodendron)..................... 8,

10, 13, 15, 16, 18, 20, 28, 29, 31, 34; pis.

1,2

williamsi, Faberophyttum.................. 18,21,33

U. S. GOVERNMENT PRINTING OFFICE : 1970 O - 378-461
PLATES 1-14
PLATE 1

FIGURES 1-7. Lithostrotion (Siphonodendron) sinuosum (Kelly) (p. 9).

1, 2. Transverse and longitudinal thin sections. X 3. USNM 160989; 690 ft below the top of section 62C-15,

Kogruk Formation, DeLong Mountains. 

3-5. 3, Transverse thin section; 4, 5, longitudinal thin sections. X 3. USNM 160988; 620 ft below the top of

section 62C-15, Kogruk Formation, DeLong Mountains. 

6, 7. Longitudinal and transverse thin sections, respectively. X 3. USNM 160987; 870 ft below the top of section

62C-31; Kogruk Formation, DeLong Mountains. 

8. Lithostrotion (Siphonodendron) aflf. L. (S.) sinuosum (Kelly) (p. 12).

Transverse thin section. X 3. USNM 160997; Utukok Formation, DeLong Mountains. (See pi. 3, figs. 1, 2, for

X 25 views of corallites.) 

9, 10. Lithostrotion (Siphonodendron) warreni Nelson (p. 13).

Longitudinal and transverse thin sections, respectively illustrating microstructure and mode of preservat; on. X 30. 

USNM 160990; 1,310 ft below the top of section 62C-31, Kogruk Formation, DeLong Mountains.
GEOLOGICAL SURVEY 

I

PROFESSIONAL PAPER 664 PLATE 1

LITHOSTROTION (SIPHONODENDRON) SINUOSUM (Kelly) and 

LITHOSTROTION (SIPHONODENDRON) WARREN I Nelson
PLATE 2

FIGURES 1-4. Lithostrotion (Siphonodendrori) warreni Nelson (p. 13).

1, 2. Transverse and longitudinal thin sections, respectively. X 3. USNM 160990; 1,310 ft below the top of section

62C-31, Kogruk Formation, DeLong Mountains. 

3, 4. Longitudinal and transverse thin sections, respectively. X 3. USNM 160993; Cape Thompson Member of the

Nasorak Formation, Cape Thompson. 

5-9. Lithostrotion (Siphonodendrori) sp. A (p. 15).

USNM 160992; Cape Thompson Member of the Nasorak Formation, Cape Thompson.

5. Longitudinal thin section (X 30) illustration microstructure of the columella and the even slope of the tabulae

from the dissepiments to the columella. 

6-8. Longitudinal thin sections. X 3. 

9. Transverse thin section. X 3.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 664 PLATE 2

LITHOSTROTION (SIPHONODENDRON) WARRENI (Nelson) and LITHOSTROTION (SIPHONODENDRON) sp.A
PLATE 3

FIGURES 1, 2. Lithostrotion (Siphonodendron) aff. L. (S.) sinuosum (Kelly) (p. 12).

Longitudinal and transverse thin sections, respectively. X 25. USNM 160997; Utukok Formation, Belong Mountains. (See pi. 1, fig. 8 for X 3 transverse thin sections of corallites.) 

3, 4. Lithostrotion (Siphonodendron) sinuosum (Kelly) (p. 9).

Longitudinal and transverse thin sections, respectively. X 25. USNM 160989; 690 ft below the top of section 62C-15;

Kogruk Formation, DeLong Mountains. 

5-8. Lithostrotionella banffensis (Warren) (p. 16).

5. Transverse thin section. X 3.

6. Longitudinal thin section. X 3.

7. Longitudinal thin section of columella, tabulae, dissepiments, and microstructure. X 25.

8. Transverse thin section of wall, dissepiment, microstructure, and sparry calcite void filling. X 25. 

USNM 161011; upper member of the Nasorak Formation, Cape Thompson section.
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LITHOSTROTION (SIPHONODENDRON) aff. L. fSJ SINUOSUM (Kelly), LITHOSTROTION (SIPHONODENDRON) SINUOSUM (Kelly), and LITHOSTROTIONELLA BANFFENSIS (Warren)

PROFESSIONAL PAPER 664 PLATE 3

f^i^^«p^

v»-

T"^ * '
PLATE 4

FIGURES 1-4. Lithostrotionella banffensis (Warren) (p. 16).

1, 2. Transverse and longitudinal thin sections, respectively. X 3. USNM 161012; 570 ft below the top of section 

62C-15, Kogruk Formation, DeLong Mountains. (See pi. 10, fig. 1 for X 25 transverse view of microstructure 

and preservation.) 

