Shorter Contributions to 

Paleontology and Stratigraphy 

Shorter Contributions to 

Paleontology and Stratigraphy 

Edited by William j. Sando 

U.S. GEOLOGICAL SURVEY BULLETIN 1690 
DEPARTMENT OF THE INTERIOR 

DONALD PAUL HODEL, Secretary 

U.S. GEOLOGICAL SURVEY 

Dallas L. Peck, Director 

UNITED STATES GOVERNMENT PRINTING OFFICE: 1987 

For sale by the Books and Open-File Reports Section, U.S. Geological Survey, 

Federal Center, Box 25425, Denver, CO 80225 

Library of Congress Cataloging-in-Publication Data 

Shorter contributions to paleontology and stratigraphy. 

(U.S. Geological Survey bulletin ; 1690A-F) 

Supt. of Docs. No.: I 19.3:1690A-F 

1. Paleontology-United States. 2. PaleontologyChina-Tibet. I. Sando, William Jasper. II. Series: 

Geological Survey bulletin ; 1690A-F. 

QE75.B9 no. 1690A-F [QE746] 557.3 s 86--600262 

[560] 
CONTENTS 

CHAPTER A 

The Upper Cretaceous Ammonite Eubostrychoceras Matsumoto in the Western 

Interior of the United States 

William A. Cobban 

CHAPTER B 

A New Ammonite from the Upper Cretaceous of Kansas 

William A. Cobban 

CHAPTER C 

The Upper Cretaceous (Cenomanian) Ammonites Metengonoceras dumbli 

(Cragin) and M. acutum Hyatt 

William A. Cobban 

CHAPTER D 

Middle Devonian Coral Faunules from Illinois and Their Bearing on Biogeography 

William A. Oliver, Jr. 

CHAPTER E 

Paleobathymetric Significance of Ostracodes from the Paine Member of the 

Lodgepole Limestone (Early Mississippian), Northeast Utah 

I.G. Sohn and William J. Sando 

CHAPTER F 

Some Ordovician and Permian-Triassic Conodonts from Xizang (Tibet) 

Anita G. Harris, john E. Repetski, and Erie G. Kauffman 

CHAPTER A 

The Upper Cretaceous Ammonite 

Eubostrychoceras Matsumoto in 

the Western Interior of the United 

States 

By William A. Cobban 

Description and illustrations of an unusual ammonite 

from Wyoming, South Dakota, and New Mexico 

U.S. GEOLOGICAL SURVEY BULLETIN 1690 

Shorter Contributions to Paleontology and Stratigraphy 

CONTENTS 

Abstract Al 

Introduction Al 

Localities of collections Al 

Systematic paleontology A2 

Family Nostoceratidae Hyatt A2 

Genus Eubostrychoceras Matsumoto A2 

Eubostrychoceras matsumotoi Cobban, n. sp. A3 

Associated fossils and age A4 

References cited A4 

PLATE 

[Plate follows References Cited] 

1. Eubostrychoceras 

FIGURES 

1. Map showing localities of Eubostrychoceras matsumotoi Cobban, n. sp. A2 

2. Suture of Eubostrychoceras matsumotoi Cobban, n. sp. A4 

Contents iii 

The Upper Cretaceous Ammonite 

Eubostrychoceras Matsumoto in the Western 

Interior of the United States 

By William A. Cobban 

Abstract 

The ammonite genus Eubostrychoceras is recorded for the 

first time in the western interior region, and the new species f. 

matsumotoi is described and illustrated. The new species has 

been found in the Wall Creek Member of the Frontier Formation in central Wyoming, in the Turner and Sage Breaks Members of the Carlile Shale in northeastern Wyoming and southwestern South Dakota, and in the D-Cross Tongue of the 

Mancos Shale in southern New Mexico. Outside the western 

interior region, the species occurs in the basal part of the Austin 

Chalk in southwestern Texas. The age is latest Turonian. 

INTRODUCTION 

The heteromorph ammonite Eubostrychoceras was 

named by Matsumoto (1967, p. 332) for helically coiled 

forms that usually have the whorls in contact. Ribs are 

conspicuous and generally simple. Constrictions are usually 

present, but tubercles are absent. Matsumoto ( 1967, p. 333) 

noted that the genus occurs in rocks of Albian to Santonian 

Age in Japan, India, Madagascar, North Africa, Western 

Europe, and the Pacific coast of North America. 

Eubostrychoceras has not been reported previously from 

the western interior of the United States. Specimens referable to the genus, however, are present in some of the 

collections of fossils of the U.S. Geological Survey. A 

specimen was collected by V. H. Barnett as far back as 1913 

in the course of mapping the Moorcroft oil field on the west 

flank of the Black Hills uplift in northeastern Wyoming. 

However, the fossil was not mentioned in his report on the 

area (Barnett, 1914). At a later date, a specimen collected 

farther southeastward near Newcastle, Wyo., was identified 

by J. B. Reeside, Jr., as Helicoceras? n. sp. (Mapel and 

Pillmore, 1963, p. N48; Robinson and others, 1964, p. 68). 

Eubostrychoceras was also found far to the south in southem New Mexico. Specimens were identified first as Turrilitoides by Alexander Stoyanow (Kottlowski and others, 

1956, p. 68) and later by me as Bostrychoceras cf. B. 

elongatum (Whiteaves) (Bachman and Myers, 1969, p. 

C39). In recent years, excellent examples of Eubostrychoceras have been collected from the Frontier Formation near Casper, Wyo., and from the D-Cross Tongue of 

the Mancos Shale in southern New Mexico. All specimens 

seem referable to a single new species described herein as E. 

matsumotoi. Outside the western interior region, fragments 

of E. matsumotoi have been found in the basal part of the 

Austin Chalk in the Rio Grande area in Terrell and Val 

Verde Counties, Tex. 

The fossils described in this report are kept in the National 

Museum of Natural History in Washington, D.C. All specimens have USNM catalog numbers. Plaster casts of a few 

of the specimens are in the reference collection of the U.S. 

Geological Survey at the Federal Center, Denver, Colo. 

R.E. Burkholder, of the U.S. Geological Survey, made the 

photographs. 

LOCALITIES OF COLLECTIONS 

Localities at which the new species Eubostrychoceras 

matsumotoi were collected in the western interior region are 

shown on figure 1. The U.S. Geological Survey Mesozoic 

locality number, names of collectors, year of collection, 

locality, and stratigraphic assignment are as follows (prefix 

D indicates Denver Mesozoic locality numbers; the others 

are Washington, D.C., Mesozoic locality numbers): 

8864. V.H. Barnett, 1913. About 24 km (15 mi) north of 

Moorcroft in the SE 1/4 sec. 33, T. 52 N., R. 67 

W., Crook County, Wyo. Carlile Shale [Turner 

Sandy Member]. 

11184. W.W. Rubey and C.R. Longwell, 1922. Beside 

highway about 3.2 km (2 mi) west of Newcastle, 

Weston County, Wyo. Carlile Shale [Turner Sandy 

Member]. 

21765. W.A. Cobban, 1948. North of Spring Creek in the 

NE 114 sec. 22, T. 1 S., R. 8 E., Pennington 

County, S. Oak. Carlile Shale, 13m (42.6 ft) above 

base of Sage Breaks Member. 

Eubostrychoceras Matsumoto A 1 
110° 108° 106° 104° 

I I I II 

------ MOJ"'T~~-------1 SOUTH 

I 

I DAKOTA 

0 Buffalo t8864 I Rapid City x 22817 Moorcroft 1 44° - 0 -

X 21765 

W y 0 ~,:,~ G 1118~~ 09118 t-------- 0935mJ 

09359 Casper I 

09362 I 42° - Rawlins I NEBRASKA _ 

Ox 22952 I 

Cheyenne I 

-----,-------------0--""-----, 

I I 

40° 1-- i l 

1 o I 

1 Denver 1 

UTAH I c 0 L 0 R A D 0 I 

I I 

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I I 

I I 

---+---------------r-J 

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Santa Fe 

0 

Albuquerque 

NEW MEXICO 

X 02493-95 

I 0 Las Cruces 

I J----~EIPaso ______ ____. 

I \ 

---'- - - '\ TEXAS 

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0 100 200 KILOMETERS 

-

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I 

Figure 1. Map of part of the western interior ot the United 

States showing localities where Eubostrychoceras matsumotoi 

Cobban, n. sp., has been collected. Numbers are U.S. Geological Survey Mesozoic localities. 

A2 Shorter Contributions to Paleontology and Stratigraphy 

22817. R.K. Hose, J.B. Reeside, Jr., and W.A. Cobban, 

1950. Dry Muddy Creek in the NE 114 sec. 1, T. 48 

N., R. 83 W., Johnson County, Wyo. Cody Shale, 

from septarian limestone concretions in lower part. 

22952. J.B. Reeside, Jr., 1950. North flank of Grenville 

dome 1.6 km (1 mi) southeast of Sinclair in the SE 

114 sec. 22, T. 21 N., R. 86 W., Carbon County, 

Wyo. Frontier Formation, from a sandstone concretion 16m (52ft) above base of Wall Creek Member. 

D2493. G.O. Bachman and D.A. Myers, 1960; S.C. Hook 

and W.A. Cobban, 1980. West side of San Andres 

Mountains in the SW 114 sec. 19, T. 20 S., R. 4 E., 

Dona Ana County, N. Mex. Mancos Shale, from 

lower part of D-Cross Tongue. 

D2494. G.O. Bachman and D.A. Myers, 1960; S.C. Hook 

and W.A. Cobban, 1980. Same locality as D2493. 

From concretion in D-Cross Tongue 2-3 m 

(6-10ft) above D2493. 

D2495. G.O. Bachman and D.A. Myers, 1960; S.C. Hook 

and W.A. Cobban, 1980. Same locality as D2493. 

From concretions in D-Cross Tongue 8 m (26 ft) 

above D2494. 

D9116. E.A. Merewether and W.A. Cobban, 1974. Emigrant Gap Ridge 16 km (10 mi) west of Casper in 

theSE 114 sec. 3, T. 33 N., R. 81 W., Natrona 

County, Wyo. Frontier Formation, from sandstone 

concretions in upper part of Wall Creek Member. 

D9118. E.A. Merewether and W.A. Cobban, 1974. Emigrant Gap Ridge in the NE 114 sec. 4, T. 33 N., R. 

81 W., Natrona County, Wyo. Frontier Formation, 

from same stratigraphic level as D9116. 

D9357. E.T. Cavanaugh, 1975. Emigrant Gap Ridge in the 

NW 114 sec. 11., T. 33 N., R. 81 W., Natrona 

County, Wyo. Frontier Formation, from same 

stratigraphic level as D9116. 

D9359. E.T. Cavanaugh, 1975. Emigrant Gap Ridge in the 

NE 114 sec. 32, T. 34 N., R. 81 W., Natrona 

County, Wyo. Frontier Formation, from top of 

Wall Creek Member. 

D9362. E.T. Cavanaugh and E.A. Merewether, 1975. 

Casper Canal in theSE 114 sec. 5, T. 33 N., R. 81 

W., Natrona County, Wyo. Frontier Formation, 

from upper part of Wall Creek Member. 

SYSTEMATIC PALEONTOLOGY 

Family NOSTOCERATIDAE Hyatt, 1894 

Genus EUBOSTRYCHOCERAS Matsumoto, 1967 

Type species-Eubostrychoceras indopacificum Matsumoto, 1967, by original designation. 

Matsumoto (1977, p. 324) gave the following amended 

definition of Eubostrychoceras: 

Main part of the septate whorls are helically coiled and the adult bodychamber deviates slightly or remarkably from this helix, with its apertural 

end facing obliquely or nearly straight upward or "backward", i.e., in more 
or less reversed orientation against the orientation of the axis of helical 

coiling. The whorls may be tightly contiguous or slightly or considerably 

separated, depending on species or in some cases even on individuals. 

Periodic constrictions, with accompanied flared ribs, may be present or 

absent, again depending on species and also on growth-stages. Even in the 

species without periodic constrictions the adult body-chamber is generally 

provided with one or more constrictions at or near its peristome. The length 

of the body-chamber is apparently variable. 

The whorl is ornamented with numerous ribs which are mostly simple, 

occasionally branched or inserted, more or less oblique and gently sinuous 

on the external part (i.e., the convex side), with bending at the shoulders. 

No tubercles are developed at any stage. 

The siphuncle runs approximately at the middle of the external side of 

the helical whorl but may somewhat deviate from that position. The suture 

is of modified lytoceratid type, deeply and finely incised, with much 

narrowed stems and expanded branches of bifid L, U, and lateral saddles. 

Wright (1979, p. 296) believed Eubostrychoceras was an 

unnecessary name or at best a subgenus of Didymoceras 

Hyatt (1894, p. 573). In a more recent work, Kennedy and 

Summesberger (1984, p. 165) regarded Didymoceras as a 

subgenus of Nostoceras (Hyatt, 1894, p. 569). Didymoceras and Nostoceras have tubercles at some growth stage. 

Eubostrychoceras seems distinct though in lacking tubercles 

at any growth stage, and in having a peculiar arrangement 

in the juvenile coiling. This odd juvenile coiling was noted 

by Matsumoto (1967, p. 335) in the description of his new 

species E. muramotoi from Coniacian strata of Japan. Matsumoto observed that: 

***the earliest shell is nearly straight, ascending and then followed by a 

subcircularly curved, half whorl, which, in turn, is twisted obliquely down, 

passing to the main helical whorls, whose axis of coiling is along the 

earliest straight shaft. Thus the youngest whorl is apparently incurved into 

the axial part of the helix. The same mode of coiling does not seem to be 

constantly held in the present species, since in some other specimens the 

apical end of the earliest whorl shows an oblique orientation. Anyhow, the 

young whorl is more or less deviated from the main helical ones, showing 

some irregularity. 

Eubostrychoceras matsumotoi Cobban, n. sp. 

Plate 1, figures 1-26; text-figure 2 

This species is characterized by its large apical angle and 

sparse ribbing. The earliest whorls are hamitid and enclosed 

by the earliest whorl of the spire. 

The holotype (pl. 1, figs. 24-26), from the Frontier 

Formation of Wyoming, is an adult sinistral spire of four 

whorls in contact that have an apical angle of 65° and a 

height of 69 mm. A little more than one half of the last whorl 

is body chamber. An impressed area around the umbilicus 

(pl. 1, fig. 26) suggests that the complete body chamber 

may have included a whorl and a half. Whorl sections are 

higher than they are wide with very broadly rounded outer 

flanks. Ribs are single and narrow and number 29 on the 

smallest whorl, 25 on the next one, 20 on the next, and 30 

on the largest. Each rib slants straight across the side and 

than bends forward a little on the opposite shoulder. 

The earliest whorls are best seen on a specimen from the 

D-Cross Tongue of the Mancos Shale of southern New 

Mexico. This specimen consists of two parallel limbs incurved into a spire of one complete whorl (p 1. 1, figs. 1-4). 

The smaller straight limb, 14 mm long, has a diameter of 

0. 5 mm at one end and 1 mm at the other. Its angle of 

growth is very low, and its whorl section is circular. Ornament is lacking. The second straight limb, which is connected to the first by a U-shaped elbow, is about 12 mm 

long. This limb has a section a little broader than it is high 

with very broadly rounded venter and narrowly rounded 

flanks. Closely spaced, transverse, rounded ribs are present 

on the younger (larger) half. Upon forming the second 

U-shaped elbow, the limb then curves obliquely downward 

and passes into a helical spire. 

Constrictions are inconspicuous and parallel to the ribs. 

Most specimens, including the holotype, have one or two 

constrictions per whorl. A deeper constriction, bounded by 

high ribs, is present just before the aperture (p 1. 1, fig. 16). 

The apical angle ranges from 65°, for the holotype, to as 

much as 90° for specimens that have lower spires and wider 

umbilici (pl. 1, figs. 17-23). Specimens are about equally 

divided between dextral and sinistral coiling. 

A complete individual is not present in the collections. 

Most specimens are fragments of whorls or no more than 

two or three whorls in the spire in addition to the hamitid 

early whorls. The last part of the adult body chamber may 

have pulled away slightly from the spire and then curved 

back to it in the manner described by Matsumoto ( 1967, 

p. 333, pl. 18, fig. 1a) for the type species of the genus, 

Eubostrychoceras indopacificum. 

The suture, which is centered at midflank, is characterized by an extremely wide, deeply bifid lateral lobe (fig. 2). 

The rest of the lobes and saddles are deeply bifid except the 

small, narrow internal lobe, which is trifid. 

The sparse ribbing of Eubostrychoceras matsumotoi 

easily distinguishes this form from the other species assigned to the genus by Matsumoto (1967, p. 332). However, 

E. elongatum (Whiteaves, 1903, p. 331, pl. 44, fig. 3), 

from Campanian rocks of British Columbia, is as coarsely 

ribbed, but it has a much more acute apical angle and, 

according to Usher (1952, p. 105, pl. 28, fig. 4), the body 

chamber becomes loosely coiled and freed from the septate 

spire. 

The holotype is from a sandy concretion at the top of the 

Wall Creek Member of the Frontier Formation at USGS 

Mesozoic locality D9359 at Emigrant Gap Ridge west of 

Casper in the NE 114 sec. 32, T. 34 N., R. 81 W., Natrona 

County, Wyo. (fig. 1). The figured paratypes are from the 

Wall Creek Member west of Casper and from sandy concretions in the D-Cross Tongue of the Mancos Shale at a small 

outcrop on the west flank of the San Andres Mountains 

northeast of Las Cruces, Dona Ana County, N. Mex. 

The species is named in honor of Prof. Tatsuro Matsumoto, Professor Emeritus, Kyushu University, Fukuoka, 

Japan, for his important contributions on Cretaceous ammonites and biostratigraphy. 

Types. -Holotype USNM 395808, paratypes USNM 

395809-395818. 

Eubostrychoceras Matsumoto A3 
E 

5 mm 

Figure 2. Suture of Eubostrychoceras matsumotoi Cobban, n. sp., at a whorl height of 13.3 mm. Paratype USNM 395818, from 

the Frontier Formation at USGS Mesozoic locality 09362 (fig. 1 ). E is the external lobe, L is the lateral lobe, U is the umbilical 

lobe, and I is the internal lobe. 

ASSOCIATED FOSSILS AND AGE 

Important molluscan fossils found with the holotype and 

paratypes of E. matsumotoi in the Wall Creek Member of 

the Frontier Formation include Inoceramus incertus Jimbo, 

Baculites yokoyamai Tokunaga and Shimizu, and Prionocyclus reesidei Sidwell. Inoceramus incertus was described by 

Jimbo (1894, p. 43, pl. 8, fig. 7) from strata in Japan later 

assigned to the Turonian (Nagao and Matsumoto, 1939, 

p. 260). The species has been treated again recently by 

Matsumoto and Noda (1983), who regard it as late Turonian. These authors pointed out that Inoceramus fiegei 

Troger (1967, p. 105, pl. 11, fig. 3; pl. 13, figs. 14, 15, 17, 

20) from the very late Turonian of Europe is probably a 

synonym. Baculites yokoyamai was described from Coniacian rocks of Japan (Tokunaga and Shimizu,1926, p. 195, 

pl. 22, fig. 5a, b; pl. 26, fig. 11). This rather small species 

is a generalized form that has a stout elliptical to subelliptical section, very low degree of taper, finely ribbed venter, 

smooth to weakly ribbed flanks, and a fairly simple suture. 

Baculitids that are indistinguishable from the Japanese B. 

yokoyamai occur abundantly in rocks of early Turonian to 

early Coniacian age in the western interior of the United 

States. Prionocyclus reesidei was described by Sidwell 

(193 2, p. 318, pl. 49, figs. 10-12) from the Frontier Formation near Rawlins, Wyo. Collections made later from this 

area reveal that P. reesidei occurs in the lower part of the 

Wall Creek Member (Cobban and Reeside, 1951, p. 60, 61; 

Merewether and Cobban, 1972, fig. 2). Associated fossils 

include Inoceramus incertus and Baculities yokoyamai. Prionocylus quadratus Cobban (1953), which also occurs at the 

stratigraphic level of P. reesidei, has been used as a guide 

fossil to rocks of latest Turonian age in the western interior 

A4 Shorter Contributions to Paleontology and Stratigraphy 

region (Cobban, 1984, p. 76, 87). The known range of 

Eubostrychoceras matsumotoi is at the very top of the upper 

Turonian. 

In the Rio Grande area of ~outhwestern Texas, Freeman 

(1961, p. 105, 106) recorded Inoceramus cf. I. incertus and 

Prionocyclus reesidei from the basal part of the Austin 

Chalk. The inoceramid can be more definitely assigned to I. 

incertus. Associated with these fossils are fragments of E. 

matsumotoi. 

REFERENCES CITED 

Bachman, G.O., and Myers, D.A., 1969, Geology of the Bear 

Peak area, Dona Ana County, New Mexico: U.S. Geological 

Survey Bulletin 1271-C, 46 p., geol. map. 

Barnett, V.H., 1914, The Moorcroft oil field, Crook County, 

Wyoming: U.S. Geological Survey Bulletin 581, p. 83-104. 

Cobban, W.A., 1953, A new species of Prionocyclus from Upper 

Cretaceous Carlile shale: Journal of Paleontology, v. 27, 

no. 3, p. 353-355, pl. 48. 

---1984, Mid-Cretaceous ammonite zones, Western Interior, 

United States: Bulletin of the Geological Society of Denmark, 

V. 33, pt. 1-2, p. 71-89. 

Cobban, W.A., and Reeside, J.B., Jr., 1951, Frontier Formation 

near Sinclair, Carbon County, Wyoming: Wyoming Geological Association Guidebook Sixth Annual Field Conference, 

South Central Wyoming; p. 60-65. 

Freeman, V .L., 1961 , Contact of Boquillas Flags and Austin 

Chalk in Val Verde and Terrell Counties, Texas: American 

Association of Petroleum Geologists Bulletin, v. 45, no. 1, 

p. 105-107. 

Hyatt, Alpheus, 1894, Phylogeny of an acquired characteristic: 

American Philosophical Society Proceedings, v. 32, no. 143, 

p. 349-647, pis. 1-14. 
limbo, Kotara, 1894, Beitrage zur Kenntniss der Fauna der 

Kreideformation von Hokkaido: Palaeontologische Abhandlungen, n. ser., v. 2, no. 3, 48 p., 9 pls. 

Kennedy, W.J., and Summesberger, Herbert, 1984, Upper Campanian ammonities from the Gschliefgraben (Ultrahelvetic, 

Upper Austria): Beitrage zur Palaontologie von Osterreich, 

no. 11, p. 149-206, 14 pls. 

Kottlowski, F.E., Flower, R.H., Thompson, M.L., and Foster, 

R.W., 1956, Stratigraphic studies of the San Andres Mountains, New Mexico: New Mexico Bureau of Mines and Mineral Resources Memoir 1, 132 p. 

Mapel, W.J., and Pillmore, C.L., 1963, Geology of the Newcastle 

area, Weston County, Wyoming: U.S. Geological Survey 

Bulletin 11~H-N, 85 p. 

Matsumoto, Tatsuro, 1967, Evolution of the Nostoceratidae (Cretaceous heteromorph ammonoids): Kyushu University Faculty of Science Memoirs, Series D, Geology, v. 18, no. 2, 

p. 331-347, pls. 18, 19. 

---1977, Some heteromorph ammonites from the Cretaceous 

of Hokkaido: Kyushu University Faculty of Science Memoirs, Series D, Geology, v. 23, no. 3, p. 303-366, pls. 43-

61. 

