California Carboniferous 

Cephalopods

GEOLOGICAL SURVEY PROFESSIONAL PAPER 483-A
SK
California Carboniferous 

Cephalopods

By MACKENZIE GORDON, JR.

CONTRIBUTIONS TO PALEONTOLOGY

GEOLOGICAL SURVEY PROFESSIONAL PAPER 483-A

Descriptions and illustrations of 

IJ Late Mississippian and

Middle P ennsy Ivanian species 

and their distribution

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1964
UNITED STATES DEPARTMENT OF THE INTERIOR 

STEWART L. UDALL, Secretary

GEOLOGICAL SURVEY 

Thomas B. Nolan, Director

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

Washington, D.C. 20402
CONTENTS

Abstract

Panamint Range

Inyo Range

Providence Mountains

Page 

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1

______________ 1

______________ 1

______________ 2

______________ 5

6

Register of localities _ _ _ _

Page 

A6

6

7

7

22

23

27

PLATE 1

FIGURE

ILLUSTRATIONS

[Plates 1-4 follow index]

Orthoconic nautiloids of the genera Rayonnoceras, Mitorthoceras, and Bactritesl; cyrtoconic nautiloid of the genus

Scyphoceras; and a possible belemnoid, Hematites'?.

Coiled nautiloid of the genus Liroceras? and ammonoids of the genera Cravenoceras, Eumorphoceras, and Delepinoceras. 

Ammonoids of the genus Cravenoceras. 

Ammonoids of the genera Anthracoceras, Dombarocanites, Bisatoceras, Prolecanites (Rhipaecanites)!, Cravenoceratoides,

and Paralegoceras?. 

Map showing the Great Basin, Western United States_________-__________-__-____--_____-----------------

Correlation chart of Upper Mississippian rocks in the Great Basin_______________________________-------_-_

Geologic map showing Carboniferous cephalopod collecting localities in the Quartz Spring area, Panamint Range. 

Cravenoceras cross sections and sutures. ________________________________________________________________

5. Scatter diagram showing relative involution of the conch in California Cravenoceras- _______________---_------

6. Scatter diagram showing relative width of conch in California Cravenoceras----------------------------------

7. Eumorphoceras paucinodum Gordon, n. sp., external suture_________________________________---_-_---_-__--

8. Anthracoceras macallisteri Gordon, n. sp., external suture_________________________---__---------_------_-

9. Delepinoceras californicum Gordon, n. sp., external sutures.__________________________-__---_------------_-

10. External sutures of Dombarocanites and Prolecanites------------------------------------------------------

11. Bisatoceras cf. B. greenei Miller and Owen, external suture._____________________________------.-----------

12. Stenopronorites sp., partial external suture__ ____--___________________-_____-___---_-------------___-----

ill

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3

4

12

13

14

18

19

19

21

23

23
CONTRIBUTIONS TO PALEONTOLOGY

CALIFORNIA CARBONIFEROUS CEPHALOPODS

BY MACKENZIE GORDON, JR.

ABSTRACT

Cephalopods are abundant locally in a late Mississippian limestone bed in the Panamint Range, where the nautiloids Rayonnoceras, Bactritesl, Mitorthoceras, Scyphoceras, Lirocerasi, and 

a possible belemnite fragment referred to Hematites'! are associated with the goniatites Cravenoceras, Eumorphoceras, Anthracoceras, Delepinoceras, and Prolccanitesf. The cephalopod 

species in this bed and another species of Cravenoceras that 

occurs a few feet higher stratigraphically are characteristic 

of the widespread Eumorphoceras bisulcatum. zone in the Great 

Basin region of the western United States. In the Inyo Range, 

Bactritesl, Cravenoceras, Cravenoceratoides, Eumorphoceras, 

and Dombarocanites apparently represent a higher part of the 

same zone. Middle Pennsylvaiiian aminonoids Bisatoceras and 

Stenopronorites occur also in the Panamint Range and an 

ammonoid referred to Paralegocerasl has been found in the 

Providence Mountains. All these localities are in southeastern 

California.