3, 4. Transverse thin section and longitudinal view of an immature corallite, respectively. X 3. USNM 161013;

335 ft below the top of section 62C-31, Kogruk Formation, DeLong Mountains. 

5, 6. Lithostrotionella aff. L. banffensis (Warren) (p. 19).

Longitudinal and tranverse thin section, respectively. X 3. USNM 161010; 1,260 ft below the top of section 62C-31

Kogruk Formation, DeLong Mountains. 

7. Lithostrotionella birdi Armstrong (p. 20).

Transverse thin section. X 3. USNM 161024; 100 ft from the top of measured section 60A-400-403, Kogruk Formation, DeLong Mountains. (See pi. 5, figs. 3, 5, for longitudinal views.)
GEOLOGICAL SURVEY PROFESSIONAL PAPER 664 PLATE 4

&«^,,^^^ _

"i.? * y >*v i.'-v. *- s, ^ ^i^.-o-t^**^*- s^

LITHOSTROTIONELLA BANFFENSIS (Warren), LITHOSTROTIONELLA afF. L. BANFFENSIS (Warren), and

LITHOSTROTIONELLA BIRDI Armstrong
PLATE 5

FIGURES 1-3, 5, 6. Lithostrotionella birdi Armstrong (p. 20).

1, 2. Transverse and longitudinal thin sections, respectively. X 3. USNM 161023; 49 ft from the top of 

section 62C-15, Kogruk Formation, DeLong Mountains.

3. 5, 6. 3, 5, Longitudinal thin sections (X 3); 6, transverse thin section (X 20). USNM 161024; 100 ft 

from the top of section 60A-400 493, Kogruk Formation, DeLong Mountains. (See pi. 4, fig. 7 for X 3 

transverse view.) 

4, 7, 8-10. Lithostrotionella mclareni (Sutherland) (p. 21).

4. 9, 10. 4, Longitudinal thin section (X 25); 9, longitudinal thin section (X 3); 10, transverse thin 

section (X 3). USNM 160999; 1,065 ft below the top of section 62C-31, Kogruk Formation, DeLong 

Mountains.

7, 8. Transverse and longitudinal thin sections, respectively. X 3. USNM 161000; 49 ft from the top of section 

62C-15, Kogruk Formation, DeLong Mountains. (See pi. 6, fig. 7 for additional transverse section.)
GEOLOGICAL SURVEY PROFESSIONAL PAPER 664 PLATE 5

8 

LITHOSTROTIONELLA BIRDI Armstrong and LITHOSTROTIONELLA MCLARENI (Sutherland)
PLATE 6

FIGURES 1, 2, 7-9. Lithostrotinella mclareni (Sutherland) (p. 21).

1, 2. Longitudinal and transverse thin sections, respectively. X 3. USNM 161003; 510 ft from the top of 

section 62C-15, Kogruk Formation, DeLong Mountains.

7. Transverse thin section. X 3. USNM 161000; 49 ft from the top of section 62C-15, Kogruk Formation, 

DeLong Mountains. (See pi. 5, figs. 7 and 8 for additional views.)

8. 9. Transverse and longitudinal thin sections, respectively. X 3. USNM 161030; 1,100 ft below the top of

section 60A-400 403, Kogruk Formation, DeLong Mountains, Alaska. 

3-6. Sdophyllum lambarti Harker and McLaren (p. 31).

3, 4. Longitudinal and transverse thin sections, respectively. X 3. USNM 161017; upper member of the

Nasorak Formation, Cape Thompson. 

5, 6. Longitudinal and transverse thin sections, respectively. X 3. USNM 161015; 1,320 ft below the top of

section 62C-31, Kogruk Formation, DeLong Mountains.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 664 PLATE 6

LITHOSTROTIONELLA MCLARENI (Sutherland) and SCIOPHYLLUM LAMBARTI Harker and McLaren
PLATE 7

FIGURES 1-6. Lithostrotionella sp. A (p. 25).

1, 2. Transverse thin sections. X 3.

3. Longitudinal thin section. X 25.

4. Transverse thin section. X 25.

5. 6. Longitudinal thin sections. X 3.

USNM 161027; 395 ft below the top of section 62C-34, Kogruk Formation, Lisburne Hills. 

7-9. Lithostrotionella sp. B (p. 26).

7, 8. Longitudinal and transverse thin sections, respectively. X 3.