Matsumoto, Tatsuro, and Noda, Masayuki, 1983, Restudy of Inoceramus incertus 1 imbo with special reference to its biostratigraphic implications: Proceedings of the Japanese 

Academy, v. 59, Series B, no. 5, p. 109-112. 

Merewether, E.A., and Cobban, W.A., 1972, Unconformities 

within the Frontier Formation, northwestern Carbon County, 

Wyoming, in Geological Survey Research 1972: U.S. Geological Survey Professional Paper 800-D, p. D57-D66. 

Nagao, Takumi, and Matsumoto, Taturo, 1939, A monograph of 

the Cretaceous Inoceramus of Japan, Part 1: Hokkaido Imperial University Journal of the Faculty of Science, Series 4, 

v. 4, nos. 3-4, p. 241-299, pls. 23-34. 

Robinson, C.S., Mapel, W.J., and Bergendahl, M.H., 1964, 

Stratigraphy and structure of the northern and western flanks 

of the Black Hills uplift, Wyoming, Montana, and South 

Dakota: U.S. Geological Survey Professional Paper 404, 

134p. 

Sidwell, Raymond, 1932, New species from the Colorado group, 

Cretaceous, in south-central Wyoming: Journal of Paleontology, v. 6, no. 4, p. 312-318, pls. 48, 49. 

Tokunaga, Shigeyasu, and Shimizu, Saburo, 1926, The Cretaceous formation of Futaba in Iwaki and its fossils: Tokyo 

Imperial University Faculty of Science Journal, sec. 2, v. 1, 

pt. 6, p. 181-212, pls. 21-27. 

Troger, Karl-Armin, 1967, Zur Palaontologie, Biostratigraphie 

und fraziellen Ausbuildung der unteren Oberkreide (Cenoman 

bus Turon); Teil 1, Palaontologie und Biostratigraphie der 

Inoceramen des Cenomans bis Turons Mitteleuropas: Dresden 

Staatlichen Museums fiir Mineralogie und Geologie Abhandlungen, v. 12, p. 13-207. 

Usher, J.L., 1952, Ammonite faunas of the Upper Cretaceous 

rocks of Vancouver Island, British Columbia: Canada Geological Survey Bulletin 21, 182 p., 31 pls. 

Whiteaves, J.F., 1903, On some additional fossils from the Vancouver Cretaceous, with a revised list of the species therefrom: Canada Geological Survey, Mesozoic fossils, v. 1, 

pt. 5, p. 309-415, pls. 40-51. 

Wright, C.W., 1979, The ammonites of the English Chalk Rock 

(Upper Turonian): British Museum (Natural History) Bulletin, Geology Series, v. 31, no. 4, p. 281-332, 7 pls. 

Eubostrychoceras Matsumoto A5 

PLATE 1 

Contact photographs of the plates in this report are available at cost from U.S. Geological 

Survey Library, Federal Center, Denver, CO 80225 
PLATE 1 

[All figures natural size. Localities shown on figure I in text] 

Figures 1-26. Eubostrychoceras matsumotoi Cobban, n. sp. (p. A3) 

1-4. Paratype USNM 395809, from the 0-Cross Tongue of the Mancos Shale at USGS Mesozoic locality 02493. 

5- 8. Paratype USNM 395810, from the Frontier Formation at USGS Mesozoic locality 09118. 

9. Paratype USNM 395811, from the Frontier Formation at USGS Mesozoic locality 09116. 

10. Paratype USNM 395812, from the same locality as figures 1-4. 

11. Paratype USNM 395813, from the Frontier Formation at USGS Mesozoic locality 09357. 

12-15. Paratype USNM 395814, from the same locality as figures 1- 4. 

16. Paratype USNM 395815, from the same locality as figure 9. 

17- 19. Paratype USNM 395816, from the same locality as 09118. 

20- 23. Paratype USNM 395817, from the Frontier Formation at USGS Mesozoic locality 09362. 

24- 26. Holotype USNM 395808, from the same locality as figures 20-23. 
BULLETIN 1690-A PLATE 1 

2 3 

4 5 6 7 8 

10 11 

12 13 14 15 

16 

19 

18 

22 

20 23 

I 

24 26 

EUBOSTRYCHOCERAS 

CHAPTER B 

A New Ammonite from the Upper Cretaceous 

of Kansas 

By William A. Cobban 

Description and illustrations of a new genus 

and species from the Greenhorn Limestone 

U.S. GEOLOGICAL SURVEY BULLETIN 1690 

Shorter Contributions to Paleontology and Stratigraphy 

CONTENTS 

Abstract Bl 

Introduction B 1 

Systematic paleontology Bl 

Family Desmoceratidae Zittel Bl 

Genus Bassites Cobban, n. gen. Bl 

Bassites reesidei Cobban, n. sp. Bl 

References cited B3 

PLATE 

[Plate follows References Cited] 

1. Bassites 

FIGURE 

1. Suture of Bassites reesidei Cobban, n. sp. B2 

Contents iii 

A New Ammonite from the Upper Cretaceous of 

Kansas 

By William A. Cobban 

Abstract 

The new ammonite genus Bassites is defined, and the new 

species B. reesidei is described and illustrated. Bassites, of early 

Turonian age, seems to have been derived from Moremanoceras of late Cenomanian age. The new genus is known 

only from a bed of limestone in the Bridge Creek Member of the 

Greenhorn Limestone of Kansas. 

INTRODUCTION 

Among the rarer forms of ammonites in the collections of 

molluscan fossils of the U.S. Geological Survey are two 

fairly large, robust specimens that cannot be assigned to any 

named genus. Both specimens represent the same genus and 

species, which is herein named Bassites reesidei. One specimen (the holotype) was collected in 1926, and the other was 

found in 1981 . 

The specimens are kept in the National Museum of Natural History, Washington, D.C., and have USNM catalog 

numbers. Plaster casts of the specimens are in the reference 

collections of the U.S. Geological Survey at the Federal 

Center, Denver, Colo. R.E. Burkholder, of the U.S. Geological Survey, made the photographs. 

SYSTEMATIC PALEONTOLOGY 

Family DESMOCERA Tl DAE Zittel, 1895 

Genus BASSITES Cobban, n. gen. 

Type species.-Bassites reesidei Cobban, n. sp. 

Bassites is characterized by its moderately large size; by 

its stout involute shell; by its ornament of weak closely 

spaced, flat, ribs; and by its simplified suture. The genus 

appears to have developed directly out of Moremanoceras 

(Cobban, 1971, p. 5) through an increase in size, loss of 

constrictions and raised ribs, and further simplification of 

the suture. Bassites is known only from lower Turonian 

rocks of Kansas. 

The genus is named for the late Nathan W. Bass, of the 

U.S. Geological Survey, who collected the type specimen 1 

during the course of his investigations of the Cretaceous 

stratigraphy of southwestern Kansas (Bass, 1926). Bass 

made many important collections of invertebrate fossils and 

contributed much to our knowledge of the mid-Cretaceous 

rocks of Kansas and southeastern Colorado (Lohman, 

1984). The late John B. Reeside, Jr., of the U.S. Geological 

Survey, had set the type specimen aside with plans to eventually describe it and name it for Bass under the name of 

Thomasites bassi. The specimen has been listed as Thomasites n. sp. (Bass, 1926, p. 71). This is not a Thomasites, but 

rather a new genus. Inasmuch as there is already a Reesidites 

(Wright and Matsumoto, 1954, p. 130) and aReesideoceras 

(Basse, 1947, p. 132), the taxon proposed in the present 

report seems the best way to honor both men. 

Bassites reesidei Cobban, n. sp. 

Plate 1 

1926. Thomasites n. sp. Bass, Kansas Geological Survey Bulletin 11, p. 71. 

This moderately large, robust, involute species has a 

rounded whorl section higher than wide. The species is 

known from only two incomplete adults. 

The holotype (pl. 1) is a slightly crushed internal mold 

147 mm in diameter with an umbilical width of23 mm (ratio 

of 0 .16). The specimen consists of a septate coil attached to 

a little less than a quarter of a whorl of the body chamber. 

Diameter at the base of the body chamber is 127.5 mm. 

Inner whorls are not preserved. The umbilicus has steep 

walls that merge evenly into a well-rounded umbilical 

shoulder. The last septate whorl has a well-rounded venter 

that grades evenly into broadly rounded flanks. Flanks on 

the preserved part of the body chamber are more rounded 

like the venter. Ornament consists of numerous weak rectiradiate ribs that begin at the umbilicus or on the lower part 

of the flank. All bend slightly forward at the ventrolateral 

shoulder and cross the venter with a little forward arching. 

There are about 56 ribs on the last half whorl of the phragmocone. The external suture (fig. 1) is rather simple with 

similar sized external (E) and lateral lobes (L) and first and 

second lateral saddles. The lateral lobe is deeply bifid. The 

next lobe is trifid and about half as large. 

New Ammonite, Upper Cretaceous of Kansas 81 
E E/L L 

( 

10 rom 

Figure 1. External suture of Bassites reesidei Cobban, n. sp., at a diameter of 106 mm. Holotype USNM 395819, from the 

Greenhorn Limestone at USGS Mesozoic locality 12773 in the SW 114 sec. 14, T. 23 5., R. 42 W., Hamilton County, Kans. 

The paratype (USNM 395820) closely resembles the 

holotype in size and appearance. Diameter is 150 mm, and 

the umbilical width is 25.3 mm (0.17). The paratype, a 

slightly crushed internal mold, is nearly complete and includes more than half a whorl of body chamber, which has 

a diameter of 114 mm at its base. 

Bassites reesidei does not closely resemble any known 

Cretaceous ammonite from North America. Occasional 

specimens of Moremanoceras scotti (Moreman), of late 

Cenomanian age, resemble B. reesidei in having stout, involute shells ornamented by numerous weak ribs (Cobban, 

1971, pl. 2, figs. 12-14). The Cenomanian species, however, has periodic constrictions and raised ribs as well as a 

more complex suture with a large trifid lateral lobe. 

Outside North America, the only species that shows some 

resemblance to B. reesidei is the ammonite from Portugal 

described originally as Ammonites (Vascoceras?) barcoicensis Choffat (1898, p. 67, pl. 16, fig. 11; pl. 17, fig. 

la-c; pl. 22, figs. 35, 36). This is a stout form with nearly 

smooth flanks except for weak closely spaced ribs much like 

those of B. reesidei. The Portuguese species, which may be 

about the same age, has been consistently considered a 

Vascoceras by many authors (for example, Wiedmann, 

1959, p. 723; Lauverjat and Berthou, 1974, p. 269 and 

unnumbered table; Berthou and Lauverjat, 1975, p. 98, 

103, 112; Berthou and others, 1975, p. 75, 81, 82). The 

Portuguese species is more evolute than the American form 

and has a suture more like Vascoceras. 

The holotype came from a bed of limestone at about the 

base of the middle third of the Bridge Creek Member of the 

Greenhorn Limestone at USGS Mesozoic locality 12773 in 

the SW 114 sec. 14, T. 23 S., R. 42 W., Hamilton County, 

Kans. Additional fossils collected by G.R. Scott and the 

author (Cobban and Scott, 1972, p. 21, bed 40) from this 

bed at or about the same locality include Mytiloides colum82 Shorter Contributions to Paleontology and Stratigraphy 

bianus (Heinz), Watinoceras coloradoense (Henderson), 

Vascoceras (Greenhornoceras) birchbyi Cobban and Scott, 

and Neoptychites cf. N. cephalotus (Courtiller). 

The paratype, collected by E.A. Merewether of the U.S. 

Geological Survey, came from the same bed of limestone as 

that of the holotype, but at a locality 178 km (111 mi) farther 

east (USGS Mesozoic loc. D11631 in the NW 1/4 sec. 7, T. 

23 S., R. 23 W., Hodgeman County, Kans.). Mytiloides 

columbianus (Heinz) was associated with it. At this locality, 

the bed of limestone forms the base of the Jetmore Chalk 

Member of the Greenhorn Limestone. 

The bed of limestone that produced the holotype and 

paratype persists westward into Colorado at least as far as 

the Front Range. Near Pueblo, the bed (Cobban and Scott, 

1972, p. 23, bed 97) contains many fossils including 

Mytiloides columbianus (Heinz), M. aff. M. opalensis 

(Bose), Watinoceras coloradoense (Henderson), W. aff. W. 

devonense Wright and Kennedy, Ampakabites collignoni 

Cobban and Scott, Vascoceras (Greenhornoceras) birchbyi 

Cobban and Scott, Fagesia sp., Neoptychites cephalotus 

(Courtiller), and Puebloites spiralis Cobban and Scott. 

Among the fossils collected from this bed along the Arkansas River valley in southeastern Colorado, is a form identified by J. B. Reeside, Jr., as Thomasites n. sp. (Dane and 

others, 1937, p. 214). This species, not to be confused with 

Reeside's Thomasites n. sp. from Kansas, was later described as Vascoceras (Greenhornoceras) birchbyi (Cobban 

and Scott, 1972, p. 84-87). 

The presence of Watinoceras coloradoense and Vascoceras birchbyi in the same bed of limestone that produced 

the types of Bassites reesidei clearly indicates an early Turonian age. W atinoceras coloradoense was proposed as a 

guide fossil for the lowest Turonian rocks of England (Hancock and Kennedy, 1980, p. 541; Wright and Kennedy, 

1981, table 1, p. 120), and the species was later noted in 
France (Kennedy and others, 1983, p. 177). Both W. coloradoense and Vascoceras birchbyi have been used as zonal 

fossils to the lower Turonian in the western interior (Cobban 

and Scott, 1972, tables 3, 4; Cobban, 1984, fig. 2, p. 82, 

83). 

Types .-Holotype USNM 395819, paratype USNM 

395820. 

REFERENCES CITED 

Bass, N.W., 1926, Geologic investigations in western Kansas, 

with special reference to oil and gas possibilities-Part 2, The 

geology of Hamilton County, Kansas: Kansas Geological 

Survey Bulletin 11, p. 53-83. 

Basse, Eliane, 1947, Les peuplements malgaches de Barroisiceras; Revision du genre Barroisiceras de Gross.: Annates de Paleontologie, v. 33, p. 97-177, pis. 7-15. 

Berthou, Pierre-Yves, Brower, J.C., and Reyment, R.A., 1975, 

Morphometrical study of Choffat's vascoceratids from Portugal: Geological Institutions of the University of Uppsala Bulletin, n. ser., v. 6, p. 73-83. 

Berthou, Pierre-Yves, and Lauverjat, Jacques, 1975, Le 

Cenomano-Turonien a Vascoceratides dans sa region type 

(embouchure du Rio Mondego, Beira littoral, Portugal: 

Newsletters on Stratigraphy, v. 4, no. 2, p. 96-118. 

Choffat, Paul, 1898, Les ammonees du Bellasien, des Couches a 

Neolobites Vibrayeanus, du Turonien et du Senonien, 2d ser., 

of Recueil d' etudes paleontologiques sur la faune cretacique 

du Portugal, v. 1, Especes nouvelles ou peu connues: Section 

des Travaux Geologiques du Portugal, p. 41-86, pis. 3-22. 

Cobban, W.A., 1971, New and little-known ammonites from the 

Upper Cretaceous (Cenomanian and Turonian) of the Western 

Interior of the United States: U.S. Geological Survey Professional Paper 699, 24 p., 18 pis. 

---1984, Mid-Cretaceous ammonite zones, Western Interior, 

United States: Geological Society of Denmark Bulletin, 

v. 33, pt. 1-2, p. 71-89. 

Cobban, W.A., and Scott, G.R., 1972 [1973], Stratigraphy and 

ammonite fauna of the Graneros Shale and Greenhorn Limestone near Pueblo, Colorado: U.S. Geological Survey Professional Paper 645, 108 p., 39 pis. 

Dane, C.H., Pierce, W.G., and Reeside, J.B., Jr., 1937, The 

stratigraphy of the Upper Cretaceous rocks north of the Arkansas River in eastern Colorado: U.S. Geological Survey 

Professional Paper 186-K, p. 207-232. 

Hancock, J.M., and Kennedy, W.J., 1980, Upper Cretaceous 

ammonite stratigraphy; Some current problems: Systematics 

Association Special Volume 18, The Ammonoidea, p. 531-

553. 

Kennedy, W.J., Wright, C.W., and Hancock, J.M., 1983, Ammonite zonation and correlation of the uppermost Cenomanian and Turonian of southern England and the type areas of 

Sarthe and Touraine in France: Memoires du Museum National d'Histoire Naturelle [Paris], n. ser., Serie C, Sciences 

de Ia Terre, v. 49, p. 175-181. 

Lauverjat, Jacques, and Berthou, Pierre-Yves, 1974, Le 

Cenomano-Turonien de I' embouchure du Rio Mondego Beira 

Litoral, Portugal: Comunica~6es dos Servi~os Geol6gicos de 

Portugal, v. 57, p. 263-301. 

Lohman, S.W., 1984, Memorial to Nathan Wood Bass, 1893-

1979: Geological Society of America Memorials, v. 14, 10 p. 

Weidmann, Jost, 1959 [1960], Le Cretace superieur de l'Espagne 

et du Portugal et ses cephalopodes, in Colloque sur le Cretace 

superieur fran~ais: Comptes Rendus du Congres des Societes 

Savantes de Paris et des Departments, Dijon, 1959, Section 

des Sciences, Sous-Section du Geologie, p. 709-764, 8 pis. 

Wright, C.W., and Kennedy, W.J., 1981, The Ammonoidea of 

the Plenus Marls and the Middle Chalk: Palaeontographical 

Society [Monograph]: 148 p., 32 pis. 

Wright, C.W., and Matsumoto, Tatsuro, 1954, Some doubtful 

Cretaceous ammonite genera from Japan and Saghalien: 

Memoirs of the Faculty of Science, Kyushu University, 

Series D, Geology, v. 4., no. 2, p. 107-134, pis. 7, 8. 

Zittel, K.A., 1895, Grundziige der Palaeontologie (Palaeozoologie ): Munich, R. Oldenbourg, VIII+ 971 p. 

New Ammonite, Upper Cretaceous of Kansas 83 

PLATE 1 

Contact photographs of the plates in this report are available at cost from U.S. Geological 

Survey Library, Federal Center, Denver, CO 80225 
PLATE 1 

[All figures natural size] 

Figures l-3. Bassites reesidei Cobban, n. sp. (p. Bl). 

Rear, side, and front views of the holotype USNM 395819, from the Bridge Creek Member of the Greenhorn 

Limestone at USGS Mesozoic locality 12773 in the SW l/4 sec. 14, T. 23 S., R. 42 W., Hamilton County, Kans. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

2 

BASSITES 

BULLETIN 1690-B PLATE 

3 

CHAPTER C 

The Upper Cretaceous (Cenomanian) 

Ammonites Metengonoceras Oumbli (Cragin) 

and M. Acutum Hyatt 

By William A. Cobban 

Description and illustrations of important 

international zonal fossi Is 

U.S. GEOLOGICAL SURVEY BULLETIN 1690 

Shorter Contributions to Paleontology and Stratigraphy 

CONTENTS 

Abstract Cl 

Introduction C 1 

Localities of collections Cl 

Systematic paleontology C2 

Family Engonoceratidae Hyatt C2 

Genus Metengonoceras Hyatt C2 

Metengonoceras dumbli (Cragin) C2 

M. acutum Hyatt C3 

Geographic distribution C3 

Stratigraphic distribution C5 

References cited C6 

PLATES 

[Plates follow References Cited) 

1-3. Metengonoceras 

FIGURES 

1. Sutures of Metengonoceras dumbli (Cragin) C4 

2. Collections and age assignments of Metengonoceras dumbli 

(Cragin) and M. acutum Hyatt C5 

Contents iii 

The Upper Cretaceous (Cenomanian) Ammonites 

Metengonoceras Dumbli (Cragin) and M. Acutum 

Hyatt 

By William A. Cobban 

Abstract 

Metengonoceras dumbli (Cragin) was originally described 

from the upper part of the Woodbine Formation of Texas. The 

species has since been found in western France and West 

Africa (Nigeria and Niger). Age range of the species is middle 

and late Cenomanian in France and middle Cenomanian in 

Texas. Metengonoceras acutum Hyatt, which was described 

from the Britton Formation of Texas, is known with certainty 

only in the United States and only in upper Cenomanian rocks. 

The species is closely related to M. dumbli, from which it 

differs mainly in retaining a sharp venter on the adult body 

chamber. 

INTRODUCTION 

Metengonoceras dumbli (Cragin) and M. acutum Hyatt 

are closely related, nearly smooth, very slender ammonites 

that have narrow, wedge-shaped whorl sections and peculiar, crowded sutures. The species have been difficult to 

separate because only the holotype of M. acutum has been 

illustrated, and only a couple of the American examples of 

M. dumbli have been figured. Crushed specimens from 

Iowa and fragments from Minnesota originally assigned to 

M. dumbli (Cobban, 1983, p. 11) now seem better assigned 

to M. acutum . The purpose of the present paper is to more 

fully describe and illustrate the two species and to document 

their geographic and stratigraphic ranges. 

All but one of the specimens illustrated in this report are 

kept in the National Museum of Natural History, Washington, D.C., where they have USNM catalog numbers. The 

exception is an example of M. acutum from Iowa, which is 

in the Yale Peabody Museum of Natural History, New 

Haven, Conn. R.E. Burkholder, of the U.S. Geological 

Survey, made the photographs. 

LOCALITIES OF COLLECTIONS 

U.S. Geological Survey localities of the collections of 

fossils that are illustrated or mentioned in this report are 

given below. The U.S. Geological Survey Mesozoic locality number, names of collectors, year of collection, locality, 

and stratigraphic assignment are as follows (prefix D indicates Denver Mesozoic locality numbers; others are Washington, D.C., Mesozoic locality numbers): 

20314. H.R. Bergquist, 1946. Bluffs along Templeton 

Branch of Cornelius Creek about 4.8 km (3 mi) 

north of Bells, Grayson County, Tex. Woodbine 

Formation, about 15m (50ft) below top of Templeton Member. 

22604. J.H. Renfro and R.F. Renfro. Mountain Creek 

about 3.2 km (2 mi) northeast of Britton, Tarrant 

County, Tex. Britton Formation. 

22606. J.H. Renfro and R.F. Renfro. Highway 287 cut 

8 km (5 mi) northwest of Midlothian, Ellis 

County, Tex. Britton Formation. 

D98. J.P. Conlin and W.A. Cobban, 1954. Bed of a 

tributary to Big Bear Creek on the Woodland Hill 

farm, 2.4 km (1 112 mi) east of Euless, Tarrant 

County, Tex. Woodbine Formation, from 

Lewisville Member. 

D3963. W.A. Cobban, 1957. SW 114 sec. 30, T. 20 S., 

R. 65 W., Pueblo County, Colo. Graneros Shale, 

from a ferruginous concretion 9.4 m (31 ft) below 

top. 

D5777. E.R. Landis and W.A. Cobban, 1967. SE 114 sec. 

8, T. 5 S., R. 2 E., Socorro County, N. Mex. 

Mancos Shale, from a thin bed of very fine 

grained sandstone in the lower part. 

D9481. J.D. Powell, 1968. East-flowing tributary to 

Templeton Branch of Cornelius Creek about 4.8 

km (3 mi) north of Bells, Grayson County, Tex. 

(same locality as Stephenson, 1952, p. 41, 

loc. 164). Woodbine Formation, from Templeton 

Member. 

D12634. Blaine Conley, 1965. Mesabi Range, Itasca 

County, Minn. Coleraine Formation. 