New species described herein are Mitorthoceras clinatum, 

Cravenoceras inyoense, Eumorphoceras paucinodum, Anthracoceras macallisteri, Delepinoceras californicum, and Dombarocanites niasoni. The genera Cravenoceratoides, Delepinoceras, 

and Dombarocanites are described for the first time from the 

Western Hemisphere.

INTRODUCTION

The fossil cephalopods upon which this report is 

based came from three southern California mountain 

ranges and were collected by several geologists during 

the course of their mapping and other field studies in 

those areas. The location of the areas is shown in 

figure 1. Most of the fossils are from a single bed at 

the top of the Mississippian Perdido Formation in the 

Quartz Spring area at the northern end of the 

Panamint Range, Iiiyo County. A few came from 

three nearby localities in higher beds of Late Mississippian and Middle Pennsylvania!! age in the Quartz 

Spring area.

With a single exception, the rest came from the 

Mississippian Chainman Shale near the Cerro Gordo 

mine in the southern part of the Inyo Range, Inyo 

County. The exception is a mold of a large paralegocerid ammonoid in a block of limestone that was 

collected in the Providence Mountains, San Bernardino 

County.

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1 Providence Mountains, Calif.

2 Cerro Gordo area, Inyo Range, Calif.

3 Quartz Spring area, Panamint Range, Calif.

4 Diamond Range, Nev.

5 Egan Range, Nev.

6 Confusion Range, Utah

FIGURE 1. Map showing the Great Basin, main area of Chainman Shale 

culm-facies rocks, and locations of sections discussed.

ACKNOWLEDGMENTS

The writer wishes to thank Prof. S. W. Muller and 

A. M. Keen of Stanford University for making available the fossil material upon which a large part of this 

report is based. J. F. McAllister, J. C. Hazzard, and 

C. W. Merriam wrere most helpful in providing information as to the collecting localities and stratigraphy in 

the areas where they mapped.

GEOLOGIC SETTING

In late Mississippian time a moderately shallow epeiric sea occupied much of the west-central and southAl
A2 CONTRIBUTIONS TO PALEONTOLOGY

western parts of what we now know as.the Great Basin 

(fig. 1). A culm facies of grayish-black shale having 

limestone interbeds was deposited in this area, and its 

remnants, broken and deformed by subsequent diastrophism, stretch today from the Confusion Eange in westcentral Utah to the Inyo Range in southeastern California. Like similar Late Mississippian black-shale 

facies in other parts of the world, this habitat was particularly suited to the development of cephalopods, and 

at some scattered localities their fossil remains are found 

in considerable numbers. This paper is concerned with 

the description of the cephalopod fauna that inhabited 

the southwestern part of the area of deposition of the 

culm-facies rocks, the part that extends into the State 

of California. It also records the occurrence of three 

cephalopods of Middle Peiinsylvanian age in the same 

region.

In much of the depositional basin here discussed, it 

has long been customary to refer the culm-facies rocks 

to the White Pine Shale. The White Pine Shale, however, was originally defined by Hague (1883, p. 253, 266, 

267) to include an underlying limestone unit of Early 

Mississippian age and a lower shale of Late Devonian 

age, now known as the Joana Limestone and Pilot Shale, 

respectively. The White Pine Shale also was originally 

defined to underlie the Diamond Peak "Quartzite" now 

called "Formation" (Nolan and others, 1956, p. 60), 

which, at its type locality in the Diamond Range near 

Eureka, Nev., represents rapid deposition of clastic 

rocks during Late Mississippian time. The Diamond 

Peak Formation fingers eastward into the cephalopodbearing culm-facies rocks, and to this date, all cephalopods described from the "White Pine Shale" in eastern 

Nevada and western Utah by various authors (that is, 

Hall and Whitfield, 1877; Miller and Furnish, 1940; 

Miller and others, 1952; and Youngquist, 1949a, b) are 

from beds that are temporal equivalents of the Diamond 

Peak Formation at its type locality.