9. Transverse thin section. X 25.

USNM 161028; 365 ft below the top of section 62C-31, Kogruk Formation, DeLong Mountains.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 664 PLATE 7

8 9 ' 

LITHOSTROTIONELLA sp.A.and LITHOSTROTIONELLA sp.B
PLATE 8

FIGTJEES 1-5. Thysanophyllum orientals Thomson (p. 27).

1-3. 1, Photomicrograph of corallite wall in transverse thin section (X 25); 2, 3, transverse and longitudinal thin

sections respectively, (X 3). USNM 161018; 1,105 ft below the top of section 62C-31, Kogruk Formation, DeLong

Mountains. 

4, 5. Longitudinal and transverrse thin sections, respectively. (X 3). USNM 161019; 70 ft below the top of section

60A-400 403, Kogruk Formation, DeLong Mountains.
GEOLOGICAL SURVEY

F~-~* 

>'*£

PROFESSIONAL PAPER 664 PLATE 8

/. A;UVX/ .,

-f-'f^Qr v~ : ^~>*- .: vH1 

THYSANOPHYLLUM ORIENT ALE Thomson
PLATE 9

FIGURES 1-6. Thysanophyllum astraeiforme (Warren) (p. 28).

1-3. 1, Transverse thin section (X 3); 2, photomicrograph of a tranverse thin section illustrating tabularium

wall, major septa, columella, and epitheca (X 25); 3, longitudinal thin section (X 3). USN 161025; 1,200 ft

below the top of section 62C-31, Kogruk Formation, DeLong Mountains. 

4-6. 4, 5, Tran verse thin section; 6, longitudinal thin section. X 3. USNM 161026; Cape Thompson Member of

the Nasorak Formation, Cape Thompson.
GEOLOGICAL SURVEY

j

PROFESSIONAL PAPER 664 PLATE 9

^"^fe> ^^fefe^^vv 4r4^or ' -^' ^H ' ': e, jr~ '^- - "* -M^ -

,-ve - 6 5

THYSANOPHYLLUM ASTRAEIFORME (Warren)
PLATE 10

FIGURES 1. Lithostrotionella banffensis (Warren) (p. 16).

Longitudinal thin section of wall, dissepiments, and septa microstructure preservation. X 25. USNM 161012; 570 ft

below the top of section 62C-15, Kogruk Formation, DeLong Mountains. (See pi. 4, figs. 1, 2, for X 3 transverse

and longitudinal thin sections of this specimen). 

2-6. Sciophyllum alaskaensis Armstrong (p. 32).

2, 3. Transverse and longitudinal thin sections, respectively. X 3. USNM 161021; 1,075 ft below the top of section

62C-31, Kogruk Formation, DeLong Mountains. 

4, 5. 4, Transverse thin section (X 3); 5, transverse thin section (X 25) illustrating septal spines on corallite

walls, microstructure of walls, septa, dissepiments, and calcite pore filling. USNM 161020; 515 ft below the top of

section 62C-31, Kogruk Formation, DeLong Mountains. 

6. Transverse thin section. X 3, USNM 161022; 300 ft below the top of section 62C-15, Kogruk Formation, DeLong

Mountains.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 664 PLATE 10

LITHOSTROTIONELLA BANFFENSIS (Warren), and SCIOPHYLLUM ALASKAENSIS Armstrong
PLATE 11

FIGURES 1-3. Thysanophyllum sp. A (p. 30).

1. Photomicrograph of corallite wall in transverse section. X 25.

2. Transverse thin section. X 3.

3. Longitudinal thin section. X 3.

USNM 161006; 520 ft below the top of section 62C-15, Kogruk Formation, DeLong Mountains. 

4-7. Sciophyllum sp. A (p. 33).

4. 5. Longitudinal thin sections. X 3.

6. Transverse thin section. X 3.

7. Photomicrograph of transverse section of epitheca. X 25.

USNM 161029; upper 50 ft of the lower member of the Nasorak Formation, Cape Thompson.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 664 PLATE 11

THYSANOPHYLLUMsp.A and SCIOPHYLLUM sp.A
PLATE 12

FIGURES 1-6. Lithostrotionella macouni (Lambe) p. (23).

Syntype, Canadian Geologiacl Survey No. 4327, "Fossil Point," Peace River, British Columbia.

1, 2. Transverse thin section (X 25) illustrating microstructure, preservation, and discontinous major septa in 

dissepimentarium.

3. Longitudinal thin section. X 5.

4. Transverse thin section. X 5.

5. 6. Longitudinal thin section (X 25) illustrating microstructure and preservation.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 664 PLATE 12

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LITHOSTROTIONELLA MACOUNI (Lambe) syntype
PLATE 13

FIGURES 1-6. Section 62C-15, USGS loc. M1019, Kogruk Formation, Belong Mountains. (See text fig. 3.)