Metengonoceras Dumbli (Cragin) and M. Acutum Hyatt C1 
SYSTEMATIC PALEONTOLOGY 

Family ENGONOCERATIDAE Hyatt, 1900 

Genus METENGONOCERAS Hyatt, 1903 

Type species.-Metengonoceras inscriptum Hyatt, 1903, 

p. 180, pl. 25, figs. 5-9; pl. 26, figs. 1-4. Subsequent 

designation, Roman, 1938, p. 491. 

Diagnosis .-This genus includes very compressed, almost smooth ammonites that have tiny umbilici and narrow, 

flattened venters, which may round on the adult body chamber. Ornament consists of falcoid growth lines and, on some 

specimens, weak arcuate ribs a little above the middle of the 

flank and rarely faint umbilical bullae. Sutures are very 

closely spaced and have numerous auxilary and adventive 

elements with most saddles undivided and the larger lobes 

moderately frilled. 

Metengonoceras dumbli (Cragin) 

Plate 1, figures 3-6, 8; plate 2, figures 1-3, 9, 1 0; text-figure 1. 

1893. Sphenodiscus dumbli Cragin, p. 243, pl. 44, fig. 6. 

1893 [ 1894]. Sphenodiscus cf. pedernalis L. von Buch. De 

Grossouvre, p. 140, text-fig . .§8. 

1903. Metengonoceras dumbli (Cragin). Hyatt, p. 185, pl. 27, 

figs. 3-14. 

1908. Metengonoceras sp. De Grossouvre, p. 11, text figs. 1-3. 

1910. Metengonoceras dumblii [sic] (Cragin). Grabau and 

Shimer, p. 214, text fig. 1489a-d. 

1912. Metengonoceras sp. De Grossouvre, p. 33, text-fig. 5. 

1912. Metengonoceras Douvillei de Grossouvre, p. 34, pl. 3, fig. 

3; text-fig. 6. 

1912. Metengonoceras Arnaudi de Grossouvre, p. 35, text-fig. 7. 

1912. Metengonoceras tolveiense de Grossouvre, p. 36, pl. 3, 

fig. 4; text-fig. 8. 

1921. Metengonoceras dumblii [sic] (Cragin). Grabau, text-fig. 

1756a-d. 

1924. Epengonoceras dumbli (Cragin). Spath, p. 508. 

1925. Metengonoceras Arnaudi Grossouvre. Diener, p. 229. 

1925. Metengonoceras Douvillei Grossouvre. Diener, p. 229. 

1925. Metengonoceras Dumblei [sic] Cragin. Diener, p. 229. 

1925. Metengonoceras tolociense [sic] Grossouvre. Diener, 

p. 229. 

1925. Metengonoceras sp. ind. Grossouvre. Diener, p. 229. 

1928. Epengonoceras dumbli (Cragin). Adkins, p. 264. 

1931. Epengonoceras dumbli (Cragin). Reeside and Weymouth, 

p. 14. 

1935. Epengonoceras Dumbli Cragin. Furon, p. 55. 

1942. Epengonoceras dumbli (Cragin). Moreman, p. 217. 

1943. Metengonoceras Dumbli Cragin. Schneegans, p. 136, textfig. 17. 

1951. Metengonoceras dumblei [sic] (Cragin). Adkins and Lozo, 

pl. 2, fig. 5. 

1952. [1953]. Metengonoceras dumbli (Cragin). Stephenson, 

p. 206, pl. 55, figs. 1-4. 

1956. M etengonoceras (Epengonoceras) aff. dumbli (Cragin). 

Reyment, p. 58. 

1957. Epengonoceras dumbli (Cragin). Barber, p. 9, pl. 25, figs. 

9, 10. 

C2 Shorter Contributions to Paleontology and Stratigraphy 

?1972 [1973]. Epengonoceras dumbli (Cragin). Cobban and 

Scott, p. 59, pl. 8. 

1976 [1978]. Metengonoceras dumbli Cragin. Kennedy and 

Hancock, pl. 13, fig. 5a-c. 

1976 [1978]. Epengonoceras dumbeli [sic] (Cragin). Young 

and Powell, p. XXV.18. 

1981. Metengonoceras dumbli (Cragin). Kennedy and others, 

p. 32, pl. 3, figs. 1-5; pl. 7, figs. 4-6; text figs. 4A-G, 5B-F. 

Types. -Lectotype USNM 29403, from Grayson 

County, Texas; hypotypes USNM 401493-401500, from 

Grayson and Tarrant Counties, Texas. 

Description .-Cragin (1893, p. 243) had nearly 20 specimens of Metengonoceras dumbli from several localities in 

northeastern Texas, but his only illustration was the external 

suture of one specimen. Hyatt (1903, p. 185, pl. 27, figs. 

3-14) described and illustrated "a superb specimen" from 

the Cragin collection, and this specimen has been designated the lectotype by Kennedy and others ( 1981 , p. 34). 

The specimen is an internal mold 94 mm in diameter with 

an umbilical ratio of 0.08. An incomplete body chamber 

occupies the last half whorl; diameter at its base is about 

69 mm. Whorls are very compressed and much higher than 

wide with the greatest width low on the flank. The venter is 

sharp on the outer whorl of the phragmocone and on the 

adjoining part of the body chamber. Most of the venter of 

the body chamber is not preserved, but the younger end is 

rounded and has a narrow midventral flattening. Ornament 

other than faint falcoid growth lines is lacking. Both the 

external and internal sutures were described and illustrated 

in detail by Hyatt (1903, p. 187, pl. 27, figs. 9-14). The 

lateral lobe and the adventitious lobes have narrow necks 

and then expand with two or three branches on each side. 

Saddles that separate these lobes are rounded and undivided. 

Most of the lobes between the lateral one and the umbilicus 

are narrow and mostly bifid, and the saddles that separate 

them are broad, shallow, and bifid to undivided. There are 

13 lobes in the external suture. 

A large topotype figured by Stephenson (1952, p. 207, 

pl. 55, figs. 2-4) has a diameter of 142 mm with a diameter 

of 108 mm at the base of the body chamber. The venter of 

the phragmocone of this internal mold is sharp, whereas the 

venter at the larger end of the body chamber is well rounded. 

The largest collection of M. dumbli at hand consists of 

nine well-preserved internal molds from the Templeton 

Member of the Woodbine Formation at USGS Mesozoic 

locality 09481 near Bells, Grayson County, Tex. Diameters 

(rounded) at the base of body chambers are 64, 65, 66, 79, 

83, 84, 88, 89, and 94 mm. Although internal molds of the 

outer whorls of the phragmocones have sharp venters, specimens that retain a little shell material reveal narrow, flat to 

concave venters (pl. 1, figs. 4, 6) as noted by Stephenson 

(1952, p. 206). External sutures of four of these specimens 

are shown in figure 1. The external lobe (E), which is not 
centered on the middle of the venter, is short and bifid and 

usually has a narrow neck. The lateral lobe and the first two 

adventitious lobes are bifid and have two branches on each 

side. Other adventitious lobes are smaller and mostly bifid. 

The first inner lobe adjacent to the lateral one is a little 

smaller than that one but branched much like it. The rest of 

the inner lobes are smaller and usually bifid. Saddles that 

separate these lobes are either bifid or undivided. There are 

about eight lobes between the lateral one and the umbilical 

seam. For illustrations of sutures of four other specimens of 

M. dumbli from northeastern Texas, the reader is referred to 

Kennedy, Juignet, and Hancock (1981, text fig. 5B-F). 

Metengonoceras acutum Hyatt 

Plate 1, figures 1, 2, 7; plate 2, figures 4-8; plate 3 

1893. Placenticeras (Sphenodiscus) sp. undet. Winchell, 

p. 221. 

1903. Metengonoceras acutum Hyatt, p. 184, pl. 26, fig. 8; 

pl. 27, figs. 1, 2. 

1925. Metengonoceras acutum Hyatt. Diener, p. 229. 

1928. Metengonoceras(?) acutum Hyatt. Adkins, p. 264. 

1931. Epengonoceras acutum (Hyatt). Reeside and Weymouth, 

p. 16. 

?1935. Metengonoceras nigeriensis Furon, p. 55, pl. 3, fig. 1a, b; 

text-fig. 16. 

1942. Protengonoceras planum Hyatt. Moreman, p. 217. 

1942. Epengonoceras acutum (Hyatt). Moreman, p. 218. 

?1943. Metengonoceras nigeriensis Furon. Schneegans, p. 137. 

1944. Epengonoceras cf. E. dumblei [sic] (Cragin). Bergquist, 

p. 30. 

1981. Metengonoceras acutum (Cragin). Kennedy and others, 

p. 36, text-fig. 5A. 

1983. Metengonoceras dumbli (Cragin). Cobban, p. 11, pl. 6; 

pl. 7, fig. 8; pl. 8, figs. 6, 7. 

Types .-Hypotypes USNM 401501-401503, from 

Itasca County, Minnesota and Ellis and Tarrant Counties, 

Texas; YPM 593, from Woodbury County, Iowa. 

Description . -This species seems to have. been based on 

two specimens, one of which (the holotype), was illustrated 

by side and end views and the external suture (Hyatt, 1903, 

pl. 26, fig. 8; pl. 27, figs. 1, 2). The holotype is an internal 

mold of most of ari outer septate whorl that has a diameter 

of about 100 mm and an umbilicus of 5 mm (0.05). Hyatt 

(1903, p. 184) briefly described the species as "The form is 

much compressed and involute, with more acute venter than 

in M. inscriptum. The umbilical shoulders also in this species are more prominent and entire, and short but distinct, 

broad, fold-like costae are present near the umbilical shoulders, but do not cross them. There are no tubercles on the 

fragments observed." The external suture, which closely 

resembles that of M. dumbli, has a small off-centered, bowtie-like external lobe and 10 narrow-necked lobes separated 

by broad, mostly undivided saddles. The lateral lobe and the 

first two adventitious lobes have two or three simple 

branches on each side. Other lobes are smaller, narrower, 

and bifid or trifid. One of the lobes midway between the 

lateral one and the umbilicus is peculiar in that it is deeply 

bifid. 

Remarks .-Hyatt (1903, p. 185) noted that his specimens were preserved as red calcareous claystone, which 

T. W. Stanton (personal commun.) informed him was typical of "brownish-red concretions*** in weathered portions 

of the Eagle Ford shales." A few fragments of internal 

molds of Metengonoceras are preserved in this manner in 

the USGS Mesozoic collections from northeastern Texas 

(pl. 2, figs. 4-8). These fragments are from rocks now 

assigned to the Britton Formation. Fragments of body chambers are narrower than those of M. dumbli and have sharp 

venters. Fragments of internal molds of body chambers 

from the Coleraine Formation of northeastern Minnesota 

also have sharp venters and seem referable toM. acutum 

(pl. 1, figs. 1, 2, 7). An internal mold of most of a very 

large body chamber from the lower part of the Mancos Shale 

in south-central New Mexico (USGS Me~ozoic loc. D5777) 

has a sharp venter and seems assignable toM. acutum. 

Types . -The holotype was at the Harvard Museum of 

Comparative Zoology at the time of Hyatt's study. 

Kennedy, Juignet, and Hancock (1981, p. 36) were unable 

to locate it. The specimen apparently came from the Britton 

Formation on Elm Fork of the Trinity River in Dallas 

County, Tex. 

GEOGRAPHIC DISTRIBUTION 

M etengonoceras dumbli has been recorded from the 

United States, France, and West Africa. A discoidal ammonite from Colombia that was identified as 

"Spengonoceras ef dumblei Gracin" (Ujueta, 1962, pl. 1, 

fig. 3) appears to be too poorly preserved for even generic 

determination. 

American records are from northeastern Texas (Cragin, 

1893, p. 244; Hyatt, 1903, p. 187; Moreman, 1942, p. 217; 

Stephenson, 1952, p. 207; Kennedy and others, 1981, 

p. 36), southeastern Colorado (Cobban and Scott, 1972, 

p. 59), Iowa (Cobban, 1983, p. 11), and Minnesota 

(Bergquist, 1944, p. 30; Cobban, 1983, p. 11). The specimens from Iowa and Minnesota are herein reassigned to 

M. acutum. 

Metengonoceras dumbli has been well documented from 

western France (Kennedy and others, 1981, p. 32, pl. 3, 

figs. 1-5; pl. 7, figs. 4-6; text fig. 4A, B, D-G). Specimens from this area were described by de Grossouvre (1912) 

as M. douvillei, M. arnaudi, and M. tolveiense. All can be 

interpreted as synonyms of M. dumbli. 

African records of M. dumbli are from Niger (Furon, 

1935, p. 55) and northeastern Nigeria (Barber, 1957, p. 9). 

The form from Niger that was described as M. nigeriensis 

Metengonoceras Dumbli (Cragin) and M. Acutum Hyatt Cl 
) 

A 

5 mm 

8 

c 

5mm 

D 

Figure 1. External sutures of Metengonoceras dumbli (Cragin) from USGS Mesozoic locality 09481. A, Hypotype USNM 401497 

at a diameter of 57.5 mm. 8, Hypotype USNM 401498 at a diameter of 63 mm. C, Hypotype USNM 401499 at a whorl height 

of 39.5 mm. 0, Hypotype USNM 401500 at a diameter of 87 mm. E is the external lobe, L is the lateral lobe, and A1-A4 are 

adventitious lobes. Heavy straight line marks the middle of the venter; curved solid line marks the umbilical seam; curved dashed 

line marks the umbilical shoulder. 

C4 Shorter Contributions to Paleontology and Stratigraphy 
by Furon (1935, p. 55, pl. 3, fig. 1a, b; text-fig. 16) and 

later assigned toM. dumbli by Schneegans (1943, p. 136) 

is herein interpreted as a probable M. acutum Hyatt. Furon's 

type has a more sharpened venter than that of typical 

M. dumbli. 

Metengonoceras acutum is not as abundant as M. dumbli 

and does not have as wide a geographic range. The questionable occurrence in Niger may be the only record outside the 

United States. Hyatt's type specimen of M. acutum and a 

few fragments in the U.S. Geological Survey's collections 

are from northeastern Texas. Other specimens are from 

northwestern Iowa and northeastern Minnesota. Part of a 

very large body chamber from the lower part of the Mancos 

Shale in south-central New Mexico may also represent this 

species. 

STRATIGRAPHIC DISTRIBUTION 

M etengonoceras dumbli seems to be confined to rocks of 

middle Cenomanian age in the United States (fig. 2) and to 

rocks of middle to late Cenomanian age in France (Juignet 

and others, 1978, fig. 11). 

The oldest specimens are from the Lewisville Member of 

the Woodbine Formation at USGS Mesozoic locality D98 in 

Tarrant County, Tex. (same as loc. 55 of Stephenson, 1952, 

p. 37). Here several complete adults were found along with 

STAGE ZONE LOCALITY 

i= Sciponoceras gracile o USGS 22604 

a: 

<{ 

a.. 

- Metoicoceras mosbyense o USGS 012634 

a: 

w 

i= a.. 

a.. a: ::J Dunveganoceras pondi o YPM 2264 

<{ 

a.. 

-

z Plesiacanthoceras wyomingense • USGS 09481 

~ 

z 

<{ Acanthoceras amphibo/um ::?i w 0 ...J 

z 0 

w 0 Acanthoceras bellense 

u ::?i 

Acanthoceras muldoonense e USGS 03963 

Conlinoceras tarrantense e USGS 098 

Figure 2. Collections of Metengonoceras dumbli (e) and M. 

acutum (0) and their probable age assignments to the Cenomanian ammonite zonation of the western interior of the United 

States. 

many specimens of Conlinoceras tarrantense (Adkins). 

This is the type locality of Turrilites dearingi Stephenson 

and Forbesiceras conlini Stephenson. Kennedy (1971, 

p. 31) regarded T. dearingi as a probable synonym of T. 

acutus Passy. In England, T. acutus and species of Forbesiceras are conspicuous members of the Turrilites acutus 

assemblage of the Acanthoceras rhotomagense Zone 

(Kennedy, 1971, p. 102). The T. acutus assemblage is the 

middle of three middle Cenomanian assemblages that make 

up the A. rhotomagense Zone. The oldest is the Turrilites 

costatus assemblage, and the youngest is the Acanthoceras 

jukes-brownei assemblage. 

The next oldest level of M. dumbli may be represented by 

an unusually large specimen from the Graneros Shale at 

USGS Mesozoic locality D3963 near Pueblo, Colo. (Cobban and Scott, 1972, p. 59, pl. 8). Associated ammonites 

include Acanthoceras muldoonense Cobban and Scott. 

The holotype and other specimens from the Templeton 

Member of the Woodbine Formation in northeastern Texas 

may be the youngest forms of M. dumbli in the United 

States. USGS Mesozoic locality 20314 (Stephenson, 1952, 

p. 41, loc. 164) near Bells, Grayson County, Tex., is important in dating the Templeton Member. HereM. dumbli was 

associated with the holotype of Mammites? bellsanus 

Stephenson (1952, p. 204, pl. 49, fig. 3; pl. 51, figs. 8-11) 

and Metoicoceras crassicostae Stephenson (1952, p. 210, 

pl. 58, figs. 6-8). Mammites? bellsanus is better assigned 

to Plesiacanthoceras Haas (1964) and is closely related to, 

but distinct from P. wyomingense (Reagan), an index fossil 

to the latest middle Cenomanian ammonite zone in the westem interior of the United States. Metoicoceras is scarce in 

the zone of P. wyomingense in the western interior region, 

but some juveniles and bits of larger specimens associated 

with P. wyomingense suggest some species much like M. 

crassicostae. The Templeton Member is probably about the 

age of the zone of P. wyomingense . 

French specimens of Metengonoceras assigned to 

M. dumbli by Kennedy, Juignet, and Hancock ( 1981) may 

be all from a late Cenomanian zone equivalent to the zone 

of Sciponoceras gracile in the western interior of the United 

States. Ammonites from the Sables a Catopygus obtusus 

includeS. gracile, Metengonoceras cf. M. dumbli, Metengonoceras sp., Euomphaloceras septemseriatum (Cragin), 

Calycoceras naviculare (Mantell), and Metoicoceras 

geslinianum (d'Orbigny) (Kennedy and others, 1981, 

p. 30). The species of Euomphaloceras, Calycoceras, and 

M etoicoceras also occur in the western interior zone of 

S. gracile. Amedro, Badillet, and Devalque (1982, p. 172) 

list the additional species Allocrioceras sp. and Vascoceras 

diartianum (d'Orbigny), both of which also occur in the 

American zone of S. gracile. Juignet, Kennedy, and Lebert 

(1978, p. 92) have also listed M. dumbli from the older 

Sables et Gres du Mans, which contains an Acanthoceras 

rhotomagense (Brongniart) fauna of middle Cenomanian 

age. 

Metengonoceras Dumbli (Cragin) and M. Acutum Hyatt C5 
The oldest specimens of M etengonoceras acutum (pl. 3) 

are from ferruginous, siltstone concretions in the basal part 

of the Graneros Shale at Riverside in northwestern Iowa. 

Flattened adult specimens were considered as M. dumbli 

(Cobban, 1983, p. 11), but an assignment to M. acutum 

seems more likely because of their acute venters on body 

chambers. Dunveganoceras pondi Haas is found with them. 

Fragments of sharp-ventered internal molds in ferruginous concretions in the Coleraine Formation of the Mesabi 

Range in northeastern Minnesota seem assignable to M. 

acutum. The are associated with Dunveganoceras hagei 

Warren and Stelck and Metoicoceras bergquisti Cobban. 

According to Warren and Stelck (1955, p. 63), D. hagei is 

the youngest of five zones of Dunveganoceras . Of the species in the western interior of the United States, D. hagei is 

most closely related to D. conditum Haas from the upper 

part of the late Cenomanian zone of M etoicoceras mosbyense Cobban. 

Hyatt's specimens of Metengonoceras acutum came from 

a locality on the Elm Fork of Trinity River in Dallas County, 

Tex. This is locality 16 of Moreman (1942, p. 197). Here 

the Britton Formation crops out, and all fossils from it 

indicate the late Cenomanian zone of Sciponoceras gracile 

(Shumard). A graphic section at this locality with some of 

the megafossils is shown by Norton (1965, pl. 2), who 

found a questionable M. acutum in the middle of the Britton. 

Other ammonites from the middle of the Britton include 

Euomphaloceras (Kanabiceras) septemseriatum (Cragin), 

Metoicoceras geslinianum (d'Orbigny), and Allocrioceras 

annulatum (Shumard) (names updated from those listed by 

Norton). A collection from the Britton Formation near Britton Tex. (USGS 22604) contains half a whorl of a body 

chamber of M. acutum (pl. 2, figs. 4, 8) along with specimens of E. septemseriatum, M. geslinianum, A. annulatum, Sciponoceras gracile (Shumard), and Scaphites brittonensis Moreman. 

REFERENCES CITED 

Adkins, W.S., 1928, Handbook of Texas Cretaceous fossils: 

Texas University Bulletin 2838, 385 p., 37 pis. 

Adkins, W.S., and Lozo, F.E., Jr., 1951, Stratigraphy of the 

Woodbine and Eagle Ford, Waco area, Texas, in Lozo, F.E., 

Jr., ed., The Woodbine and adjacent strata of the Waco area 

of central Texas: Fondren Science Series, no. 4, p. 101-164, 

pls. 1-6. 

Amedro, F., Badillet, G., and Devalque, Ch., 1982 [1983], Biostratigraphie et biozonation des ammonites du Turonien fran-

~ais: Memoires du Museum National d'Histoire Naturelle 

Paris, n. ser., C, v. 49, p. 167-173. 

Barber, W.M., 1957, Lower Turonian ammonites from northeastern Nigeria: Nigeria Geological Survey Bulletin 26, 

67 p., 34 pls. 

Bergquist, H.R., 1944, Cretaceous of the Mesabi iron range, Minnesota: Journal of Paleontology, v. 18, no. 1, p. 1-30, 

pls. 1-11. 

C6 Shorter Contributions to Paleontology and Stratigraphy 

Cobban, W.A., 1983, Molluscan fossil record from the northeastern part of the Upper Cretaceous seaway, Western Interior, in 

Cobban, W.A., and Merewether, E.A., Stratigraphy and paleontology of mid-Cretaceous rocks in Minnesota and contiguous areas: U.S. Geological Survey Professional Paper 

1253-A, p. 1-25, 15 pls. 

Cobban, W.A., and Scott, G.R., 1972 [1973], Stratigraphy and 

ammonite fauna of the Graneros Shale and Greenhorn Limestone near Pueblo, Colorado: U.S. Geological Survey Professional Paper 645, 108 p., 39 pis. 

Cragin, F. W., 1893, A contribution to the invertebrate paleontology of the Texas Cretaceous: Texas Geological Survey 4th 

Annual Report, pt. 2, p. 139-246, pis. 24-46. 

Diener, Carl, 1925, Ammonoidea neocretacea, Pt. 29 of Animalia, 

[Pt.] 1 of Diener, Carl, ed., Fossilium catalogus: Berlin, 

W. Junk, 244 p. 

Furon, Raymond, 1935, Le Cretace et le Tertiaire du Sahara soudanais (Soudan, Niger, Tchad): Museum National Histoire 

Naturelle Archives, 6th ser., v. 13, p. 1-96, pls. 1-7. 

Grabau, A.W., 1921, A textbook of geology, pt. 2, Historical 

geology: New York, D.C. Heath and Co., 976 p. 

Grabau, A.W., and Shimer, H.W., 1910, North American index 

fossils, v. 2: New York, A.G. Seiler and Company, 909 p. 

Grossouvre, Albert de, 1893 [1894], Les ammonites de la craie 

superieure, Pt. 2, Paleontologie, of Recherches sur la craie 

superieure: Carte Geologique Detaillee de la France Memoires, 264 p., 39 pls. 