In recent years, use of the name Chaiiirnan Shale to 

refer to the Late Mississippian predominantly pelitic 

rocks discussed here has become rather widespread. The 

Chainman Shale was originally defined by Spencer 

(1917, p. 27,28) from exposures in the Egan Range near 

Ely, Nev., to include the rocks that lie between the 

Joana Limestone of Early Mississippian age and the 

Ely Limestone of Early Peiinsylvanian age. Subsequent investigations have shown that in much of eastcentral Nevada and west-central Utah the Chainman 

Shale represents roughly the entire span of Late 

Mississippian time.

The relation of Upper Mississippian rocks and the 

units that underline and overlie them in selected Carboniferous sections in Utah and Nevada are shown in

the correlation chart (fig. 2), together with those of the 

California sections that were previously discussed. 

California cephalopod horizons are marked with an 

asterisk (*). The approximate locations of the sections 

in figure 2 are shown in figure 1.

PANAMINT RANGE

The Paiiainint Range stands at the west side of Death 

Valley in Inyo County. Cephalopod-bearing beds of 

Late Mississippian age crop out in the Quartz Spring 

area in the Cot ton wood Mountains at the north end of 

the range. The Quartz Spring area was mapped by 

J. F. McAllister and most of the collections under study 

are those that he made. The presence of Cravenoceras 

in this area was pointed out by McAllister (1952, p. 24) 

in his report.

In the Quartz Spring area the Early Mississippian 

Tin Mountain Limestone is overlain by a sequence of 

varied beds that consists of calcareous siltstone, sandstone, conglomerate and interbedded chert, limestone, 

silty limestone, and siltstone having some shale. These 

constitute the Perdido Formation of McAllister (1952, 

p. 22-25), approximately 610 feet thick in its composite 

type section south of Perdido Canyon and south of Rest 

Spring. The topmost bed of this formation, a darkgray fine-grained limestone, 6 to 12 inches thick, is 

crowded with fossils, mostly Cravenoceras hesperium 

Miller and Furnish. Four to five feet of very soft shale, 

grayish red to purplish gray, separate it from the gray 

locally sandy limestone below that carries productids, 

spirif ers, and other brachiopods. The lower part of the 

Perdido Formation contains an Early Mississippian 

coral fauna.

The Perdido Formation is overlain by the Rest 

Spring Shale (McAllister, 1952, p. 25, 26), which consists mainly of olive-gray to olive-brown siltstone and 

shale but include some thin interbeds of light-gray 

quartzite and poorly sorted intraformational conglomerate. Incompetent, structurally contorted, and poorly 

exposed, the shale is nearly impossible to measure for 

thickness, but McAllister recorded 310 feet at one locality in the nearby Ubehebe Peak quadrangle. The shale 

rests with -apparent conformity on the Perdido Formation. Concretions from the basal part yielded Cravenoceras merriami Youngquist, which is supporting 

evidence for the absence of a hiatus of any consequence 

at its base.

The Upper Mississippian, therefore, is represented 

in the northern part of the Pananiint Range by the 

Perdido Formation and Rest Spring Shale. The lower 

part of the Perdido, however, is Early Mississippian in 

age and the upper part of the Rest Spring Shale may 

be Pennsylvanian in age (McAllister, 1952, p. 24-26).
CALIFORNIA CARBONIFEROUS CEPHALOPODS A3

CONFUSION RANGE,

UTAH

Gordon, Hose, and Repenning 

(1957, p. 1737)

EGAN RANGE,

NEVADA

Spencer

(1917, p. 26-28)

DIAMOND RANGE,

NEVADA

Nolan, Merriam, and Williams 

(1956, p. 54-63)

PANAMINT RANGE, 

CALIFORNIA

McAllister 

(1952, p. 20-27)

INYO RANGE,

CALIFORNIA

Merriam and Hall

(1957, p. 4)

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FIGURE 2. Correlation chart of Upper Mississippian rocks in the Great Basin.

The cephalopods in the following table are from 12 

collections made at 6 localities in the vicinity of Rest 

Spring. The collecting localities are shown on a generalized geologic map of part of the Quartz Spring area 

(fig. 3). With the exception of FL 36C, which is from 

a few feet above the base of the Rest Spring Shale, 

all the collections are from the limestone bed that McAllister took as the top of the Perdido Formation. 