1. Bryozoan-brachiopod-echinoderm-foraminiferal packstone; most particles are abraded, rounded, and have fair 

sorting. This carbonate rock type is common in the Kogruk Formation. X 25. 280 ft from top of section.

2. Echinoderm-bryozoan-brachiopod packstone; poorly sorted fossil fragments. Many of the smaller particles are 

abraded and rounded. This carbonate rock type is very common in the Kogruk Formation. X 25. 520 ft from 

top of section.

3. Echinoderm-bryozoan-brachiopod packstone; broken and abraded fossil fragments. Some dolomitization of the 

lime mud; dolomite rhombs range in size from 40 to 80 microns. The dolomite rhombs have generally not affected 

the fossils but have begun to modify the exterior shape of the pellets. Carbonate rocks with this type of texture 

are the most abundant within the Kogruk Formation. X 25. 880 ft from the top of section.

4. Echinoderm-bryozoan-foraminiferal packstone; fossil fragments are broken, abraded, and well sorted and are 

200-300 microns long. X 25. 1,210 ft below top of section.

5. Algal-echinoderm-bryozoan grainstone; fragments are large, broken, and winnowed. Rock contains abundant 

fragments of algae of the Solenoporaceae and appears to represent sedimentation in shallow, shoaling water. 

This carbonate rock type is relatively scarce and is generally found only in the lower 200-300 ft of the Kogruk 

Formation. X 25. 1,490 ft from top of the section.

6. Bryozoan-foraminiferal-echinoderm ooid grainstone; rounded and sorted fossil fragments have one layer of 

oolitic coating. Ooid packstones and grainstone of this texture are commonly found in the basal beds of the 

Kogruk Formation above the Utukok Formation. Environment of deposition is thought to be moderate energy 

shoaling water. X 25. 1,760 ft from top of section. 

7-8. Section 62C-31, USGS loc. M1020, Kogruk Formation, DeLong Mountains. (See text fig. 5.)

7. Bryozoan-foraminiferal-echinoderm ooid packstories to grainstone; rounded and sorted fossil fragments have 

one layer of oolitic coating. Deposition is believed to be in a shoaling-water environment. X 25. 330 ft from 

top of section.

8. Bryozoan-echinoderm-foraminiferal packstone; fair to poor sorting, some hard pellets. A typical Kogruk 

carbonate rock type with initial phase of dolomitization characterized by scattered dolomite rhombs which range 

in size from 40 to 60 microns. X 25. 980 ft below top of section.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 664 PLATE 13

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Photomicrographs of carbonate rock types sections
PLATE 14

FIGURES 1-3. Section 62C-31, USGS loc. M1020, Kogruk Formation, DeLong Mountains. (See text fig. 5.)

1. Bryozoan-echinoderm-foraminiferal packstone with broken, abraded, poorly sorted fossil fragments. X 25. 

1,390 ft from top of section.

2. Lime mudstone to bryozoan-echinoderm wackestone. The lime mudstone is affected in part by calcite neomorphism which has formed crystals of microspar calcite that range in size from 50 to 100 microns. X 25. 1,680 ft 

from top of section.

3. Bryozoan-echinoderm-pelletoid packstone. Fair to poor sorting of broken and abraded fossil fragments. Much 

of the lime mud has undergone calcite neomorphism to form microspar calcite between the fossil fragments. 

X 25. 1,820 ft from top of section. 

4-6. Section 60A-400 403, USGS loc. M1021, Kogruk Formation, DeLong Mountains. (See text fig. 7.)

4. Bryozoan-echinoderm packstone; broken and abraded fossil fragments. X 25. 31 ft from top of section.

5. Foraminiferal-echinoderm wackestone. X 25. 330 ft from top of section.

6. Foraminifera-bryozoan-echinoderm wackestone to packstone. Rock has initial phase of dolomitization and is 

composed of less than 5 percent dolomite. The dolomite rhombs are 50 microns in size. 1,680 ft below top of 

section. 

7-8. Section 62C-34, USGS loc. M1022, Kogruk Formation, Lisburne Hills. (See text fig. 9.)

7. Coarse-grained bryozoan-echinoderm grainstone X 25. 50 ft from top of the section.

8. Oolite-echinoderm-formainiferal packstone to wackestone. X 25. 270 ft from top of section.
GEOLOGICAL SURVEY

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Photomicrographs of carbonate rock types, sections 62C-31, 60A-400- 403, 62C-34.