---1908, Description des ammonitides du cretace superieur du 

Limbourg Beige et Hollandais et du Hainaut: Musee Royale 

d'Histoire Naturelle de Belgique Memoires, v. 4, p. 1-38, 

pls. 1-11. 

---1912, Le Cretace de la Loire-Inferieure et de la Vendee: 

Societe des Sciences Naturelles de l'Ouest de la France Bulletin, 3d ser., v. 2, p. 1-38, pls. 1-3. 

Haas, Otto, 1964, Plesiacanthoceras, new name for Paracanthoceras Haas, 1963, non Furon, 1935: Journal of Paleontology, v. 38, no. 3, p. 610. 

Hyatt, Alpheus, 1900, Cephalopoda, in Zittel, K.A. von, Textbook of palaeontology [1896-1900]: London, MacMillan, 

p. 502-604. 

Hyatt, Alpheus, edited by T.W. Stanton, 1903, Pseudoceratites of 

the Cretaceous: U.S. Geological Survey Monograph 44, 351 

p., 47 pis. 

Juignet, Pierre, Kennedy, W.J., and Lebert, Andre, 1978, Le 

Cenomanien du Maine; formations sedimentaires et faunes 

d'ammonites du stratotype: Geologie Mediterraneenne, v. 5, 

no. 1, p. 87-100. 

Kennedy, W .J., 1971, Cenomanian ammonites from southern 

England: Palaeontological Association of London Special 

Papers in Palaeontology 8, 133 p., 64 pls. 

Kennedy, W.J., and Hancock, J.M., 1976 [1978], The midCretaceous of the United Kingdom, in Mid-Cretaceous 

events, Uppsala-Nice symposium, 1975-1976: Annales du 

Museum d'Histoire Naturelle de Nice, v. 4, p. v.1-v.72, 

30 pis. 

Kennedy, W.J., Juignet, Pierre, and Hancock, J.M., 1981, Upper 

Cenomanian ammonites from Anjou and the Vendee, western 

France: Palaeontology, v. 24, pt. 1 , p. 25-84, pis. 3-17. 

Moreman, W.L., 1942, Paleontology of the Eagle Ford group of 
north and central Texas: Journal of Paleontology, v. 16, 

no. 2, p. 192-220, pls. 31-34. 

Norton, G.H., 1965, The surface geology of Dallas County, 

Texas, in The geology of Dallas County: Dallas Geological 

Society, p. 40-125. 

Reeside, J.B., Jr., and Weymouth, A.A., 1931, Mollusks from the 

Aspen shale (Cretaceous) of southwestern Wyoming: United 

States National Museum Proceedings, v. 78, art. 17, p. 1-24, 

pls. 1-4. 

Reyment, Richard, 1956, On the stratigraphy and palaeontology of 

the Cretaceous of Nigeria and the Cameroons, British West 

Africa: Geologiska Foreningens i Stockholm Forhandlingar, 

v. 78, pt. 1, no. 484, p. 17-96. 

Roman, Frederic, 1938, Les ammonites jurassiques et cretacees; 

Essai de genera: Paris, Masson et Cie, 554 p., 53 pls. 

Schneegans, Daniel, 1943, Invertebres du Cretace superieur de 

Damergou (Territoire du Niger), in Etudes stratigraphiques et 

paleontologiques sur le Bassin du Niger: French West Africa 

Direction Mines Bulletin 7, p. 87-166, 8 pls. 

Spath, L.F., 1924, On a new ammonite (Engonoceras iris, sp. n.) 

from the Gault of Folkestone: Annals and Magazine of Natural History, 9th ser., v. 14, no. 82, p. 504-508. 

Stephenson, L. W., 1952 [ 1953], Larger invertebrate fossils of the 

Woodbine formation (Cenomanian) of Texas: U.S. Geological Survey Professional Paper 242, 211 p., 58 pls. 

Ujueta, L.G., 1962, Geologia de Noreste de Bogota: Servicio 

Geologico Nacional Colombia Boletin Geologico, v. 9, nos. 

1-3, p. 23-46, 7 pis. 

Warren, P.S., and Stelck, C.R., 1955, New Cenomanian ammonites from Alberta: Research Council of Alberta Report 

No. 70, p. 63-75, pls. 4-9. 

Winchell, H.V., 1893, Note on Cretaceous in northern Minnesota: 

The American Geologist, v. 12, no. 4, p. 220-223. 

Young, Keith, and Powell, J.D., 1976 [1978], Late Albian-Turonian correlations in Texas and Mexico, in Mid-Cretaceous 

events, Uppsala-Nice symposium, 1975-1976: Annales du 

Museum d'Histoire Naturelle de Nice, v. 4, p. XXV.1-

XXV .36, 9 pls. 

Metengonoceras Dumbli (Cragin) and M. Acutum Hyatt C7 

PLATES 1-3 

Contact photographs of the plates in this report are available at cost from U.S. Geological 

Survey Library, Federal Center, Denver, CO 80225 
Figures 

PLATE 1 

[All figures natural size] 

1, 2, 7. Metengonoceras acutum Hyatt (p. C3). 

Rear, bottom, and side views of hypotype USNM 401501, from USGS Mesozoic locality 012634 in the Mesabi Range, Itasca 

County, Minn. 

3-6, 8. Metengonoceras dumbli (Cragin) (p. C2). 

From USGS Mesozoic locality 09481 north of Bells, Grayson County, Tex. 

3, 4. Hypotype USNM 401493. 

5, 6, 8. Hypotype USNM 401494. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

METENGONOCERAS 

BULLETIN 1690-C PLATE 
PLATE 2 

[All figures natural size] 

Figures 1- 3, 9, 10. Metengonoceras dumbli (Cragin) (p. C2). 

From USGS Mesozoic locality 098 on Big Bear Creek near Euless, Tarrant County, Tex. 

1- 3. Hypotype USNM 401495. 

9, 10. Hypotype USNM 401496. 

4- 8. Metengonoceras acutum Hyatt (p. C3). 

5-7. Hypotype USNM 401502, from USGS Mesozoic locality 22606 near Midlothian, Ellis County, Tex. 

4, 8. Hypotype USNM 401503, from USGS Mesozoic locality 22604 near Britton, Tarrant County, Tex. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

5 

' 'I 

~ / 

I 

( 

;1·~1 ' I' 

,_) 

,, 

\ I \ 

'>. '' 

·" 

BULLETIN 1690--C PLATE 2 

4 

METENGONOCERAS 
PLATE 3 

[Figure is natural size] 

Metengonoceras acutum Hyatt (p. C3). 

Hypotype Yale Peabody Museum 593, from the basal part of the Graneros Shale at the Sioux City Brick and Tile Company's clay pit in North Riverside, 

Iowa . 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

• J 

t' .. 

·~ ,-• . 

\ 

l 

\ 

BULLETIN 1690--C PLATE 3 

METENGONOCERAS 

CHAPTER D 

Middle Devonian Coral Faunules from Illinois 

and Their Bearing on Biogeography 

By William A. Oliver, Jr. 

U.S. GEOLOGICAL SURVEY BULLETIN 1690 

Shorter Contributions to Paleontology and Stratigraphy 

CONTENTS 

Abstract Dl 

Introduction Dl 

Acknowledgments Dl 

Lingle corals Dl 

Stratigraphy Dl 

Previous work on rugose corals D3 

New faunule D3 

Siphonophrentis sp. aff. S. halli (E. and H.) D3 

Tabulophyllum sp. cf. T. conatum (Hall) D3 

T. sp. cf. T. zaphrentiforme (Davis) D3 

Heliophyllum sp. cf. H. halliE. and H. D4 

Bethanyphyllum sp. aff. B. robustum (Hall) D4 

Prismatophyllum arachnoideum (Stumm) D4 

Eridophyllum sp. cf. E. archiaci (Billings) D4 

E. n. sp. A. D4 

Acanthophyllum sp. DS 

Ptenophyllid coral, undetermined DS 

"Anderdon" corals DS 

Stratigraphy DS 

New coral faunule DS 

Amphipora nattressi (Grabau) DS 

Grypophyllym n. sp. A DS 

Holmophyllia n. sp. A D6 

Biogeography D6 

Introduction D6 

Lingle faunule D6 

"Anderdon" faunule D7 

Logansport, Indiana D7 

Michigan Basin D7 

Discussion D8 

Summary and conclusions D8 

References cited D8 

PLATES 

[Plates follow References Cited] 

1-4. Corals from the Lingle Limestone 

5, 6. "Anderdon" corals 

FIGURE 

1. Index map showing distribution of Grand Tower and Lingle Limestones and correlative units D2 

TABLES 

1. Subsurface Devonian stratigraphy from Herkimer No. 5 well core, Coles County, 

Illinois D3 

2. Rugose corals from the outcropping "Lingle" Limestone D3 

3. Corals from the Herkimer No. 5 well core, Coles County, Illinois D4 

4. Ptenophyllids in the Eastern Americas Realm D7 

5. Corals from the Miami Bend Limestone D7 

Contents iii 

Middle Devonian Coral Faunules from Illinois and 

Their Bearing on Biogeography 

By William A. Oliver, Jr. 

Abstract 

Two rugose coral faunules from a single well in Coles 

County, Ill., are of contrasting origins. A Lingle Limestone 

faunule is of Centerfield age (Givetian). It is dominated by 

characteristic Eastern Americas Realm corals, but includes 

three specimens of Old World Realm ptenophyllids. An upper 

Grand Tower Limestone faunule is derived from the Michigan 

Basin Anderdon Limestone of late Onondaga age (Eifelian). 

This contains only two species of rugose corals, both having 

Old World Realm affinities. The Old World corals of both 

faunules are thought to have entered the Michigan Basin from 

the west and to have migrated from there into the Illinois Basin. 

An analogous superposition of Old World and Eastern Americas corals is known in the Logansport, Ind., area on the Kankakee Arch that separates the Michigan and Illinois basins. 

INTRODUCTION 

Two coral faunules from the subsurface Devonian strata 

of Coles County, Ill. , are important because of their biogeographic affinities. An assemblage from the upper part of the 

Lingle Limestone is of Centerfield (Givetian) age and dominated by genera and species characterisitic of the Eastern 

Americas Realm, Appohimchi Province, although it includes two ptenophyllids that have Old World relationships. 

An older assemblage, from the top of the Grand Tower 

Limestone (Eifelian) in the same well, includes two coral 

species, both of which indicate an Old World source. These 

are part of a fauna previously related to the Michigan Basin 

Anderdon Limestone by Linsley and Kesling (1982). 

The Old World elements in both faunules probably entered the Illinois Basin from the Michigan Basin where Old 

World faunas are intermixed or interbedded with more common Eastern Americas species. Old World access to the 

Michigan Basin was apparently from the Williston Basin 

which was part of the Old World Realm. 

Both faunules were recovered from the Herkimer No. 5 

well in Coles County, Ill. (fig. 1 , loc. 1). Pertinent parts of 

the stratigraphic sequence in the well are shown in table 1, 

extracted from drilling records in the files of the Illinois 

Geological Survey. The Lingle corals were taken from a 

core 3 112 inches in diameter, from the interval 3, 121-3, 125 

feet; this is 4-9 feet below the top of the formation and some 

42 feet above its base. The "Anderdon" corals were bailed 

by the driller from a cave ("crevasse") at 3,167-3,172 feet. 

The drilling record describes "gallons of corals every run" 

but only some 20 specimens are in the preserved collections. 

Acknowledgments 

I am indebted to Dr. Lois S. Kent, Curator and Geologist, 

Illinois Geological Survey, for aiding in the search for the 

"Anderdon" corals, for calling my attention to the Lingle 

corals, for providing the drilling records with stratigraphic 

interpretations, and for her patience in allowing me to have 

the collections in my own laboratory for a prolonged period. 

The "Anderdon" corals were originally brought to my attention by Prof. R.M. Linsley while he was studying the gastropods from the same interval. The manuscript was critically reviewed by A.E.H. Pedder, Geological Survey of 

Canada, Calgary, Charles Collinson, Illinois State Geological Survey, Champaign, and by J.T. Dutro, Jr., and W.J. 

Sando, U.S. Geological Survey, Washington, D.C. Thin 

sections and photographs are by W. C. Pinckney, Jr.; photo 

processing is by H.E. Mochizuki. 

LINGLE CORALS 

Stratigraphy 

The regional stratigraphy of the Middle Devonian in central and southern Illinois was discussed by North (1969). In 

Coles County, the Lingle (15m; 50 feet thick) is overlain by 

the New Albany Shale Group and overlies the Grand Tower 

Limestone (North, 1969, fig. 13). The corals came from the 

upper 2 m (8 feet) of the Lingle (table 1). 

Cooper and others (1942) correlated the Lingle Limestone 

with the Beechwood Limestone Member of the Sellersburg 

Limestone of Kentucky and the Centerfield Limestone 

Member of the Ludlowville Formation of New York. 

Cooper's "Lingle" is only the upper part of the Lingle Limestone as defined by North (1969), but it is the part represented by the Lingle corals described here which are clearly 

of Centerfield affinities. North identified the subsurface 

Lingle in Coles County as the Tripp Limestone Member 

overlying a thin Howardton Limestone Member (North, 

1969, p. 20, fig. 13). However, in the southwest Illinois 

outcrop area, these units constitute the lower, preCenterfield, part of the Lingle, and North's interpretation of 

the subsurface Devonian (1969, p. 12, fig. 6) must be questioned. The Lingle Limestone as a whole is of Hamilton age, 

probably ranging from Mottville (basal Skaneateles Shale) 

to Centerfield (basal Ludlowville Formation) or slightly 

higher, in New York terms (Cooper and others, 1942, 

Middle Devonian Coral Faunules, Illinois Dl 
430 

DOME 

EXPLANATION 

-- Edge of Grand Tower L1mestone 

and equ1valents 

r--r---1 Edge of L1ngle Limestone and equivalents where they extend beyond 

the Grand Tower 

- - - Boundary of areas where the T1oga 

Bentonite has been found 

0 20 

I I I I 

0 20 40 

80 MILES 

I 

1

KY. 

MO.J 

~--- ) TENN. 

\ K 

840 

MICHIGAN 

BASIN 

v 

~ 

:I: 

u 

a: 

<( 

1-

<( 

2 

----,-----

v 

Figure 1. Distribution of Grand Tower and Lingle Limestones and correlative units and their relation to major structures (from 

North, 1969). Principal localities are marked: 1, Herkimer No.5 well, Coles County, Illinois; 2, Logansport, Indiana area. The age 

of the formations truncating the Grand Tower are indicated by a letter: Q, Quaternary; K, Cretaceous; P, Pennsylvanian; M, 

Mississippian and Upper Devonian. 

D2 Shorter Contributions to Paleontology and Stratigraphy 
Table 1. Subsurface Devonian stratigraphy in Herkimer 

No.5 well, Coles County, Illinois 

[Sec. II, T.I2N.,R. 7E.;IllinoisGeologicaiSurvey,core#2687. Coral 

faunules are from 3,121 to 3,125 feet and from the "crevasse" at 3,167 to 

3,172 feet. Data from driller's logs in files of the Illinois State Geological 

Survey. Surface elevation, 696 feet] 

Depth below surface, in feet 

Surlace --------------------------------------- 0 

Carboniferous - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - - 108-3,009 

New Albany Shale Group ---------------------3,009-3,117 

Lingle Limestone - - - - - - - - - - - - --- - - -- - - - - - - -- -3, 117-3, 167 

Limestone - - - - - - - - - - - - - - - - - - -3, 117-3, 120 

Diamond Core # 1 - - - - - - - - - - - -3, 120-3, 134 

Limestone, coralliferous- - - -3, 120-3, 121 

Limestone, fossiliferous--- -3,121-3,123 

Favosite coral bioherm---- -3,123-3,125 

Limestone, fossiliferous---- 3,125-3,133 

Limestone, shaly--------- -3,133-3,134 

Limestone, varied descriptions 

and cored in part----------3,134-3,167 

Grand Tower Limestone---------------------- -3,167-3,172 

"Crevasse" or cave------------3,167-3,172 

Bottom of hole ----------------------------------- -3,172 

p. 1770; Collinson and others, 1968, p. 956; North, 1969; 

Willman and others, 1975, p. 118). Within the Hamilton of 

eastern North America, the Centerfield fauna is the most 

widespread, having been recognized from New York and 

Pennsylvania to Tennessee, Kentucky, Illinois, Michigan, 

and southwestern Ontario (Cooper and others, 1942, chart; 

Cooper and Warthin, 1942). 

Previous \\:'ork on Rugose Corals 

Fraunfelter (1970) described numerous silicified corals 

from the outcropping Lingle Limestone in southwestern Illinois and reviewed previous work on the corals (1970, p. 7-

10). Fraunfelter noted that only one coral species had previously been described from the Lingle (Microcyclus discus 

Meek and Warthin, a pre-Centerfield species from the 

lower Lingle or St. Laurent Limestone) although numerous 

faunal lists had included corals. Fraunfelter seems to have 

used "Lingle" in the same restricted sense as Cooper; he 

assigned the lower, Skaneateles-age beds to the St. Laurent 

Limestone. In his columnar section (Fraunfelter, 1970, fig. 

2), collections a-f seem to be St. Laurent and g-n, Lingle. 

On this basis, the rugose corals that Fraunfelter described 

from the Centerfield-age "Lingle" are listed in table 2, for 

comparison with the corals in the Coles County core. Comparison of Fraunfelter' s corals with those from Coles 

County is difficult because Fraunfelter's specimens were 

silicified and separated from the limestone matrix, whereas 

the new faunule is calcitic and known from thin sections 

only. 

Table 2. Rugose corals identified and described from the outcropping "Lingle" Limestone by Fraunfelter, 1970 

[Collections are from southwestern Illinois and adjacent Mi~souri] 

Amplexiphyllum pauciseptum Fraunfelter 

Bethanyphyllum robustum (Hall) 

Billingsastraea ingens (Davis) 

Craterophyllum brevicyathum Fraunfelter 

Cystiphylloides americanum (E. and H.) 

Eridophyllum archiaci (Billings) 

Heliophyllum confluens Hall 

H. gurleyi Greene 

H. halli E. and H. 

Heterophrentis simplex (Hall) 

Hexagonaria percarinata (Sloss) 

Iowaphyllum alpenense (Rominger) 

I.? sp. 

Odontophyllum cornutiformis Fraunfelter 

Tabulophyllum variformis Fraunfelter 

New Faunule 

Rugose corals from the 3,121-3,125-foot interval in the 

Coles County core are listed in table 3 and briefly annotated 

in the following paragraphs. All specimens are from the 

collections of the Illinois State Geological Survey (ISGS), 

Champaign, and are numbered in their collections, as indicated. 

Siphonophrentis sp. aff. S. halli (E. and H.) (pl. 1, figs. 5-7) 

The Coles County specimen has relatively short, amplexoid septa that suggest Siphonophrentis (or Breviphrentis) 

rather than the closely related Heterophrentis. The tabulae 

are more widely spaced than in New York specimens of S. 

halli (see Hall, 1877, pl. 20, fig. 8), but in this and other 

characters the specimen falls well within the range of variation in this species accepted by Stumm, 1965 (pl. 14) for 

Beechwood specimens. This may be Heterophrentis simplex 

ofFraunfelter (1970, p. 13, pl. 1, fig. 4). The Coles County 

specimen is ISGS 72P-13A, from 3,123 feet. 

Tabulophyllum sp. d. T. conatum (Hall) (pl. 1, figs. 13-15) 

Four specimens, none complete, are assigned to Tabulophyllum. Two of these are closest to T. conatum (Hall, 

1877, pl. 31, fig. 2, 5, 6, 11-13, other figs. uncertain) from 

the New York Centerfield in having abbreviated minor septa 

and more-or-less uniform majors. Most characteristic is 

ISGS 72P-17 (3, 123 feet) with moderately attenuate septa 

but ISGS 72P-1 (3,121 feet) is probably the same species. 

T. variformis Fraunfelter from the outcropping "Lingle," is 

similar to T. conatum, differing mainly in its larger size. 

T. sp. d. T. zaphrentiforme (Davis) (pl. 1, figs. 8-12) 

Stumm (1965, p. 50, pl. 45, figs. 10-13) redescribed 

Middle Devonian Coral Faunules, Illinois 03 
Table 3. Corals (and one stromatoporoid) identified from 

Herkimer No. 5 well, Coles County, Illinois 

[Realm affinities indicated to right: EAR, Eastern Americas Realm; OWR, 

Old World Realm; MB, Michigan Basin] 

Lingle Limestone, upper part 

Siphonophrentis sp. aff. S. halli (E. and H.) 

Tabulophyllum sp. cf. T. conatum (Hall) 

T. sp. cf. T. zaphrentiforme (Davis) 

Heliophyllum sp. cf. H. halli E. and H. 

Bethanyphyllum sp. aff. B. robustum (Hall) 

Prismatophyllum arachnoideum (Stumm) 

Eridophyllum sp. cf. E. archiaci (Billings) 

E. n. sp. A 

Acanthophyllum sp. 

Ptenophyllid coral, genus and species undetermined 

Grand Tower Limestone, "Anderdon" beds 

Amphipora nattressi (Grabau) 

Grypophyllum n. sp. A 

Holmophyllia n. sp. A 

EAR 

EAR 

EAR 

EAR 

EAR 

EAR 

EAR 

EAR 

OWR 

OWR 

MB 

OWR 

OWR 

this species as having an enlarged and long counter septum, 

but illustrated it only with exterior views of silicified specimens. New York Centerfield Tabulophyllum specimens are 

divisible into two species. Typical T. conatum Hall (see 

above) have more-or-less uniform septa although a cardinal 

fossula is commonly developed. A second species has a 

more prominent fossula and a long and enlarged counter 

septum and is tentatively referred to T. zaphrentiforme 

Davis (although T.? gradatum Hall, 1877, pl. 31, figs. 

15-16, may be conspecific and, if so, has priority). The two 

New York species are distinct in other characters also. 

Davis' and Stumm's specimens are from the Beechwood 

and equivalent units in Kentucky and southern Indiana. The 

most characteristic Coles County specimen is ISGS 72P-3 

(3, 121 feet); ISGS 72P-21 (3, 125 feet) is tentatively referred to this species also. 

Heliophyllum sp. d. H. halliE. and H. 

One fragment of a calice rim shows the characteristic 

long, cross-bar carinae of Heliophyllum and is probably this 

species. Fraunfelter listed H. halli from the "Lingle," but it 

is not clear whether his illustrated specimens are from the 

"Lingle" or St. Laurent. ISGS 72P-15; 3,123 feet. 

Bethanyphyllum sp. aff. B. robustum (Hall) (pl. 2, figs. 1-6) 

New York Centerfield specimens have abundant vepreculae on the sides of septa at all stages of growth (Hill, 1981, 

p. F305-306, figs. 199-1a-d). Specimen ISGS 72P-10 is 

very like Centerfield specimens in other respects but vepreculae are common only in early stages where septa are dilated; mature septa have fewer vepreculae. Fraunfelter cited 

B. robustum from the "Lingle" (1970, p. 20, pl. 2, fig. 14) 

but his identification is uncertain because the significance of 

04 Shorter Contributions to Paleontology and Stratigraphy 

the vepreculae had not been noted when he did his work. 

Identification of this form is based on ISGS 72P-10 (from 

3,122 feet) but a second, less complete, specimen (ISGS 

72P-19; 3,124 feet) is probably the same species. 