Twelve species are recorded from this bed. The only 

species in the list not found in this bed is Cravenoceras 

merriami Youngquist, which occurs in calcareous to 

ferruginous claystoiie concretions in the basal several 

feet of the overlying Rest Spring Shale. The collection 

from USGS locality 157S3-PC represents approximately a 15-foot sequence of beds, as it includes blocks 

of the Cravenoceras hesperium-vich bed, slabs of 

brachiopod-bearing medium-grained gray limestone 

from another bed about 5 feet lower stratigraphically, 

and weathered-out specimens of C. merriam'i from the 

overlying Rest Spring Shale.

In addition to these collections, an unusually well 

preserved specimen of Rayonnoceras aff. R. solidiforme 

Croneis was provided by C. W. Merriam (USGS loc.

19806-PC). It had been collected by Mr. Lawrence 

Dietz, a prospector, and came from an unknown locality 

in the Cottonwood Mountains, Panamint Range, probably from the vicinity of Rest Spring.

Two specimens of ammonoids also were collected from 

the Pennsylvanian Tihvipah Limestone near Rest 

Spring. McAllister (1952, p. 26, 27) proposed this 

name for a unit of platy light-gray limestone interbedded with shaly limestone and calcareous shale and 

some beds, 1 to 3 feet thick, of fine-grained mediumgray limestone, aggregating about 200 feet in thickness. 

Characteristic spherical concretionary chert nodules, 

0.1 inch to 2 inches in diameter, are scattered through 

the limestone and fusulinids occur in scattered lenses. 

The Tihvipah unconformably overlies the Rest Spring 

Shale at its type locality and fossils indicate that beds 

corresponding to parts of the Lower and Middle Pennsylvariian are represented by the hiatus.

One collection of fusulinids from about a thousand 

feet due east of Rest Spring and 100 feet stratigraphically above the base of the formation was determined by 

Henbest (in McAllister, 1952, p. 26, 27) as representing 

either late Atoka or early Des Moines age, although
A4 CONTRIBUTIONS TO PALEONTOLOGY

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CALIFORNIA CARBONIFEROUS CEPHALOPODS A5

Upper Mississippian cephalopod collecting localities and their fauna 

in the Quartz Spring area

Cephalopod species

Rayonnoceras aff. R. solidiBactrites! cf. B.? carbonarius 

Smith ____________________ 

Mitorthoceras cf. M. perfiloclinatum n. sp

Scyphoceras cf. S. cessator 

(Hall and Whitfield) _______

Hematites'! sp _

Cravenoceras hesperium Miller and Furnish

inyoense n. sp

Eumorphoceras paucinodum n.

q"n

Anthracoceras macallisteri n.

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Delepinoceras californicum n. 

sp

Collection No. 

and locality No. on fig. 3

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early Missouri age must be regarded as a possibility. 

The ammonoid Bisatoceras cf. B. greenei Miller and 

Owen presently identified from USGS locality 19804- 

PC, about 1,500 feet due east of Rest Spring and a few 

feet higher stratigraphically than the fusulinids, is 

very close to if not identical with a Des Moines species. 

The two determinations thus suggest a Middle Pennsylvaiiiaii age for the Tihvipah Limestone.

The other ammonoid from the Tihvipah Limestone 

is an incomplete fragment of a phragmocone of Stenopronoritex sp.; part of the external suture is preserved 

(McAllister loc. FL 5). It was collected in an outlier 

of the limestone about 7,200 feet north by west of Eest 

Spring.

INTO RANGE

The section in the southern part of the Iiiyo Range 

has yielded cephalopods in the Cerro Gordo area in 

Inyo Comity about 20 miles west-southwest of the 

Quartz Spring area. This section, roughly a thousand 

feet of dark-gray silty shale and phyllite, including 

some limestone interbeds, is at least in part Late Mississippian in age; it was called "'White Pine shale" in an 

early report by Kirk (1918, p. 38, 39) and was described briefly by Merriam and Hall (1957, p. 4) who 

referred it to the Chainman Shale. It overlies the Perdido Formation, which in the Cerro Gordo area is only 

50 to 200 feet thick.