Prismatophyllum arachnoideum (Stumm) (pl. 3) 

Cerioid craspedophyllids with an aulos are uncommon 

(Oliver, 1981), only two species having been described 

(Stumm, 1954; Oliver, 1976, p. 108, 1981). Coles County 

specimens are referable toP. arachnoideum (Stumm, 1954, 

p. 6, pl. 2, figs. 1-2), from the Stone Mill Limestone 

(=Centerfield) in New York. The only other known occurrence of the species is in the Joshua Submember of the 

Otisco Shale Member of the Ludlowville Formation (which 

overlies the Centerfield in central New York). Coles County 

specimens have the small aulos (missing in some corallites) 

and other characters of the species. Two specimens, ISGS 

72P-18 and 72P-20, are both from 3,124 feet; a third specimen (ISGS 72P-22B) is "probably from this core" (ISGS 

label). 

Eridophyllum sp. d. f. archiaci (Billings) (pl. 1, fig. 1-4} 

Two cylindrical fragments are similar to forms illustrated 

by Ehlers and Stumm (1949, p. 29, pl. 4, figs. 3-7; pl. 8, 

figs. 1-6) from the Hungry Hollow Formation, Ontario, and 

the Four Mile Dam Formation, Michigan. The species has 

also been described from the "Lingle" Limestone in southwestern Illinois (Fraunfelter, 1970, p. 22), the Beechwood 

Limestone Member in Kentucky-Indiana (Stumm, 1965, 

p. 45), the Tenmile Creek Dolomite in northwestern Ohio 

(Stumm, 1968, p. 41), and is known from the Centerfield 

Limestone Member of New York. All these units are Centerfield in age. Coles County specimens are ISGS 72P-8A 

and 72P-12 (both 3,122 feet); 2 or 3 crushed corallites at 

3,121 feet (ISGS 72P-5) may be the same species. 

Eridophyllum new species A (pl. 4) 

Numerous cylindrical corallites of a typical Eridophyllum 

are in the Coles County core at 3,122 and 3,123 feet. Corallites range from 2.3 to 5.4 mm in diameter (commonly 

2.5-4.0 mm) with 12-21 major septa (commonly 14-17). 

The aulos occupies approximately a quarter the diameter 

and is open in the direction (assumed) of the cardinal septum. All specimens are discrete and no connections between 

individuals have been noted, but the species is most likely 

phaceloid. Except for its small size, this is a fairly typical 

Eastern Americas Realm Eridophyllum. Other known Eridophyllum species have significantly larger diameters (1-2 

em) and it seems likely that the Coles County specimens 

represent an undescribed species. 

Two clusters are known (ISGS 72P-14, 12 or more corallites, and 72P-13B, 15 or more corallites) both from 3123 

feet. Additional single corallites are: from 3122 feet, ISGS 
72P-7B, 72P-9, 72P-11; from 3,123 feet, ISGS 72P-15, 

72P-16. In addition, a single corallite was found in the 

DuncanNo. 7Taylorwell(ColesCounty, sec.ll, T.l2N. 

R. 7 E.) at 3, 150 feet. 

Acanthophyllum sp. (pl. 2, figs. 11-12) 

Specimen ISGS 72P-4 (3,121 feet) is incomplete but has 

the characteristic tabularium, thin wall, and microstructure 

of Acanthophyllum, a common Old World genus not otherwise reported from the Devonian of the Eastern Americas 

Realm. A second specimen (ISGS 72P-8B, 3,122 feet) has 

a somewhat wider tabularium but is probably conspecific. 

Ptenophyllid coral, genus and species not determined (pl. 2, 

figs.7-10) 

A single specimen (ISGS 72P-7 A, 3,122 feet) has the 

characteristic tabularium of Acanthophyllum and other 

ptenophyllids. The specimen is unusual in having prominent 

spines on the sides of the septa in both the dissepimentarium 

and tabularium. In other respects, the specimen is similar to 

Acanthophyllum and it may be conspecific with ISGS 72P4, and 72P-8B. 

"ANDERDON" CORALS 

Stratigraphy 

During drilling of the Herkimer No. 5 well, a cavity was 

struck at 3,167 feet. At this point, the drill stem and bit 

dropped 5 feet and drilling was stopped so that the rocks 

beneath the cavity were not sampled. At 3,167 feet, the drill 

had penetrated 50 feet of limestone below the New Albany 

Shale Group (Cluff, Reinbold, and Lineback, 1981) (table 

1). This is the approximate thickness of the Lingle Limestone in the area (North, 1969, figs. 13, 16). Given this, the 

5-foot cavity was close to the contact between the Lingle 

Limestone and the underlying Grand Tower Limestone and 

could be in the basal Lingle, uppermost Grand Tower or 

both. However, fossils bailed from the cavity are of Grand 

Tower age (Linsley and Kesling, 1982, and this paper), so 

the cavity interval is assumed to be in the uppermost Grand 

Tower (table 1). It seems logical to suggest that cave formation took place beneath an unconformity separating the Lingle and Grand Tower Limestones. 

Fossils bailed from the cave were listed by Linsley and 

Kesling (1982, p. 1079) as "a multitude of broken fragments 

of twiglike stromatoporoids, hundreds of steinkerns of ostracodes ... , numerous gastropods, several bivalves, and a 

few solitary corals." Brachiopods and charophytes were also 

mentioned. The gastropods and ostracodes were described 

by Linsley and Kesling ( 1982) and the fauna was recognized 

as that of the Michigan Basin Anderdon Limestone (upper 

Detroit River Group). The exact age of the Anderdon is in 

dispute but, in general terms, it would be Onondaga, rather 

than Hamilton. Therefore, Linsley and Kesling's suggestion 

that the cavity fauna is from the upper Grand Tower is very 

reasonable. It is here referred to as the "Anderdon" fauna 

because of its exotic nature and importance. 

New Coral Faunule 

The collections of the ISGS include some 20 rugose 

corals. Of these, 11 were considered suitable for thin sectioning and are identified as two species (table 2); others are 

incomplete or fragmental but most of these clearly belong to 

one of the sectioned species. The two species are annotated 

below. 

Accompanying the rugose corals are hundreds of small 

fragments of "twig like stromatoporoids." Only a few of 

these have been studied but all may belong to a single 

species of Amphipora , also annotated below. The driller's 

log refers to "gallons of corals"; very possibly the "corals" 

are Amphipora fragments rather than rugose corals as might 

otherwise have been expected. Correspondence in the ISGS 

files regarding the bailed collection indicate that there were 

only a few corals in the original collection when received. 

Amphipora nattressi (Grabau) 

This stromatoporoid was redescribed and illustrated by 

Galloway and Ehlers (1960, p. 99-101, pl. 11), from the 

Anderdon Limestone of the "Anderdon Quarry," near 

Amherstburg, Ontario. The "multitude of broken fragments 

of twiglike stromatoporoids" noted by Linsley and Kesling 

are mostly or entirely this species. Possibly, the "gallons of 

corals" referred to by the driller were these fragments of 

ramose stromatoporoids rather than rugose corals. 

Grypophyllum n. sp. A (pl. 5) 

This is a typical ptenophyllid, but not a typical Grypophyllum, although it seems to fit more comfortably in that 

genus here than in other described genera. The transverse 

section is characteristic except that spines are variably developed on the sides of the septa within the dissepimentarium, and minor septa are well developed and complete. In 

longitudinal section, the dissepiments are large, irregular, 

unequal, and steeply inclined; the tabularium is ptenophylloid. In these characters, the longitudinal section resembles 

the N eomphyma illustrated by Hill (1981 , p. F239, fig. 

150-la). 

Grypophyllum n. sp. A differs from described species of 

the genus in the characters indicated. G. gracile Wedekind 

has very large, inclined dissepiments but they are not irregular. G. n. sp. A differs from the ptenophyllids in the Lingle 

faunule in having a well-developed, thick outer wall, and in 

the longitudinal characters noted. The presence of spines on 

the sides of the septa appears to be coincidental , as they are 

quite different in detail. 

Middle Devonian Coral Faunules, Illinois 05 
Grypophyllym is widespread in rocks of Middle Devonian 

(Eifelian and Givetian) age in the Old World Realm, although, at present, it is known only from the Givetian of 

western North America (A.E.H. Pedder, oral communication, May 1985). It also occurs in the Early Devonian (Emsian) of the Urals (Pedder and Oliver, 1979, table 1). 

In eastern North America, only one occurrence is known 

in addition to the one described here. Grypophyllum sp. cf. 

G. denckmani is known from the topmost part of the Cedar 

Valley Limestone at Marble Rock, Iowa (J.E. Sorauf, oral 

communication, May 3, 1985). 

Eight specimens of G. n. sp. A are known; four were thin 

sectioned (ISGS 72P-23 to 72P-26) but four additional 

fragments are con specific. 

Holmophyllia n. sp. A (pl. 6) 

This genus is characterized by having septa composed of 

trabeculae that are partly discrete and partly fused to form 

continuous units. Hill (1981, p. F105) synomized Holmophyllia with H olmophyllum . The latter is characterized by 

discrete spines that pierce several layers of dissepiments or 

trabeculae. I agree with McLean (1975, p. 185-186) that 

the morphologic difference seems important enough to justify recognition of both genera. McLean noted a generic 

range for Holmophyllia of Middle? and Upper Silurian to 

Lower Devonian, but Hill illustrated an Eifelian species 

from the Urals (1981 , p. F 104, fig. 46-lf, g) that seems 

closer to Holmophyllia than Holmophyllum. 

Typical Holmophyllum s.s. have been described from 

Upper Silurian rocks of Maine (Stumm, 1963), Quebec 

(Oliver, 1963), and western Canada (Pedder, 1978) but no 

H olmophyllia , or Devonian forms of either genus, have 

previously been described from North America. 

Six sectioned specimens are assigned to Holmophyllia n. 

sp. A (ISGS 72P-27 to 72P-32); sectioned specimen 72P33 and two to eight additional fragments are probably the 

same species. 

BIOGEOGRAPHY 

Introduction 

The Middle Devonian world is divisible into three biogeographic realms: 1) The Eastern Americas Realm (EAR) 

was relatively small, consisting of northern South America 

and eastern North America (ENA; east of the Transcontinental Arch and south of the Canadian Shield). 2) The Old 

World Realm (OWR) included western and Arctic North 

America, Eurasia, northern Africa, and Australia. 3) The 

Malvinokaffric Realm included central and southern South 

America and Africa, and Antarctica. Both the EAR and 

OWR had rich and varied rugose coral faunas that were 

significantly different from each other on the generic level 

(Oliver, 1977). The Malvinokaffric was a high-latitude area 

D6 Shorter Contributions to Paleontology and Stratigraphy 

containing no significant coral faunas (Oliver, 1980). 

The EAR is considered to have been a single biogeographic province (Appohimchi) during the Eifelian but is 

divided into the Michigan Basin-Hudson Bay Lowland 

Province and the Appohimchi Province during the Givetian 

(Oliver, 1977, p. 107-114; Oliver and Pedder, 1979, 

p. 135-13 7). The southern boundary of the Michigan Basin 

Province is the Kankakee Arch (fig. 1) and the Illinois Basin 

is part of the Appohimchi Province. In contrast to these two 

EAR provinces, nine or more provinces can be recognized 

at various times in the much larger Old World Realm (Oliver 

and Pedder, 1984). 

The basis for recognizing two separate EAR provinces in 

the Givetian is the presence in the Michigan Basin-Hudson 

Bay Lowland area of Old World genera that are not known 

farther east or south in the Appohimchi Province. Oliver 

(1977, p. 114) suggested that the Old World forms must 

have emigrated from the west or north and most likely from 

the Williston Basin. A few genera were apparently introduced earlier. Old World Dendrostella is locally common in 

Eifelian rocks (Detroit River Group) on the eastern margin 

of the Michigan Basin, and Disphyllum s.s. is known from 

the Dundee Limestone (upper Eifelian) within the Basin. 

The latter also occurs in rocks of the same age (Famine 

Limestone, Quebec) in the Appohimchi Province where it 

is the only Old World genus known to have migrated this 

far; it also presumably entered by way of the Michigan 

Basin (Oliver, 1977, p. 114). 

The Coles County faunules are of interest because, in this 

small area, a Michigan Basin/Old World fauna was followed in later time by a dominantly EAR fauna. A similar 

superposition of Old World and Eastern Americas faunas is 

known near Logansport, Ind. The relationship of the two 

faunas in the Michigan Basin as a whole requires further 

study. 

Lingle Faunule 

The Lingle rugose corals from Coles County (table 3) are 

predominantly genera and species that are common in the 

Appohimchi Province in rocks of Centerfield age; several 

belong to EAR endemic genera. There are two exceptions; 

bothAcanthophyllum sp. and the undetermined ptenophyllid 

are Old World corals and exotic in central Illinois. 

The distribution of ptenophyllids (Family Ptenophyllidae) 

in eastern North America is shown in table 4. Several 

species in four genera are common in latest Silurian (Pridolian) rocks of the central and northern Appalachians. Two 

of the genera survived into the Lochkovian but then the 

family seems to have become extinct in the EAR, because 

no ptenophyllids have been recognized in the reasonably 

well-known coral faunas of Emsian to Eifelian age (except 

as noted herein). Middle Devonian ptenophyllids are rare 

and, except for Coles County, Ill. , limited to the Michigan 

Basin. 
Table 4. Ptenophyllids in the Eastern Americas Realm (EAR) 

[Stages from left to right: Pri, Pridolian; L, Lochkovian; Pra, Pragian; Em, Emsian; Ei, Eifelian; G, Givetian. Occurrences: A, Appalachian Basin; I, Illinois 

Basin; M, Michigan Basin] 

Stage 

Genera Pri L Pra 

Acanthophyllum A 

Entelophylloides A 

Embolophyllum A A 

Spongophylloides A A 

Grypophyllum 

G. cf. denckmanni 

Australophyllum 

Ptenophyllid undet. 

"Anderdon" Faunule 

The two "Anderdon" corals from Coles County are not 

known to occur elsewhere in the Devonian EAR. Grypophyllum is an Old World ptenophyllid genus (table 4) that is 

assumed to have reached Illinois after migrating into the 

Michigan Basin from the west. Holmophyllia is not otherwise known to occur in Devonian rocks in North America, 

but the genus may occur in the Eifelian of the Urals and is 

known from the Lower Devonian of other Old World areas. 

The associated gastropods are a Michigan Basin assemblage (Linsley and Kesling, 1982) and are largely endemic 

(Linsley, 1968). Most of the gastropods were described by 

Linsley (1968) from the Anderdon Limestone in southeastem Michigan (south of Detroit) and in adjacent parts of 

Ontario and Ohio. In this area, many of the gastropods are 

associated with Amphipora nattressi (Grabau) and other 

stromatoporoids in biostromes. The Illinois occurrence may 

have been in a similar bed. 

Logansport, Indiana 

The Logansport area is on the Kankakee Arch that separates the Illinois and Michigan Basins, some 225 km northeast of Coles County (fig. 1, loc. 2). In this area, the Miami 

Bend Limestone of Cooper and Phelan ( 1966) is immediately overlain by the Logansport Limestone (see Cooper and 

Phelan for a detailed description of the stratigraphy). The 

Logansport Limestone was recognized as Centerfield in age 

by Cooper and Warthin (1942) and contains numerous 

corals, most of which are EAR endemics. The coral fauna 

is basically that of the Centerfield (New York) and Beechwood (Kentucky) as discussed in connection with the Lingle 

corals. 

In contrast, the Miami Bend Limestone contains an Old 

World fauna that is closely related to that of the Rogers City 

Limestone of Michigan and the Winnipegosis Formation of 

Manitoba (Cooper and Phelan, 1966; see Oliver, 1977, 

p. 112-114, for discussion of the coral fauna). The Miami 

Bend and Rogers City are early Givetian in age and provide 

Middle Devonian 

Em Ei G occurrence in EAR 

Lingle Limestone, Ill. 

"Anderdon" faunule, Ill. 

M Cedar Valley Limestone, Iowa 

M Miami Bend Limestone, Ind. 

Lingle Limestone, Ill. 

the closest and most direct tie of a Michigan Basin Old 

World fauna to the Old World Realm Williston Basin. An 

updated list of Miami Bend rugose corals (table 5) includes 

three EAR species, six OWR species and one new form. 

None of the OWR forms is known from the Appohimchi 

Province. Winnipegosis corals have not been described or 

illustrated, so direct comparison is not feasible. However, 

the OWR Miami Bend genera are all known from western 

or Arctic Canada with the possible exception of cf. Chlamydophyllum. Australophyllum is a ptenophyllid and is listed 

on table 4 for completeness. 

Table 5. Corals from the Miami Bend Limestone (of Cooper 

and Phalen, 1966) 

[Realm affinities indicated to right: EAR, Eastern Americas Realm; OWR, 

Old World Realm] 

Heterophrentis sp. 

Heliophyllum halli E. and H. 

Bethanyphyllum sp. cf. B. robustum (Hall) 

Chostophyllum sp. 

H exagonaria borealis Stumm 

cf. Chlamydophyllum sp. 

Australophyllum sp. 

Stringophyllum? sp. 

Lekanophyllum sp. 

New genus, new species 

Michigan Basin 

EAR 

EAR 

EAR 

OWR 

OWR 

OWR 

OWR 

OWR 

OWR 

Endemic? 

Coral faunas in the Michigan Basin Traverse Group are a 

mixture of EAR endemics, Old World genera, and cosmopolitan forms with the EAR forms predominating (Oliver, 

1977, p. 114). Many of the Traverse rugose corals have 

been described, but it is not clear whether the Old World 

genera tend to be stratigraphically isolated, as in Coles 

County and the Logansport area, or whether they were 

living in association with EAR corals. This is a major biogeographic question that has yet to be answered. 

Middle Devonian Coral Faunules, Illinois 07 
Discussion 

Oliver (1977, p. 107-114) and Oliver and Pedder (1979, 

p. 135-138) have detailed and discussed the movement of 

Old World rugose corals into the Michigan Basin during 

Eifelian and Givetian times. Only a few forms are known to 

have moved out of the Basin into other parts of the EAR. 

The Coles County corals discussed in this paper are the first 

Old World genera recorded from the Middle Devonian 

within the Illinois Basin. 

SUMMARY AND CONCLUSIONS 

Two small coral faunules from a single well in Coles 

County, east-central Illinois, have contrasting compositions. The lower ("Anderdon") faunule is Eifelian in age and 

contains Old World corals in association with Michigan 

Basin gastropods and other invertebrates. The upper 

(Lingle) faunule is of Centerfield (Givetian) age and is dominated by typical Eastern Americas Realm genera, including 

two Old World forms. The two faunules supplement previous knowledge of Old World coral distributions within the 

Eastern Americas Realm and support earlier conclusions 

that the dilution of EAR faunas that began in Eifelian time 

was through migration into the Michigan Basin-Hudson 

Bay Lowlands area from the west, probably from the Williston Basin. Dilution was great enough during the Givetian to 

enable the subdivision of the Eastern Americas Realm into 

the Michigan Basin-Hudson Bay Lowlands Province and 

the Appohimchi Province. By the end of the Middle Devonian, all EAR endemic genera were extinct and Frasnian 

corals in the area are part of a cosmopolitan fauna. 

REFERENCES CITED 

Cluff, R.M., Reinbold, M.L., and Lineback, J.A., 1981, The 

New Albany Shale Group of Illinois: Illinois State Geological 

Survey Circular 518, 83 p. 

Collinson, Charles, and others, 1968, Devonian of the northcentral region, United States, in Oswald, D.H., ed., International symposium on the Devonian System, Calgary, 1967, 

Volume 1: Alberta Society of Petroleum Geologists, p. 933-

971. 

Cooper, G.A., and Phelan, Thomas, 1966, Stringocephalus in the 

Devonian of Indiana: Smithsonian Miscellaneous Collections, v. 151, no. 1, 20 p. 

Cooper, G.A., and Warthin, A.S., 1942, New Devonian (Hamilton) correlations: Geological Society of America Bulletin 53, 

no. 6, p. 873-888. 

Cooper, G.A., and others, 1942, Correlation of the Devonian 

sedimentary formation of North America: Geological Society 

of America Bulletin 53, p. 1729-1794. 

Ehlers, G.M., and Stumm, E.C., 1949, Corals of the Devonian 

Traverse Group of Michigan. Part II, Cylindrophyllum Depassophyllum, Disphyllum, Eridophyllum, and Synaptophyl08 Shorter Contributions to Paleontology and Stratigraphy 

fum: University of Michigan, Contributions from the Museum 

of Paleontology, v. 8, no. 3, p. 21-41. 

Fraunfelter, G.H., 1970, Silicified corals from the Lingle and St. 

Laurent limestones (Middle Devonian) of southern Illinois 

and southeastern Missouri: Southern Illinois Studies, Southem Illinois University, University Museum and Dept. of Geology, Research Records, No. 3, 41 p. 

Galloway, J.J., and Ehlers, G.M., 1960, Some Middle Devonian 

stromatoporoids from Michigan and southwestern Ontario, 

including the types described by Alexander Winchell and 

A. W. Grabau: University of Michigan, Contributions from 

the Museum of Paleontology, v. 15, no. 4, p. 39-120. 

Hall, James, 1877, Illustrations of Devonian fossils; corals of the 

Upper Helderberg and Hamilton Groups: Albany, New York 

Geological Survey, 39 plates and explanations. 

Hill, Dorothy, 1981, Part F, Coelenterata, Supplement 1, Rugosa 

and Tabulata. Treatise on Invertebrate Paleontology: Geological Society of America and Kansas University, 762 p. 

Linsley, R.M., 1968, Gastropods of the Middle Devonian Anderdon Limestone: Bulletins of American Paleontology, v. 54, 

no. 244, p. 333-465. 

Linsley, R.M., and Kesling, R. V., 1982, A Detroit River (Middle 

Devonian) fauna from the subsurface of Illinois: Journal of 

Paleontology, v. 56, p. 1079-1092. 

McLean, R.A., 1975, Silurian rugose corals from the Mumbil 

area, central New South Wales: Linnean Society of New 

South Wales, Proceedings, v. 99, p. 181-196. 

North, W. G., 1969, The Middle Devonian strata of southern Illinois: Illinois State Geological Survey Circular 441, 45 p. 

Oliver, W.A., Jr., 1963, Silurian rugose corals from the Lake 

Temiscouata area, Quebec: U.S. Geological Survey Professional Paper 430-B, p. 11-19. 

---1976, Noncystimorph colonial rugose corals of the Onesquethaw and lower Cazenovia stages (Lower and Middle Devonian) in New York and adjacent areas: U.S. Geological 

Survey Professional Paper 876, 156 p., 108 pls. 

---1977, Biogeography of Late Silurian and Devonian rugose 

corals: Palaeogeography, Palaeoclimatology, Palaeoecology, 

v. 22, p. 85-135. 

---1980, Corals in the Malvinokaffric Realm: Munster. 

Forsch. Geol. Palaont., No. 52, p. 13-27. 

---1981, The Middle Devonian rugose coral Prismatophyllum 

conjunctum (Davis) and the age of the "Columbus" Limestone 

at Ingersoll, Ontario: Geological Society of America Bulletin 

92, p. 873-877. 

Oliver, W.A., Jr., and Pedder, A.E.H., 1979, Biogeography of 

Late Silurian and Devonian rugose corals in North America, 

in Gray, Jane, and Boucot, A.J., Historical biogeography, 

plate tectonics, and the changing environment: Corvallis, Oregon State University Press, p. 131-145. 

---1984, Devonian rugose coral biostratigraphy with special 

reference to the Lower-Middle Devonian boundary: Canada 

Geological Survey Paper 84-1A, p. 449-452. 

Pedder, A.E.H., 1978, Corals, in Jackson, D.E., Lenz, A. C. and 

Pedder, A.E.H., Late Silurian and Early Devonian graptolite, 

brachiopod and coral faunas from northwestern and Arctic 

Canada: Geological Association of Canada Special Paper 17, 

p. 31-49. 
Pedder, A.E.H., and Oliver, W.A., Jr., 1979, Rugose corals in 

Devonian stratigraphical correlation: Palaeontological Association, Special Paper in Palaeontology, v. 23, p. 233-248. 

Stumm, E.C., 1954, Four new species of rugose corals of the 

Middle Devonian genus Eridophyllum, from New York, 

Michigan, and Ohio: University of Michigan, Contributions 

from the Museum of Paleontology, v. 12, no. 1, p. 1-11. 

---1963, Silurian corals from the Moose River synclinorium, 

Maine: U.S. Geological Survey Professional Paper 430-A, 

p. 1-9. 

---1965, Silurian and Devonian corals of the falls of the Ohio: 

Geological Society of America Memoir 93, 184 p. 

---1968, The corals of the Middle Devonian Tenmile Creek 

Dolomite of northwestern Ohio: University of Michigan, 

Contributions from the Museum of Paleontology, v. 22, 

no. 3, p. 37-44. 

Willman, H.B., and others, 1975, Handbook of Illinois stratigraphy: Illinois State Geological Survey Bulletin 95, 261 p. 

Middle Devonian Coral Faunules, Illinois D9 

PLATES 1-6 

Contact photographs of the plates in this report are available at cost from U.S. Geological 

Survey Library, Federal Center, Denver, CO 80225 
PLATE 1 

Corals from the Lingle Limestone 

[Transverse and longitudinal thin sections] 

Figures 1-4. Eridophyllum sp. cf. E. archiaci (Billings), all X5. 1,2, ISGS 72P-12; 3,4, ISGS 72P-8. 

5-7. Siphonophrentis sp.aff. S. halli (E. and H.). ISGS 72P-13; 5,6, X 1.5; 7, X2.5, detail of fig. 6. 

8-12. Tabulophyllum sp. cf. T. zaphrentiforme (Davis). 8-10, ISGS 72P-3, X5. 11-12, ISGS 72P-21, X2.5. 

13-15. Tabulophyllum sp. cf. T. conatum (Hall). 13, ISGS 72P-17, X2.5; 14,15, ISGS 72P-1, X5. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

11 12 

8 

BULLETIN 1690- D PLATE 1 

4 

CORALS FROM THE LINGLE LIMESTONE 
PLATE 2 

Corals from the Lingle Limestone 

[Transverse and longitudinal thin sections] 

Figures 1-6. Bethanyphyllum sp. aff. B. robustum (Hall). ISGS 72P-10. 1-3, X2.5; 4-6, x 10. Figs. 4, 5, and 6 are details of sections in figs. I, 2, 

and 3, respectively. 

7-10. Ptenophylloid coral, genus and species not determined . ISGS 72P-7A. 7, longitudinal section , X2.5. 8, tabularium of same, xs. 9, 

transverse section, X2.5 . 10, detail of same showing septal spines, x 10. 

ll-12. Acanthophyllum sp. ISGS 72P-4; X5 and X2.5. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

5 

BULLETIN 1690--D PLATE 2 

6 

CORALS FROM THE LINGLE LIMESTONE 
PLATE 3 

Corals from the Lingle Limestone 

[Transverse and longitudinal thin sections] 

Figures 1-7. Prismatophyllum arachnoideum (Stumm). 1, 2, ISGS 72P-20, Xl.5, X2.5; 3, 4, ISGS 72P-22B, X2.5; 5-7, ISGS 72P- 18, X2.5, X5. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

CORALS FROM THE LINGLE LIMESTONE 

BULLETIN 1690-D PLATE 3 
PLATE 4 

Corals from the Lingle Limestone 

[Transverse and longitudinal thin sections] 

Figures 1-13. Eridophyllum n. sp. A. 1-5, ISGS 72P-14; 1-3, x5; 4-5, x 10. 6-13, ISGS 72P-13B, all x 10. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

2 

5 

7 8 

11 

13 

10 

CORALS FROM THE LINGLE LIMESTONE 

BULLETIN 1690---D PLATE 4 
PLATE 5 

"Anderdon" Corals 

[Transverse and longitudinal thin sections] 

Figures 1-11. Grypophyllum n. sp. A. All xs. 1, 2, ISGS 72P-23. 3-5, ISGS 72P- 24. 6, 7, ISGS 72P- 25. 8- 11, ISGS 72P-26. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

"ANDERDON" CORALS 

BULLETIN 1690--D PLATE 5 

5 
Plate 6 

"Anderdon" Corals 

[Transverse and longitudinal thin sections] 

Figures 1-11. Holmophyllia n. sp. A. All X5. 1-3, ISGS 72P-27. 4-6, ISGS 72P-28. 7, 8, ISGS 72P-29. 9-11, ISGS 72P-30. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

"ANDERDON" CORALS 

BULLETIN 1690-D PLATE 6 

CHAPTER E 

Paleobathymetric Significance of Ostracodes 

from the Paine Member of the Lodgepole 

Limestone (Early Mississippian), Northeast Utah 

By I.G. Sohn and William J. Sando 

U.S. GEOLOGICAL SURVEY BULLETIN 1690 

Shorter Contributions to Paleontology and Stratigraphy 

CONTENTS 

Abstract El 

Introduction El 

Acknowledgments El 

Environment of deposition inferred from other evidence El 

Evidence from the orientation and epibiont relationships of dissociated valves E2 

Evidence from inferred paleoecology of Paleozoic marine ostracodes E3 

Paleoecologic conclusions E3 

Systematic paleontology E4 

Superfamily Paraparchitacea Scott, 1959 E4 

Family Paraparchitidae Scott, 1959 E4 

Genus Chamishaella Sohn, 1971 E4 

C. lodgepoleana Sohn n. sp. ES 

References cited E6 

PLATES 

[Plates follow References Cited) 

1. Chamishaella lodgepoleana 

2. Chamishaella lodgepoleana 

TABLES 

1. Stratigraphic positions of ostracodes from the Paine Member of the Lodgepole 

Limestone at Brazer Canyon E2 

2. Measurements (in mm) of illustrated and selected specimens E4 

3. Recorded size (in mm), age, and geographic occurrences of species of 

Chamishaella ES 

Contents iii 

Paleobathymetric Significance of Ostracodes from 

the Paine Member of the Lodgepole Limestone 

(Early Mississippian), Northeast Utah 

By I.G. Sohn and William j. Sando 

Abstract 

Silicified ostracodes recovered from the Paine Member of 

the Lodgepole Limestone at Brazer Canyon, northeast Utah, 

form the basis for the first description of these fossils from the 

Lodgepole Limestone. The faunule represents a new species, 

Chamishael/a /odgepo/eana Sohn, which appears to have been 

transported from shallow water into the deep-water environment of the Paine Member. 

INTRODUCTION 

Although ostracodes have been collected previously from 

the Lodgepole Limestone, that material was too sparse and 

too poorly preserved for description and detailed taxonomic 

analysis. Discovery of abundant, well-preserved silicified 

ostracode carapaces and dissociated valves in insoluble 

residues of 18 limestone samples from the Paine Member of 

the Lodgepole at Brazer Canyon, northeast Utah, provided 

an opportunity to gain some new insights into the nature and 

significance of these fossils in the Lodgepole. 

The ostracodes were found in residues obtained by etching the limestone samples with dilute hydrochloric acid in 

order to recover silicified brachiopods, corals, and gastropods, which were visible in the field. Because recovery 

of ostracodes was not anticipated prior to etching, only the 

+ 16 mesh and larger residues were retained, and all of the 

limestone was processed before the ostracodes were discovered. Hence the samples do not permit evaluation of the 

younger growth stages of the species described nor possible 

other ostracode taxa of size smaller than about 0. 9 mm in 

diameter. Moreover, any unsilicified ostracodes were destroyed by the etching process. 

The described material is from the lower half of the Paine 

Member of the Lodgepole Limestone (0.6-37.8 m above 

the base) in a measured section at Brazer Canyon in 

NW1/4SE1/4 sec. 20, T. 11 N., R. 8 E., Randolph quadrangle (15 min.), Crawford Mountains, Rich County, Utah. 

This sequence was formerly called member 1 of the Lodgepole Limestone by Sando and others ( 1959, section 2 in 

figs. 2, 3, and 4) and was reinterpreted as Paine Member by 

Gutschick and others (1980, fig. 3, column 12). Detailed 

stratigraphic data on the collections are given in table 1. 

Samples from the Paine Member above USGS 16836-PC 

did not yield ostracodes. 

The ostracode faunule consists exclusively of large 

smooth forms described herein as a new species of 

Chamishaella Sohn, 1971. In addition to describing this 

new species, the purpose of this report is to assess its paleoecologic significance with respect to the bathymetric model 

for the Paine Member based on other criteria. 

Acknowledgments 

We thank the following colleagues: Drs. J. M. Berdan 

and J. T. Dutro, Jr., U.S. Geological Survey, made valuable suggestions that improved this paper. Dr. Kristan 

Fauchald, Smithsonian Institution, provided information on 

the encrusting worms. Dr. 0. L. Karklins, U.S. Geological 

Survey, identified the bryozoan fragment. The scanningelectron micrographs are by Mr. Walter M. Brown, Smithsonian Institution, and the prints are by Mr. 

H. E. Mochizuki, U.S. Geological Survey. 

ENVIRONMENT OF DEPOSITION INFERRED 

FROM OTHER EVIDENCE 

The Paine Member in the area studied constitutes the 

lower part of the Lodgepole Limestone and consists of thinbedded, dark-colored, cherty, silty micrite and biomicrite. 

Shelly benthos (corals, brachiopods, and gastropods), 

crinoidal columnals, bryozoan, and echinoid fragments are 

generally rare; conodonts, radiolarians and sponge spicules 

are common in this lithofacies. Benthonic calcareous algae 

are absent. 

Wilson (1969) proposed a "deeper-water" origin for the 

Paine Member based on analogy with other strata of known 

deep-water origin having similar faunas, sedimentary structures, and petrographic features. Smith (1972, 1977) postulated a "deep-water" origin for the Paine Member based on: 

"1) dominance of lime mud, 2) even horizontal lamination, 

Ostracodes, Paine Member of the Lodgepole Limestone, Utah E1 
Table 1. Stratigraphic positions of ostracode collections from 

the Paine Member of the Lodgepole Limestone at Brazer 

Canyon 

Meters (feet) above base 

USGS colin. no. of Lodgepole Limestone 

16801-PC 0.0-0.6 (0-2) 

16802-PC (float) Do 

16803-PC 0.6-1.2 (2-4) 

16804-PC (float) Do 

16805-PC 1.2-1.8 (4-6) 

16806-PC 1.8-2.4 (6-8) 

16808-PC 2.4-3.0 (8-10) 

16809-PC (float) Do 

16810-PC 3.0-3.6 (10-12) 

16816-PC 6.6-7.2 (22-24) 

16818-PC 7.8-8.4 (26-28) 

16825-PC 10.8-11.4 (38-40) 

16827-PC 12.0-12.6 (40-42) 

16829-PC 13.2-13.8 (44-46) 

16831-PC (float) 15.6 (52) 

16835-PC 33.5-34.8 (110-114) 

16836-PC 37.8 (123.9) 

3) large "intraformational truncation surfaces" that may represent submarine mass movements, 4) sparse, specialized 

fauna of delicate, but commonly unbroken, bryozoans and 

brachiopods, as well as articulated crinoids, 5) Zoophycus 

trace fossils, 6) position of the unit on an unstable shelf with 

a well-documented tectonic history, 7) overall stratigraphic 

and sedimentologic similarity to better documented deepwater carbonates, and 8) pronounced lack of shallow-water 

depositional features." (Smith, 1977, p. 194-195). According to Smith (1977), depositional relief on bioherms associated with the deep-water limestones of the Paine indicate 

water depths of 70-100 m. Similar conclusions about deepwater origin of the Paine Member were also reached by 

Cotter (1965) and Stone (1972). Sando (1980), using benthonic algae as a determinant of the euphotic zone, concluded that the depth of Paine deposition must have been 

more than 100 m below sea level, the effective lower limit 

of the euphotic zone in clear tropical seawater. 

E2 Shorter Contributions to Paleontology and Stratigraphy 

Thus, the evidence cited on the depositional environment 

of the Paine Member unanimously favors a deep-water 

origin at depths from 70 to more than 100 m below sea level 

on a slope offshore from the ancient shelf margin (Gutschick 

and others, 1980). We will now determine whether the 

ostracodes herein described conform to this paleoecologic 

model. 

EVIDENCE FROM THE ORIENTATION AND 

EPIBIONT RELATIONSHIPS OF DISSOCIATED 

VALVES 

The ostracodes in the Paine Member are smooth forms 

that occur as rare carapaces and mostly as dissociated valves 

(pls. 1 , 2). Some of the valves have attached worm tubes on 

the inside concave surfaces (pl. 1, figs. 17, 18; pl. 2, 

fig. 27); rare crinoid and bryozoa fragments were in the 

residues. Dr. Kristan Fauchald, Curator of Worms, Department of Invertebrate Zoology, Smithsonian Institution, examined the photograph illustrated in plate 2, figures 25-28, 

and identified the worm as a serpulid-like taxon. He stated 

that most serpulids attach themselves to the lower sides of 

rocks and shells for protection against predators, but they 

need to be able to project their tentacular crown into the 

water for both oxygen and food. The worm must have easy 

access to open water at all times, that is, not much sediment 

can be deposited inside the shell (written communication, 

Feb. 27, 1985). 

Dr. 0. L. Karklins identified a 3-mm fragment of a bryozoan from USGS colln. 16808-PC as belonging to an 

undeterminate genus in the family Rhomboporidae 

Simpson, 1894. Blake's (1981) review of the paleoecology 

of Bryozoa concluded that, like the serpulids, bryozoans are 

dependent on water current for food and oxygen, confirming 

a slow rate of sedimentation. 

Nineteen valves with worms on the inside (concave side) 

were recovered from collections 16802-PC (USNM 

401112), 16808-PC (USNM 401113), 16809-PC (USNM 

401143), and 16810-PC (USNM 401114), 13 of which are 

from coHn. 16809-PC, (pl. 1, fig. 18; pl. 2, fig. 27). The 

worm tubes are attached across the entire length and (or) 

breadth of the concave surface. Dr. Fauchald estimated that 

it would take 1 or 2 months for the worm to grow that long. 

This indicates that the valves had to be oriented with the 

convex side down in order for the worms to extend their 

tentacular crowns into the water, because if the valves were 

oriented with the concave side down, the worms could not 

have survived. Convex fossils are usually oriented with the 

concave side down for stability in the presence of currents 

(Adamczak, 1981, p. 1). The presence of 13 valves in one 

collection with worms on the concave side indicates the 

absence of wave or current action for at least a month in 

order for the worms to grow. It also suggests that the sedimentation rate was minimal or nonexistent for the same 
length of time. In addition, worm predators were rare or 

nonexistent during the time necessary to secrete a tube more 

than 1 mm long. 

Dissociated valves in the collections do not necessarily 

indicate a high-energy environment. Examination of living 

ostracode cultures in glass or plastic containers without a 

sediment substrate discloses random orientation of single 

valves. Some valves are convex side up and some are concave side up. The molted or dead carapaces are dissociated 

by bacteria and predator activities including possible cannibalism. Ostracodes have been observed feeding on dead 

carapaces and in dissociated valves, but it is not known 

whether they eat bacteria or the ostracode tissue. Whatley 

(1983, p. 55) cited an example from the English upper 

Oxfordian, where the ostracodes lived on a soft, muddy 

substrate and were periodically overwhelmed and entombed 

by sudden influxes of arenaceous and oolitic material, probably the result of storms. In the intervals between the 

catastrophic episodes, more than 95 percent of the juveniles 

were represented by disarticulated valves, whereas at the 

levels of more rapid sedimentation, between 75 percent and 

95 percent were articulated. Although Whatley referred to 

juveniles, the same phenomenon may be operative on 

adults. Dissociated valves are more abundant than carapaces 

in the collections from the Paine Member, and the range in 

size of the valves (table 2) indicates that more than one 

growth stage is represented. The presence of dissociated 

valves in the Paine Member of the Lodgepole Formation 

does not contradict a very slow rate of sedimentation inferred from other evidence. 

Thus, the evidence from epibiont relationships and the 

preservation of the ostracode specimens shows that the 

valves probably came to rest, after death of the animals, in 

an environment characterized by a slow rate of sedimentation below wave base. This fits the bathymetric model for 

the Paine based on other evidence. 

EVIDENCE FROM INFERRED PALEOECOLOGY 

OF PALEOZOIC MARINE OSTRACODES 

The paleoecology of Paleozoic marine ostracodes is based 

on the known habitats of closely related living forms, speculations on the functions of structural features of the carapace, known or inferred habitats of associated fossils, and 

interpretation of the environment based on the enclosing 

sediments (Benson, 1961, p. Q60). Unfortunately, there are 

no modem counterparts of the deep-water epicontinental 

Paleozoic ostracode assemblages. Moreover, the living 

marine ostracode assemblages do not contain morphotypes 

similar to the large, smooth forms found in Paleozoic rocks. 

Few attempts have been made to determine the bathymetry 

of Paleozoic marine ostracode morphotypes, and the depth 

ranges of individual genera are poorly documented. 

Becker ( 1971) proposed a model for the paleoecology of 

Middle Devonian ostracodes from the Eifel region that consisted of six biotopes ranging from shallow water less than 

50 min depth to a probable maximum of 100m. This model 

was later revised (Becker, 1981, 1982) to include a shallowwater biotope (shelf= Eifeler Okotyp) and a deep-water 

biotope (Becken = Thiiringer Okotyp). Large smooth ostracodes occur in Becker's Eifeler Okotype, which is characterized by water depths of 50 m or less. Becker's deep-water 

biotope is characterized by ornamented forms. 

Sohn (1979, p. 1250) postulated that Pseudoleperditia 

gerki Sohn, a large (as much as 4 mm), relatively smooth, 

calcareous ostracode from the Early Mississippian of Iowa, 

was a reef dweller that was washed into a backreef lagoon. 

Both Becker (1971) and Berdan (1984) considered the Leperditicopida (large smooth forms) to be lagoonal inhabitants. 

Bless (1983) presented a paleoecologic model that consists of four main depositional realms for Late Devonian and 

Carboniferous ostracodes in western Europe, North Africa, 

and southeast Canada. The large smooth forms are found in 

shallow offshore and nearshore environments. Chamishaella is found in the nearshore environment in the Namurian of Libya. According to Bless, the basinal environment is characterized by thin-shelled entomozoans, diverse 

bairdiaceans, and heavily ornamented spinose ostracodes. 

Sandberg and Gutschick ( 1980) listed ostracode genera in 

the foreslope facies of their model for the Deseret starved 

basin in the Osagean and Meramecian of Utah and adjacent 

States. The depositional relief of the foreslope was estimated at 100-200 m (Sandberg and Gutschick, 1980, p. 

139). The ostracodes in this facies are silicified, robust, 

commonly articulated, and of low diversity. The assemblage consists of both smooth forms (Paraparchites, Bairdia) and ornamented forms (Graphyadactyloides, Beyrichiopsis, Kirkbya, and Waylandella ). Only a few ostracode 

specimens were recovered from the deep basinal facies (at 

least 300 m deep). 

PALEOECOLOGIC CONCLUSIONS 

The weight of evidence from previous analyses of the 

paleoecology of marine Paleozoic large smooth ostracodes 

(Becker, 1971, 1981, 1982; Bless, 1983; Berdan, 1984; and 

Sohn, 1979) suggests that the living habitat of this morphotype was mainly or entirely in water depths of less than 

50 m. Deeper waters were characterized by highly ornamented pelagic forms. However, the discovery of large 

smooth forms associated with ornamented forms in the 

foreslope facies of the Deseret Limestone (Sandberg and 

Gutschick, 1980) at depths estimated as 100-200 m demonstrates that the shallow-water morphotype can be found in 

deep-water environments under some circumstances. These 

anomalous occurrences are best explained by transportation 

of the carapaces after death by water currents or turbidity 

currents from the shallow-water living habitat down the 

Ostracodes, Paine Member of the Lodgepole Limestone, Utah E3 
Table 2. Measurements (in mm) of illustrated and selected specimens 

[C, carapace; R, right valve; L, left valve] 

Specimen 

USNM 401101, pl. 2, fig. 1-4, C 

USNM 401103, pl. 2, figs. 9-11, R 

USNM 401102, pl. 2, figs. 5-8, C 

USNM 401109, unfig., R, USGS coHn. 16808-PC 

USNM 401106, pl. 2, figs. 21-24, R 

USNM 401104, pl. 2, figs. 12-15, C 

USNM 401105, pl. 2, figs. 16-20, C 

USNM 401100, pl. 1, figs. 18, 19, R 

USNM 401095, pl. 1, figs. 5-8, L 

USNM 401093, pl. 1, figs. 1, 2, R 

USNM 401094, pl. 1, figs. 3, 4, L 

USNM 401097, pl. 1, figs. 11, 12, R 

USNM 401096, pl. 1, figs. 9, 10, L 

USNM 401110, unfig., R, USGS coHn. 16810-PC 

USNM401107, pl. 2, figs. 25-28, L 

USNM 401099, pl. 1, fig. 17, L 

USNM 401111, unfig., C, USGS coHn. 16836-PC 

USNM 401098, pl. 1, figs. 13-16, C 

USNM 401108, unfig., C, USGS coHn. 16808-PC 

foreslope to their final resting place in the sediment. This 

interpretation is consistent with evidence from the relationship of worm tubes found on the dissociated valves, which 

indicates quiet aerobic water conditions at the time that the 

worms lived on the valves. 

The absence of ornamented, characteristically deep-water 

forms from the sample studied is probably the result of 

sample-preparation techniques. Sandberg and Gutschick' s 

(1980) samples were processed with acetic acid, and the fine 

fractions of the residue were retained. Hence, their ostracode samples contained both autochthonous deep-water 

forms and allochthonous shallow-water forms. Only Paraparchites would have been retained in our collections in the 

+ 16 mesh residue. Because the Brazer Canyon samples 

were processed with hydrochloric acid, and only the + 16 

mesh fraction was retained, any characteristically deepE4 Shorter Contributions to Paleontology and Stratigraphy 

Greatest length Greatest height 

1.40 0.94 

1.54 1.00 

1.94 1.44 

2.00 1.40 

2.42 1.42 

2.42 1.62 

2.50 1.52 

2.65 1.66 

2.70 1.82 

2.72 1.80 

2.76 1.78 

2.79 1.80 

2.80 1.80 

2.80 1.80 

2.80 1.90 

2.85 1.86 

2.90 1.90 

3.00 2.04 

3.30 2.10 

water forms may have been lost during sample processing. 

SYSTEMATIC PALEONTOLOGY 

Superfamily PARAPARCHITACEA Scott, 1959 

emend. Sohn, 1971 

Family PARAPARCHITIDAE Scott, 1959 

[See Sohn (1971, p. A5) for a discussion 

of the above classification.] 

Genus CHAMISHAELLA Sohn, 1971 

Chamishaella Sohn, 1971, U.S. Geol. Survey Prof. Paper 711-A, 

p. 11. 

Paraparchites Ulrich and Bassler, 1906 part. of authors. 

Type-species.-C. brosgei Sohn, 1971, U.S. Geol. Survey Prof. Paper 711-A, p. 12, pl. 6, figs. 1-32, early 

Meramecian, Brooks Range, Alaska. 
Discussion-Chamishaella was established for large, 

smooth, straightbacked, subovate ostracodes with the left 

valve overlapping the right along the free margins, and the 

right valve overreaching the left along the dorsum. Species 

in this genus are dimorphic in that the greatest width is along 

the venter in heteromorphs (presumed females) (pl. 1, 

figs. 1-16, 18, 19). The tecnomorphs (presumed males and 

growth stages) are widest at or near the midheight (pl. 1 , 

fig. 17?; pl. 2, figs. 1-28). The hinge structure of the genus 

has not been described previously, because dissociated 

valves were not available. The species described herein is 

based mostly on single valves that show the hinge structure 

to consist of a ridge in the overlapping valve which fits into 

a groove in the overreaching valve. 

Table 3 lists all the known species in Chamishaella, their 

recorded size, age, and geographic occurrence. Species 

smaller than approximately 1 mm in greatest length probably are either based on immature individuals, or are 

misidentified. 

Stratigraphic range. -Except for C. sparsa, which is 

recorded from the Moskovian (Westphalian), Mississippian 

and Lower Carboniferous (lower Toumaisian through lower 

Namurian). 

Chamishaella lodgepoleana Sohn, n. sp. 

Plate 1, figures 1-19; plate 2, figures 1-28 

Etymology of name. -For the Lodgepole Limestone of the 

Madison Group. 

Holotype .-Heteromorphic carapace, USNM 401098 

Paratypes. -USNM 401093-401097, 401099-401122 

Voucher specimens. -USNM 401123-401143 

Type locality. -Brazer Canyon, Randolph Quadrangle, 

Utah. 

Type level. -Paine Member of the Lodgepole Limestone, 

Upper Siphonodella crenulata Zone (coral zone IC). 

Diagnosis.-Chamishaella with elongated lateral outline, 

weak overreach of right valve along dorsum, and weak 

incised hinge margin. 

Description. -The greatest length is at or slightly above 

midheight, the greatest height is at approximately midlength, and the greatest width of heteromorphs is near the 

ventral margin; it is closer to midheight on tecnomorphs. 

The cardinal angles are obtuse. The dorsal portions of the 

end margins are straight to slightly convex and merge ventrally into the convex ventral margin. The anterior margin 

has a larger curvature than the posterior margin, and its 

greatest convexity is slightly lower than that of the posterior 

margin. Both end margins merge evenly into the convex 

ventral margin. The dimorphic swelling near the venter of 

heteromorphs overreaches and covers the contact margin 

(pl. 1, figs. 1, 4). The hinge consists of a ridge in the 

overlapping valve and a groove in the overreaching valve. 

Both valves have a narrow band near the end margins that 

marks the limit covered by the larger valve (pl. 1, figs. 1, 

12, 14, 15; pl. 2, figs. 5, 14, 15, 23). The dorsal outline is 

subelliptical, tapering more towards the anterior end (pl. 1, 

figs. 7, 11; pl. 2, figs. 6, 8, 14, 16, 23), and the greatest 

Table 3. Recorded size (in mm), age, and geographic occurrence of species of Chamishaella 

[*, measured on illustration] 

Species 

C. aenigmatica Sohn, 1971 .................... . 

C. auriculata (Prozner, 1951) Sohn, 1971 ........ . 

C. brosgei Sohn, 1971 ........................ . 

C. cf. brosgei Sohn, 1971. Bless and Massa, 1982* .. 

C. carbonaria (Hall, 1858) Sohn, 1972 .......... . 

C. cf. carbonaria (Hall, 1858) Crasquin, 1984* ... . 

C. disjuncta (Morey, 1935) Sohn, 1971 .......... . 

C. grekoffi Tschigova, 1977 .................... . 

C. aff. inflata (Munster, 1830) Sohn, 1971 ....... . 

C. kaisini Rome, 1973 ........................ . 

C. lima Tschigova, 1977 ...................... . 

C. lysi Tschigova, 1977 ....................... . 

C. nuda (Tkatcheva, 1972) Tschigova, 1977 ...... . 

C. obscura Tschigova, 1977 ................... . 

C. procera (N. lvanova, 1975) Kotschetkova, 1980 .. 

C. rare (Tschigova, 1958) new combination ...... . 

C. sparsa Kotschetkova, 1984 .................. . 

C. suborbiculata (Pozner, 1951) Sohn, 1971 ...... . 

C. tumida (Kummerow, 1939) Sohn, 1971 ........ . 

C.? sp. Sohn, 1971 ........................... . 

Greatest length 

2.15 

0.93 

2.42 

2.00 

3.25 

3.20 

0.70 

1.17 

2.42 

1.10 

1.37 

1.55 

0.975 

1.17 

1.20 

1.20 

1.125 

1.21 

2.70 

2.07 

Greatest height 

1.40 

0.81 

1.90 

1.50 

2.45 

2.55 

0.40 

0.84 

1.46 

0.70 

0.95 

1.20 

0.925 

0.88 

0.99 

0.93 

0.87 

1.01 

2.03 

1.52 

Age 

Late Meramecian ....... . 

Visean ............... . 

Early Meramecian ...... . 

Early Namurian ........ . 

Visean ............... . 

Late Tournaisian ....... . 

Basal Mississippian ..... . 

Early Toumaisian ...... . 

Early Meramecian ...... . 

Early Toumaisian ...... . 

. ........ do ........ . 

. ........ do ........ . 

Late Toumaisian ....... . 

Early Toumaisian ...... . 

......... do ........ . 

Late Tournaisian ....... . 

Moscovian ............ . 

Visean ............... . 

. . . . . . . . . do ........ . 

Early Meramecian ...... . 

Occurrence 

Alaska. 

U.S.S.R. 

Alaska. 

Libya. 

Indiana. 

Canada. 

Missouri. 

Europe. 

Alaska. 

Belgium. 

U.S.S.R. 

Europe. 

U.S.S.R. 

U.S.S.R. 

U.S.S.R. 

U.S.S.R. 

U.S.S.R. 

U.S.S.R. 

Germany . 

Alaska. 

Ostracodes, Paine Member of the Lodgepole Limestone, Utah E5 
width is behind midlength (pl. 1 , fig. 11; pl. 2, figs. 8, 14, 

23, 28). The inner lamella is of even width (pl. 1, figs. 9, 

10). 

Discussion.-The valves are larger than any of the species referred to Chamishaella except C. carbonaria (Hall, 

1858), which is more rounded in lateral outline and wider in 

dorsal outline. C. lodgepoleana differs from the European 

C. lysi Tschigova, 1977, in lacking a step-like offset of the 

posterior part of the ventral margin, in larger size, and in 

more elongated lateral outline. Only large specimens were 

available for study, because the fine fraction of the acid 

residues was not recovered. There are more dissociated 

valves and fragments than carapaces, but the size range 

suggests that the specimens were not size-sorted as individuals. They could, however, have been transported by mudslides. The presence of encrusting worm tubes inside and 

outside of dissociated valves (pl. 1, figs. 7, 17, 18; pl. 2, 

figs. 25-28) indicates that the rate of sedimentation was 

slow enough to permit other animals to settle and grow on 

and in the valves. 

REFERENCES CITED 

Adamczak, F .J., 1981, Preliminary results of a study of sedimentary structures and orientation of ostracode valves in carbonate rocks of Gotland, Sweden: Stockholm Contributions in 

Geology, v. 37, p. 1-8, 2 pls. 

Becker, Gerhard, 1971, Paleocology of Middle Devonian ostracods from the Eifel Region, Germany, in Oertli, H.J., ed., 

Colloque sur Ia paleoecologie des ostracodes-Colloquium 

on the paleoecology of ostracodes, Pau. 20-27, VII, 1970: 

Centre Recherches de Pau-SNPA Bulletin, v. 5, supplement, 

p. 801-816, 6 figs. 

---1981 , Ostracoden im Devon Europas - Palaogeographische 

and biostratigraphische Aspekte: Natur und Museum, v. Ill, 

no. II, p. 378-383, 2 figs. 

---1982, Ostracoden-Entwicklung im Kantabrischen 

Variszikum (Nordspanien): Neues Jahrbuch fiir Geologie und 

Palaontologie, v. 163, no. 2, p. 153-163, 3 figs. 

Benson, R.H., 1961, Ecology of ostracode assemblages, in 

Moore, R.C., ed., Treatise on invertebrate paleontology, 

Part Q, Arthropoda 3, Crustacea, Ostracoda: New York and 

Lawrence, Kansas, Geological Society of America and University of Kansas Press, p. Q56-Q63, I fig. 

Berdan, J.M., 1984, Leperditicopid ostracodes from Ordivician 

rocks in Kentucky and nearby States, and characteristic features of the Order Leperditicopida: U.S. Geological Survey 

Professional Paper 1066-J, 40 p., II pis. 

Blake, D.B., 1981, Paleoecology of Bryozoa, in Broadhead, 

T. W., ed., Lophophorates, notes for a short course: University of Tennessee, Department of Geological Sciences, 

Studies in Geology 5, 251 p. 

Bless, M.J.M., 1983, Late Devonian and Carboniferous ostracode 

assemblages and their relationship to the depositional enviE6 Shorter Contributions to Paleontology and Stratigraphy 

ronment: Bulletin de Ia Societe beige de Geologie, Periodique 

trimestriell, v. 92, fasc. I, p. 31-53, 20 figs. 

Bless, M.J .M., and Massa, D., 1982, Carboniferous ostracodes in 

the Rhadames Basin of western Libya-Paleoecological implications and comparison with North America, Europe, and 

the USSR: Revue de l'Institut Fran~ais du Petrole, v. 37, 

no. 1, p. 19-61, 5 pls. 

Cotter, Edward, 1965, Waulsortian-type carbonate banks in the 

Mississippian Lodgepole Formation in central Montana: Journal of Geology, v. 73, no. 6, p. 881-888, 4 figs. 

Crasquin, Sylvie, 1984, Ostracodes du Dinantien, systematique -

biostratigraphie-paleoecologie (France, Belgique, Canada): 

Ph.D Thesis, Universite des Sciences et Technique de Lille, 

v. I, 238 p., v. 2, 68 p., 23 pls. 

GutschickR.C., Sandberg, C.A., and Sando, W.J., 1980, Mississippian shelf margin and carbonate platform from Montana to 

Nevada, in Fouch, T.D., and Magathan, E.R., eds., Paleozoic paleogeography of the west-central United States [-

Proceedings of the Rocky Mountain Paleogeography Symposium I, Denver, Colorado, June 1980]: Denver, Rocky 

Mountain Section of Society of Economic Paleontologists and 

Mineralogists, p. 111-128, 10 figs. 

Kotschetkova, N.M., 1980, Novye khel'diidae (ostracoda) iz 

turneiskikh otlozhenii yuzhnogo Yurala, in Yusupov, B. M. , 

ed., Stratigrafiya i fauna Devona i Karbona yuzhnogo Yurala: 

Akademia Nauk SSR, Bashkirskii Filial, Institut Geologii, 

Yufa, p. 33-43, pl. 6. 

---1984, Ostrakody Moskovskogo Yarusa vostochnogo 

sklona yuzhnogo Yurala: Paleontologicheskii Zhurnal, 1984, 

no. 2, p. 73, 75-81, pl. 8. 

Rome, Remade, 1973, Contribution a l'etude des ostracodes du 

Tournaisien Inferieur de la Belgigue (Suite): Bulletin de Ia 

Societe beige de Geologie Periodique trimestrielle, v. 82, 

fasc. 2, p. 301-349, 45 figs. 

Sandberg, C.A., and Gutschick, R.C., 1980, Sedimentation and 

biostratigraphy of Osagean and Meramecian starved basin and 

foreslope, western United States, in Fouch, T.D., and Magathan, E.R., eds., Paleozoic paleogeography of the westcentral United States [-Proceedings of Rocky Mountain Paleogeography Symposium I, Denver, Colorado, June 1980]: 

Denver, Rocky Mountain Section of Society of Economic 

Paleontologists and Mineralogists, p. 129-147, 10 figs. 

Sando, W.J., 1980, The paleoecology of Mississippian corals in 

the western conterminous United States: Acta Palaeontologica 

Polonica, v. 25, no. 3-4, p. 619-631, 4 figs. (published in 

1981). 

Sando, W.J., Dutro, J.T., Jr., and Gere, W.C., 1959, Brazer 

Dolomite (Mississippian), Randolph Quadrangle, Northeast 

Utah: American Association of Petroleum Geologists Bulletin, v. 43, no. 12, p. 2741-2769, 6 figs. 

Smith, D.L., 1972, Depositional cycles of the Lodgepole Formation (Mississippian) in central Montana, in Montana Geological Society 21st Annual Field Conference Guidebook, 

Billings, Montana, Sept. 22-24, 1972: p. 29-35, 7 figs. 

---1977, Transition from deep- to shallow-water carbonates, 

Paine Member Lodgepole Limestone, central Montana, in 
Cook, H.E., and Enos, Paul, eds., Deep-water carbonate 

environments: Society of Economic Paleontologists and Mineralogists Special Publication 25, p. 187-201. 

Sohn, I.G., 1969, Pseudoleperditia Schneider, 1956 (Ostracoda, 

Crustacea), an Early Mississippian genus from southwestern 

Nevada: U.S. Geological Survey Professional Paper 643-C, 

p. Cl-C6, 1 pl. 

---1971, New Late Mississippian ostracode genera and species from northern Alaska: U.S. Geological Survey Professional Paper 711-A, 24 p., 2 pls. 

---1972, Late Paleozoic ostracode species from the conterminous United States: U.S. Geological Survey Professional 

Paper 711-B, 13 p., 12 pls. 

---1979, Biostratigraphic significance of the Late Devonian 

and Mississippian genus Pseudoleperditia Schneider, 1956 

(Ostracoda, Crustacea): Journal of Paleontology, v. 53, no. 5, 

p. 1243-1256, 2 pls. 

Stone, R.A., 1972, Waulsortian-type bioherms (reefs) of Mississippian age, central Bridger Range, Montana, in Montana 

Geological Society 21st Annual Field Conference Guidebook, 

Billings, Montana, Sept. 22-24, 1972: p. 37-55, 23 figs. 

Tschigova, V.A. (Chizhova), 1958, Ostrakody kizelovskogo gorizonta Sartovsko-Stalingradskogo Povol'zhya: Trudy 

V sesoyuznyi Neftegazovyi Nauchno-Issledovatel' skii Institut 

(VNII), vyp. 14, p. 58-85, 10 pls. 

---1977, Stratigrafiya i korrelatsiya neftegazonosnykh 

otlozhenii Devona i Karbona Evropeiskoi chasti SSSR i 

zarubezhnykh stran: Izdat. "Nedra", Moscow, 263 p., 47 pls. 

Ulrich, E.O., and Bassler R.S., 1906, New American Paleozoic 

Ostracoda. Notes and descriptions of Upper Carboniferous 

genera and species: U.S. National Museum Proceedings, 

v.30,p.149-164,pl.ll. 

Whatley, Robin, 1983, The application of Ostracoda to paleoenvironmental analysis, in Maddocks, R.F., ed., Application of 

Ostracoda: Proceedings of the Eighth International Symposium on Ostracoda, July 26-29, 1982. Department of Geosciences, University of Houston, Texas, p. 51-77, 7 figs. 

Wilson, J.L., 1969, Microfacies and sedimentary structures in 

"deeper water" lime mudstones, in Friedman, G.M., ed., 

Depositional environments in carbonate rocks: Society of 

Economic Paleontologists and Mineralogists Special Publication 14, p. 4-19. 

Ostracodes, Paine Member of the Lodgepole Limestone, Utah E7 

PLATES 1-2 

Contact photographs of the plates in this report are available at cost from U.S. Geological 

Survey Library, Federal Center, Denver, CO 80225 
PLATE 1 

[Magnification approx. X 20] 

Figures 1-19. Chamishaella lodgepo/eana Sohn, n. sp. 

1,2. Posterior and outside views of right valve, heteromorph, paratype, USNM 401093, USGS colln. 16809-PC. 

3,4. Outside and posterior views of left valve, heteromorph, USNM 401094, USGS coHn. 16810-PC. 

5-8. Outside, posterior, dorsal (anterior to left), and interior views of left valve, heteromorph, para type, USNM 401095, USGS colln. 1681 0-PC. 

9, 10. Dorsal oblique (anterior to left) and inside views of left valve, heteromorph, paratype, USNM 401096, USGS coHn. 16827-PC. Note inner 

lamella. 

11, 12. Dorsal (anterior and left) and posterior views of right valve, heteromorph, paratype, USNM 401097, USGS colln. 16809-PC. 

13-16. Left, anterior, posterior, and dorsal (anterior to top) views of carapace, heteromorph (adult female), holotype, USNM 401098, USGS colln. 

16808-PC. 

17. Inside of fractured and misshaped left valve, tecnomorph, paratype, USNM 401099, USGS coHn. 16809-PC. Note encrusting worm 

emplaced probably after the valve was fractured. 

18,19. Ventral oblique (anterior to left) and outside views of right valve, heteromorph, paratype, USNM 401100, USGS colln. 16809. Note 

over-reaching dimorphic swelling on fig. 18. 
DEPARTMEI'\T OF THE 11'\TERIOR 

U.S. GEOLOG ICAL SURVEY 

11 

12 

CHAJMISHAELLA LODGEPOLEANA 

BULLET!!'\ 1690--E PLATE 
PLATE 2 

[Magnification approx. X20] 

Figures 1-28. Chamishaella lodgepoleana Sohn, n. sp. 

1- 4. Left, posterior, right, and dorsal (anterior to right) views of carapace, smallest growth stage recovered, tecnomorph, paratype, USNM 

401101, USGS colin. 16809-PC. 

5-8. Posterior, dorsal (anterior to left), right, and ventral (anterior to right) views of carapace, tecnomorph, paratype, USNM 401102, USGS 

colin. 16810- PC. 

9- 11. Posterior, outside, and inside views of right valve, tecnomorph, paratype, USNM 401103, USGS colin. 16810- PC. 

12- 15. Dorsal (anterior to left), left, ventral (anterior to right), and posterior views of carapace, tecnomorph, paratype, USNM 401104 USGS colin. 

16810-PC. 

16-20. Dorsal (anterior to right), right, anterior, posterior, and ventral (anterior to right) views of carapace with the right valve slightly dislocated, 

tecnomorph, paratype, USNM 401105, USGS colin. 16810-PC. 

21 - 24. Inside, outside, ventral (anterior to right), and anterior views of cracked right valve, tecnomorph, paratype, USNM 401106, USGS colin. 

16810-PC. 

25- 28. Outside, posterior, inside, and ventral (anterior to right) views of left valve, presumed male, paratype, USNM 401107, USGS colln. 

16810- PC. Note encrusting worm on inside. 
DEPARTMENT OF THE INTERIOR 

U.S. GE OLOGICAL SURVEY 

CHAMISHAELLA LODGEPOLEANA 

BULLETI N 1690-E PLATE 2 

CHAPTER F 

Some Ordovician and Permian-Triassic 

Conodonts from Xizang (Tibet) 

By Anita G. Harris, john E. Repetski, and Erie G. Kauffman 

U.S. GEOLOGICAL SURVEY BULLETIN 1690 

Shorter Contributions to Paleontology and Stratigraphy 

CONTENTS 

Abstract Fl 

Introduction Fl 

Acknowledgments F3 

Analysis of Paleozoic clasts in Mesozoic strata F3 

Ordovician conodonts from the Nyalam Road section F3 

Conclusions FS 

References cited FS 

PLATES 

[Plates follow References Cited] 

1. Neogondolella sp. from locality KC-80-24-1 

2. Ordovician conodonts from Nyalam Road section 

FIGURES 

1. Map showing location of conodont samples along route of Academia Sinica excursion across Qinghai-Xizang (Tibet) Plateau F2 

2. Section showing pre-Mesozoic stratigraphy of Tethys-Himalayan southern sub-belt 

in Xi gaze District F 4 

Contents iii 

Some Ordovician and Permian-Triassic Conodonts 

from Xizang (Tibet) 

By Anita G. Harris, john E. Repetski, and Erie G. Kauffman 

Abstract 

Conodonts from Tibet extend the known geographic range of 

several taxa and demonstrate the utility of these fossils for 

Tibetan Paleozoic and Mesozoic geologic studies. One Late 

Permian or Triassic conodont dates its host-rock, which is an 

olistolith within an Upper Triassic unit. Samples from an 

Ordovician succession north of Nyalam yielded conodonts 

indicative of the North Atlantic conodont faunal province. One 

of these contains the index species Pygodus serra (Hadding), 

which provides a precise global correlation for this collection. 

INTRODUCTION 

Our present knowledge of conodont occurrence and distribution in Tibet is quite sparse due both to difficulty of 

access and, until recently, to the general lack of conodont 

study in this remote region. In May, June, and July 1980, 

the Academia Sinica of the People's Republic of China 

sponsored a stimulating international conference in Beijing 

(Peking) on the biological and geological evolution of the 

Qinghai-Xizang (Tibet) Plateau, during which a considerable amount of new and/or poorly known geologic data on 

this area were presented and then published (Liu DongSheng and others, 1981). Of particular importance to 

stratigraphers in these volumes are updated stratigraphic 

summaries, biozonal schemes, and regional correlations for 

Tibet and surrounding regions. For the Paleozoic, especially 

significant papers are by Chen Ting-en (1981), Gupta 

(1981), Jin Yu-gan (1981), Wang Yu-jing and Mu Xi-nan 

(1981), Waterhouse and Gupta (1981), Wen Shi-xuan and 

others (1981), Wu Wang-Shi and Liao Wei-hua (1981), 

Zhang Lin-xin ( 1981 ), and the Scientific Guidebook to South 

Xizang (Tibet) (Organizing Committee; Scientific Guidebook to South Xizang; 1980). These works serve as bases 

for new international correlations. One of us (EGK) had the 

privilege to participate in this conference and the subsequent 

Tibet expedition. 

The final phase of the Qinghai-Xizang Conference was a 

2-week field trip across the Tibet Plateau, focusing on a 

transect between Lhasa, Xigaze, Lhaze, Tingri, Nyalam, 

and Zham (fig. 1), which crossed the famous YarlungZangbo ophiolite belt, the Greater Himalayas, and provided 

a rare opportunity to study and collect fossils through representative, well-exposed Paleozoic and Mesozoic sequences. 

Visiting scientists were encouraged by the Chinese hosts to 

collect, identify, and report on relevant fossil material. This 

paper documents the conodonts collected in the transect 

across Tibet by one of us (EGK). 

Paleozoic rocks occur in four settings in south-central 

Tibet. To the north of the Yarlung-Zangbo suture, which 

parallels the river of that name (fig. 1), Paleozoic carbonate 

and chert cobbles are common elements of Mesozoic (predominantly Cretaceous) inner-shelf conglomerates, proximal turbidites, and submarine fan systems in a rapidly deepening back-arc basin. Probable Paleozoic blocks are caught 

up in melange marginal to the ophiolite belts as well. South 

of the Yarlung-Zangbo suture (fig. 1), massive olistostromes, or "exotic blocks" of fossiliferous Permian shelf 

carbonates, as much as 4.4 km2 in diameter, occur in basinal 

Triassic sandstones and shales apparently reflecting early 

phases of subduction of an encroaching Gondwanan plate 

margin into a deepening fore-arc basin or trench. Further 

south, between Chiatsun and Y arleb in the' region north of 

Nyalam (fig. 1), south of the 5,100-m Yagru-Xongla Pass, 

an extensive in situ Paleozoic sequence was transected by 

this trip, and collections were made from Ordovician 

through Devonian marine strata. 

In total, collections of Paleozoic rocks were made from 

17 different localities during the expedition. Conodonts 

were recovered from 3 of 17 Paleozoic samples, and are 

reported on herein. This report is necessarily deficient in 

scope and geological context because of the reconnaissance 

sampling. We believe, however, that these findings add 

significant information concerning world wide conodont and 

conodont-biofacies distribution. We hope that this note will 

stimulate further interest and research on the faunas and 

biostratigraphy of this geologically important, remote region. 

Ordovician and Permian-Triassic Conodonts, Xizang (Tibet) Fl 
.., 

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- - - - EXCURSION ROUTE 

X SAMPLE LOCALITIES 

r 

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85° 90° 

Figure 1. Map showing location of conodont samples along route of Academia Sinica excursion across Qinghai-Xizang (Tibet) Plateau (modified from Organizing 

Committee; A Scientific Guidebook to South-Xizang, 1980). 

30° 
Acknowledgments 

We wish to thank many paleontological colleagues in the 

People's Republic of China who provided guidance, fellowship, and who gave freely of their time and expertise during 

the Qinghai-Xizang (Tibet) Plateau expedition. In particular 

we express our gratitude to Prof. Liu Dong-sheng of the 

Academia Sinica, Secretary General of the conference, principal coordinator of the expedition, and chief editor of the 

proceedings, and Dr. S. Dillon Ripley, Secretary of the 

Smithsonian Institution and good colleague during the expedition, who provided funding through a grant to the junior 

author (EGK). Dr. Chen Jun yuan, Nanjing Institute of 

Geology and Paleontology, Academia Sinica, PRC, kindly 

read the manuscript during his visit to the U.S. National 

Museum in June 1982; his suggestions and discussions improved the manuscript and brought us to a better understanding of Ordovician stratigraphy in China. We also thank R. T. 

Lierman and H.E. Mochizuki (USGS) for their excellent 

technical assistance in preparing the figures and illustrations. 

ANALYSIS OF PALEOZOIC CLASTS IN 

MESOZOIC STRATA 

Paleontologic analysis of older clasts in the Mesozoic 

rocks of Tibet is an important tool in defining the geology 

of source areas. In regions as tectonically active as the Tibet 

Plateau, where older terranes have commonly been metamorphosed or destroyed, residual clast analysis may also 

yield the only evidence of facies, age, biozone(s), and correlations for older rock suites. Clasts further provide minimum ages for large-scale tectonic events which incorporate 

host rocks, or which produce olistostromes, debris flows, 

etc. 

Thirteen of the samples processed in this study were individual clasts collected from Mesozoic (predominantly Cretaceous) conglomerates, melange, and olistostrome-bearing 

units. These clasts ranged from 15 to 146 grams each. 

Possible Paleozoic clast samples came from (a) 

olistrostromes in the Upper Cretaceous Zonghuo Group 

(Kauffman locality KC-80-16 along the road between 

N angagarze and Gyangze); (b) conglomerates of the 

Qiabuling Formation (Middle Cretaceous), upper part 

(Kauffman locality KC-80-18, 18 km west-northwest of 

Xigaze ); (c) the "Castle" Conglomerate (Xigaze Group; 

Middle Cretaceous) at the base of the upper N gamring 

flysch, behind the Zhaxilhunbo Temple in Xigaze (Kauffman locality KC-80-22-1); and (d) from cobbles in 

melange (Triassic?) facies at the top of Cuola Pass (Kauffman locality KC-80-23-1). All proved barren of 

conodonts. 

Only one clast produced phosphatic microfossils (Kauffman locality KC-80-24-1: USGS collection number 

29820-PC), a 143-g piece of limestone from a large olistostrome block embedded in dark, finely laminated "Upper 

Triassic Shale Formation." The sample was collected from 

an exposure in a river cut in a north-flowing tributary of the 

Yarlung-Zangbo River, 100 m northwest of the road between Xigaze and Lhaze, 40 km east of Lhaze, on the east 

side of Cuola Pass (fig. 1). This clast yielded only one 

posterior platform fragment of a Neogondollela (sp. indet.) 

of a Late Permian through Triassic morpho type (pl. 1). The 

color alteration index (CAl) of this fragment is 3 to 4, 

indicating that that host rock (but not necessarily the entire 

olistostrome unit) reached at least 120° to 180° C during its 

burial and tectonic history. The limestone olistostromes in 

this area are unnamed. Brachiopod faunas reported from 

these blocks include Permian species of Neospirifer, Spiriferrella, Stenoscisma, and Marginifera. This assemblage 

and the carbonate facies of the blocks are similar to those of 

crystalline limestones of the late Early Permian Baidingpu 

Formation in the Tethys-Himalyan Northern Sub-Belt of the 

Xigaze District (Wen Shi-xuan and others, 1981, Table 2; 

Organizing Committee; Scientific Guidebook to South Xizang, 1980, p. 66). The Late Permian to Triassic age of the 

conodont in the Cuola Pass exotic block may indicate 

younger Permian carbonates in the Tethyan-Himalayan 

Province than are known at present. 

ORDOVICIAN CONODONTS FROM THE 

NYALAM ROAD SECTION 

The best Paleozoic sequence encountered on this expedition is exposed along both sides of the road between Y agru 

Xongla Pass and Nyalam (fig. 1), and in particular between 

the villages of Chiatsun and Y arleb. Figure 2 outlines the 

stratigraphic section in this region. The Lower Ordovician 

(current conventional usage in China places the boundary 

between the Lower and Upper Ordovician at the 

Llanvimian-Llandeilian Series boundary, fide Chen Junyuan, written commun., 1982), in ascending order, consists 

ofthe Rougicun Formation (a nonfossiliferous, poorly dated 

unit that may be wholly or partly of Cambrian age;fide Chen 

J.Y., oral commun., to JER, 1982), consisting of laminated 

argillaceous crystalline limestone and marble; and the 

"Lower Formation" (unnamed) of the Ordovician Chiatsun 

Group. The "Lower Formation", 726 m thick, is composed 

of fossiliferous dark-gray limestone with minor sandstone, 

siltstone, and dolomite, and contains a nautiloid fauna suggesting a middle Arenigian (Chen Jun-yuan, 1975), Early to 

early Middle Ordovician age (in North American usage) at 

the base (Pomphoceras-Wutinoceras Biozone), and an early 

Llanvimian age at the top (Dideroceras-Paradnatoceras 

Biozone) (Organizing Committee; Scientific Guidebook to 

South Xizang, 1980, p. 82, 83). Limestone samples collected from the "Lower Formation" of the Chiatsun Group 

in outcrops along the east side of the road between Y agru 

Xongla Pass and Nyalam, 24 to 25 km north-northeast of 

Nyalam yielded conodonts from one sample (USGS colin. 

Ordovician and Permian-Triassic Conodonts, Xizang (Tibet) F3 
9207-CO; 150-g sample processed). The conodont assemblage consists of three graciliform elements of Panderodus 

cf. P. sulcatus (Ffthraeus) (Pl. 2A, B) and one scandodontiSYSTEM NAMES OF STRATA LITHOLOGY AND 

THICKNESS 

Siltstone intercalated w1th bioclastic 

Chubujeka Formation limestone and shale z 375m < Selung :i p 

a: Group 

~ Chubuk Formation Sandstone. quartzose. intercalated with 

dark-gray shale; 20 m 

Chaya Quartzose Sandstone. quartzose; 700 m Sandstone Member 

c3 Gilung Stepanoviella-beanng sandy siltstone member; 1 m Formation f/) 

::> 

0 Chataje Diamictite a: Glac1o-manne sediments; about 30 m w Member ~ 

z 

0 

CD 

~ Naxing Formation Shale. gray Intercalated w1th quartz 

sandstone and a little marlite; 1,888 m 

c,+2 

Yali Format1on Alternating beds of marlite and shale; 

60m 

Upper Formation Shale. grayish-black intercalated w1th 

sandstone; 66 m 

z 02+3 Pochu Group 

~ Lower Formation Sandstone. light-gray, quartzose 

z 12.56 m 

~ 

~ 

o, Liangquan Formation Shale. dark-gray; 40 m 

z s2+3 Pulu Group Sandstone. quartzose intercalated with 

~ calcareous shale and limestone; 46 m 

a: 

::> 

...1 

iii s, Sandstone. graptolith1c shale and Shiqipo Formation limestone; 90 m 

03 Hongshantou Formation Shale. brown intercalated w1th tine 

sandstone; 70 m 

02 Limestone. argillaceous, purplish-red 

Upper Formation 97 m z 

< I--- Q 

8 Chiatsun 

Group Limestone Intercalated w1th dolomitic 

~ Lower Format1on limestone and calcareous sandstone; 

o, 726m 

Rouqicun Formation Limestone. striped and laminated. marble; 

237-48 m 

6-Z North Col Formation Phyllite. quartzite. marble. biotite quartz 

schist. greater than 1.000 m 

FAULT 

ANZ (7) Nyalam Group 

Kyanite schist. staurolite schist, sillimanite 

gneiss. marble. ocular and striped 

m1gmatite. greater than 10.000 m 

Figure 2. Pre-Mesozoic stratigraphy of Tethys-Himalayan 

southern sub-belt in Xigaze District (modified from Organizing 

Committee; Scientific Guidebook to South Xizang, 1980, Tables 

1-3). 

F4 Shorter Contributions to Paleontology and Stratigraphy 

form element of Scolopodus cf. S. cornuformis Sergeeva 

(Pl. 2C). These taxa are typical of the North Atlantic 

conodont province, reflecting cool and/or deeper water 

marine paleoenvironments. Further, they indicate a probable Llanvimian age (Whiterockian to early Chazyan in 

North American usage), which is compatible with associated macrofaunas in the upper part of the "Lower Formation." 

The "Upper Formation" (unnamed) of the Chiatsun 

Group consists of 97 m of purplish-red, argillaceous limestone containing abundant nautiloids, crinoids, and brachiopods representing most of the Middle Ordovician (Organizing Committee; Scientific Guidebook to South Xizang, 

1980, p. 83, 84). The nautiloids represent the widespread 

Asian (Tethyan) biozone of Sinoceras chinense (with S. 

densum and Beloitoceras xizangense) of Middle Ordovician 

(Llandeilian to Caradocian) age (Chen Jun-yuan, 1975; 

Chen Ting-en, 1981, p. 164). 

Three blocks from the Middle Ordovician "Upper Formation" of the Chiatsun Group were processed for conodonts. 

One of the three limestone blocks (USGS colln. 9206-CO; 

411 g), yielded Cornuodus cf. C. longibasis (Lindstrom) (5 

elements), Dapsilodus? similaris (Rhodes), Drepanoistodus 

spp. (7 elements), Drepanodus arcuatus Pander, Panderodus sp. (3 elements), Periodon cf. P. aculeatus Hadding, Protopanderodus varicostatus (Sweet and Bergstrom) 

(14 elements), and Pygodus serra (Hadding) (1 haddingodontiform and 6 pygodontiform elements). The CAl of 

these elements is 5112, indicating that the host rock reached 

at least 300° C during or after burial. The conodonts from 

both productive Ordovician samples show little if any structural deformation; most of the problems of identification 

were due to fragmental specimens and adventitious material. 

This species association represents an early Middle Ordovician fauna that is typical of the Pygodus serra Biozone 

of the North Atlantic Province; it is thus compatible with the 

cephalopod biozone date. The P. serra Zone correlates with 

the uppermost part of the Whiterockian Stage through the 

lower half of the Chazyan Stage of the North American, 

Middle Ordovician, Champlainian Series (see Bergstrom, 

1977). This fauna also correlates with part of the Middle 

Ordovician sequence from southern Jiangsu Province reported by Chen Ming-juan and Chen Yan-tang (1979). The 

lower part of the range of this conodont association overlaps 

the upper limit of the possible range of the species association found in USGS colln. 9207-CO. The two horizons 

could be the same or nearly the same age, but these faunules 

show that at least they are consistent in sequence. 

Although most of the taxa in these two Ordovician 

faunules are long-ranging within the Ordovician, the presence here of the Middle Ordovician zonal index Pygodus 

serra is of considerable biostratigraphic significance. Because of its short range and widespread occurrence, P. serra 

represents a taxon that can be used in correlation of Middle 
Ordovician strata virtually around the globe. It is now 

known from both sides of the Atlantic Ocean (Bergstrom, 

1971; 1973; Bergstrom and Carnes, 1976; Bergstrom, Riva, 

and Kay, 1974; Dzik, 1978; Hunter, 1978; Lamont and 

Lindstrom, 1957; Lofgren, 1978), from along the western 

side of the North American Cordillera (Harris and others, 

1979; Tipnis and others, 1978; USGS collections made by 

AGH from southeastern Alaska) and from Australia (Nicoll, 

1980) and possibly New Zealand (Simes, 1980), the Ural 

Mountains, USSR (Nassedkina and Puchkov, 1979), Xinxiang, South China (An Tai-xiang, 1981), southern Jiangsu, 

China (Chen Ming-juan and Chen Yun-tang, 1979), the 

eastern Yangtze Gorges (Zeng Qing-luan and others, 1983), 

and now Tibet. 

CONCLUSIONS 

These small samples provide important data on geographic extensions of several conodont species, some of 

which are of proven utility for regional and intercontinental 

correlation of Ordovician sequences. They also demonstrate 

the potential of conodonts in identifying sources of rocks 

found as introduced clasts in Tibetan Mesozoic conglomerates, melange, and olistostromes. The Ordovician succession northeast of Nyalam has the potential to provide an 

important sequence of North Atlantic Province conodont 

faunas, and further work on this and other Paleozoic rocks 

in the region is strongly encouraged. 

REFERENCES CITED 

An Tai-xiang, 1981, Recent progress in Cambrian and Ordovician 

conodont biostratigraphy of China, in Teichert, Curt, Liu, 

Lu, and Chen Pei-ji, eds., Paleontology in China, 1979: Geological Society of America Special Paper 187, p. 209-225. 

Bergstrom, S.M., 1971, Conodont biostratigraphy of the Middle 

and Upper Ordovician of Europe and eastern North America, 

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conodont biostratigraphy: Geological Society of America 

Memoir 127, p. 83-162. 

---1973, Biostratigraphy and facies relations in the lower 

Middle Ordovician of easternmost Tennessee: American Journal of Science, Cooper Volume 273-A, p. 261-293. 

---1977, Early Paleozoic conodont biostratigraphy in the Atlantic borderlands, in Swain, F .M., ed., Stratigraphic micropaleontology of Atlantic basin and borderlands: Elsevier, 

Amsterdam, p. 85-110. 

Bergstrom, S.M., and Carnes, J.B., 1976, Conodont biostratigraphy and paleoecology of the Holston Formation (Middle 

Ordovician) and associated strata in eastern Tennessee, in 

Barnes, C.R., ed., Conodont paleoecology: Geological Association of Canada Special Paper 15, p. 27-57. 

Bergstrom, S.M., Riva, John, and Kay, Marshall, 1974, Significance of conodonts, graptolites, and shelly faunas from the 

Ordovician of western and north-central Newfoundland: 

Canadian Journal of Earth Science, v. 11 , p. 1625-1660. 

Chen Jun-yuan, 1975, The fossil nautiloids from the Mount Jolmo 

Lungma Region, in A report of scientific expedition in the 

Mount Jolmo Lungma Region (1966-1968): Palaeontol., 

Fasc. I, p. 267-308, [in Chinese]. 

Chen Ming-juan and Chen Yun-tang, 1979, Middle Ordovician 

conodontes [sic] from southern Jiangsu [abs.]: The Palaeontological Society of China, 12th Annual Conference and 3rd 

National Congress, Abstracts of Papers, p. 35-36. 

Chen Ting-en, 1981 , Ordovician and Silurian cephalopod provincialism in Xizang, with comments on the continental drift, in 

Liu Dong-sheng, editor-in-chief, and others, 1981, Geological and ecological studies of Qinghai-Xizang Plateau; 

Volume 1, Geology, Geological History, and Origin of Qinghai-Xizang Plateau: Proceedings of Symposium on QinghaiXizang [Tibet] Plateau (Beijing, China); Sciences Press, 

Beijing; and Gordon and Breach, Science Publishers, Inc., 

New York, 974 p. 

Dzik, Jerzy, 1978, Conodont biostratigraphy and paleogeographical relations of the M6jcza Limestone (Holy Cross Mountains, Poland): Acta Palaeontologica Polonica, v. 23, no. 1, 

p. 51-72, pis. 12-15. 

Gupta, V .J., 1981, Palaeozoic biostratigraphy and palaeogeography of the Himalaya, p. 293-296, in Liu Dong-sheng, editorin-chief, and others (see reference in this list). 

Harris, A.G., Bergstrom, S.M., Ethington, R.L., and Ross, R.J., 

Jr., 1979, Aspects of Middle and Upper Ordovician conodont 

biostratigraphy of carbonate facies in Nevada and southeast 

California and comparison with some Appalachian successions, in Sandberg, C.A., and Clark, D.L., eds., Conodont 

biostratigraphy of the Great Basin and Rocky Mountains: 

Brigham Young University Geology Studies, v. 26, Part 3, 

p. 7-43. 

Hunter, D.R., 1978, Conodonts from the Cobbs Arm Formation 

(Middle Ordovician) north-central Newfoundland: St. John's, 

Memorial University of Newfoundland, unpublished M. Sc. 

thesis. 

Jin Yu-gan, 1981, On the paleoecological relation between Gondwana and Tethys faunas in the Permian of Xizang, in Liu 

Dong-sheng, editor-in-chief, and others (see reference in this 

list), p. 171-178. 

Lamont, Archie, and Lindstrom, Maurits, 1957, Arenigian and 

Llandeilian cherts identified in the Southern Uplands of Scotland by means of conodonts, etc.: Edinburgh Geological Society, Transactions, v. 17, p. 60-70. 

Liu Dong-sheng, editor-in-chief, and others, 1981, Geological and 

ecological studies of Qinghai-Xizang Plateau; Volume 1, Geology, Geological History, and Origin of Qinghai-Xizang 

Plateau. Proceedings of Symposium on Qinghai-Xizang 

[Tibet] Plateau (Beijing, China): Science Press, Beijing, and 

Gordon and Breach, Science Publishers, Inc., New York, 

p. i-xxv and 1-974. 

LOfgren, Anita, 1978, Arenigian and Llanvirnian conodonts from 

Jamtland, northern Sweden: Fossils and Strata, no. 13, 129 p. 

Nassedkina, V.A., and Puchkov, V.N., 1979, Middle Ordovician 

conodonts of the northern Urals and their stratigraphic significance, in Papulov, C. N., and Puchkov, V. N., eds., 

Conodonts from the Urals and their stratigraphic significance: 

Akaderniya Nauk SSSR, Ural'skiy Filial, Trudy Instituta Geologiya i Geokhimiya, v. 145, p. 5-24. 

Ordovician and Permian-Triassic Conodonts, Xizang (Tibet) FS 
Nicoll, R.S., 1980, Middle Ordovician conodonts from the 

Pittman Formation, Canberra, ACT: Bureau of Mineral Resources Journal of Australian Geology and Geophysics, v. 5, 

p. 150-153. 

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(Tibet) Plateau, A Scientific Guidebook to South Xizang 

(Tibet): Academia Sinica, Beijing, 104 p., map. 

Simes, J.E., 1980, Age of the Arthur Marble: conodont evidence 

from Mount Owen, northwest Owen: New Zealand Journal of 

Geology and Geophysics, v. 23, p. 529-532. 

Tipnis, R.S., Chatterton, B.D.E., and Ludvigsen, R., 1978, 

Ordovician conodont biostratigraphy of the southern District 

of Mackenzie, Canada, in Stelck, C.R., and Chatterton, 

B.D.E., eds., Western and Arctic Canadian biostratigraphy: 

Geological Association of Canada Special Paper 18, p. 39-

91. 

Wang Yu-jing and Mu Xinan, 1981, Nature of the Permian biotas 

in Xizang and the northern boundary of the Indian plate, in 

Liu Dong-sheng, editor-in-chief, and others (see reference in 

this list), p. 179-185. 

Waterhouse, J.B., and Gupta, V.J., 1981, Permian brachiopod 

and bivalve zones in the Himalaya of India and Nepal, in Liu 

F6 Shorter Contributions to Paleontology and Stratigraphy 

Dong-sheng, editor-in-chief, and others (see reference in this 

list), p. 277-282. 

Wen Shi-xuan, Sun Dong-li, Dong De-yuan, Zhang Bing-gao, 

Wang Yu-jing, Liao Wei-hua, Wang Yi-gang, Chen Chuzhen, Chen Ting-en, He Guo-xiong, Mu Xi-nan, Yin Jiziang, and Wu Hao-tuo, 1981, Sedimentary development and 

formation of stratigraphic region in Xizang, in Liu Dongsheng, editor-in-chief, and others (see reference in this list), 

p. 119-130. 

Wu Wang-shi, and Liao Wei-hua, 1981, Stratigraphic distribution 

of fossil corals and their palaeobiogeographic provinces in 

Xizang, in Liu Dong-sheng, editor-in-chief, and others (see 

reference in this list), p. 165-170. 

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Xiang, Li-wen, 1983, Subdivision and correlation on the 

Ordovician in the eastern Yangtze Gorges, China: Bulletin of 

Yichang Institute of Geology and Mineral Resources, Chinese 

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p. 187-192. 
PLATES 1-2 

Contact photographs of the plates in this report are available at cost from U.S. Geological 

Survey Library, Federal Center, Denver, CO 80225 
PLATE 1 

Neogondolella sp. from locality KC-80-24-1. Stereo-pairs, upper (A) and lower (B) views 

of posterior platform fragment, USNM 398523, x 225. 
DEPARTMENT OF THE INTERJOl~ 

U.S. GEOLOGICAL SURVEY 

NEOGONDOLELLA 

BULLFTI:-< 1690-F PLATE 1 
PLATE 2 

A, B. Panderodus cf. P. sulcatus (Hihraeus); left lateral, X200, and right lateral, x 165, respectively, views of graciliform elements 

USNM 398524 and 398525. 

C. Scolopodus cf. S. cornuformis Sergeeva; inner lateral view of scandodontiform element, X 165, USNM 398526. 

D. Cornuodus longibasis (Lindstrom); left lateral view, X90, USNM 398527. 

E. Drepanodus? sp.; lateral view of drepanodontiform element, X66, USNM 398528. 

F, G. Protopanderodus varicostatus (Sweet and Bergstrom); outer lateral, X90, and inner lateral, X 100, views, respectively, of 

USNM 398529 and 398530. About half of the specimens in the collection have an anterobasal notch (pl. 2F). 

H. Drepanoistodus sp; inner lateral view of drepanodontiform element, USNM 398531, X 100. 

I, P. Drepanodus arcuatus Pander; inner lateral views of drepanodontiform, USNM 398532, x 100, and oistodontiform, USNM 

398533, X 115, elements, respectively. 

J. Drepanoistodus? sp.; lateral view of oistodontiform element, USNM 398534, x 115. 

K, L. Dapsilodus? similaris (Rhodes); left, x 115 and right, X80, lateral views of USNM 398535 and 398536, respectively. 

M, N, R. Pygodus serra (Hadding); upper views of pygodontiform elements (M, N) USNM 398537 and 398538, both X 130 and lateral 

view of haddingodontiform element (R), USNM 398539, x 180. 

0. Periodon cf. P. aculeatus Hadding; inner lateral view of falodontiform (= M) element, USNM 398540, X 130. 

Q. Drepanodus sp.; inner lateral view of drepanodontiform element, USNM 398541, x66. 

S. Panderodus sp.; left lateral view, USNM 398542, X80. 
DEPARTMENT OF THE INTERIOR 

U.S. GEOLOGICAL SURVEY 

ORDOVICIAN CONODONTS FROM NYALAM ROAD SECTION 

BULLETIN 1690-F PLATE 2