Because the Chainman Shale is much thicker than the 

Perdiclo Formation in this area, the Chainman might 

appear to represent a considerable part of Late Mississippian time, as the Chainman Shale does in eastern 

Nevada and western Utah. The present study, however, 

shows that the cephalopods that occur in the lower part 

of the Chainman Shale in the Inyo Range are very Late 

Mississippian in age and are probably younger than 

those at the top of the Perdido Formation in the Quartz 

Spring area. The "Chainman Shale" of the Inyo Range 

appears therefore to be approximately equivalent to the 

Rest Spring Shale of the Panamint Range (fig. 2) and 

represents only a small part of the Chainman Shale of 

eastern Nevada. It also might be in part Pennsylvanian 

in age, like the Rest Spring. Whether the Perdido Formation of the Inyo Range is equivalent in total to that 

of the Panamint Range is not known at present. This 

uncertainty is indicated by questioned hiatuses on the 

correlation chart (fig. 2).

Cephalopods were first noted in the "White Pine 

Shale" of the Inyo Range by Kirk (1918, p. 39) along 

the Cerro Gordo Spring trail, about iy2 miles north 

of the Cerro Gordo mine (USGS loc. 10403-PC). The 

fossils occur in grayish-black slightly altered shale, 

some of them flattened, some as molds, and some as 

partly distorted partly limonitic casts. They were identified by Girty for Kirk, who listed the following cephalopods.

Orthoceras, several species

Oastrioceras aff. G. ricliardsonianuin Girty

Goniatites sp.

Eumorphoceras bisulcatum Girty?

The cephalopods in this collection have been reexamined, along with additional specimens from the same 

locality collected by Merriam and his party (USGS 

Iocs. 15334-PC, 15335-PC) and are now identified as 

follows:

Orthoceracone inclet. 

Bactritcsl cf. B.'! carbonarius Smith? 

Crai^enoceratoides cf. C. nititoides Bisat 

Eumorphoceras bisulcatum Girty

Merriam (oral communication, 1960) stated that the 

cephalopod-bearing beds at this locality are in a stratigraphic position about one-quarter of the way from 

the bottom to the top of the Chainman Shale, which at 

this locality is a little more than 800 feet thick.

Three small lots of fossil cehalopods collected by 

J. F. Mason and now in the Stanford University collection also came from near the Cerro Gordo mine. 

Two lots (23137 and. 23145, SU fossil register) are 

labeled as coming from the Cerro Gordo Spring trail.
A6 CONTRIBUTIONS TO PALEONTOLOGY

These are the species Craven-oceras merriami Youngquist and Eumorphoceras bisulcafum Girty, respectively. The Eutnorphoceras occur in matrix similar 

to that of Kirk's and Merriam's collections and presumably came from approximately the same locality as the 

others. The Crav'enoceras specimens appear to have 

come from a concretion.

One other fossil lot of three specimens is labeled as 

coming from the trail, 2% miles north of the Cerro 

Gordo mine. Three specimens, apparently from a 

dark-gray calcareous concretion, constitute the type 

lot of Doiiibarocanites masonl n. sp.

The fauna of the Chainman Shale of the Inyo Range, 

including Cravenoceras inerriami Youngquist and Cra- 

 venoceratoides cf. C. n-ititoides (Bisat), probably represents a slightly higher horizon than the fauna that has 

abundant Cravenoceras hesperium Miller and Furnish 

at the top of the Perdido formation in the Panamint 

Range. Cravenoceras m\erriami, as noted earlier occurs 

in the Great Basin normally at a higher stratigraphic 

level than C. hexpermm*, though locally the two species 

have been found together in the same bed. The occurrence of C. merriami near the base of the Rest Spring 

Shale in the Panamint Range as well as in the goniatitebearing beds of the Ghainman Shale along the Cerro 

Gordo Spring trail suggests a rough stratigraphical 

equivalence of the two localities. And as these goniatite-bearing beds in the Inyo Range are at a relatively 

low horizon in the Chainman Shale, the correlation of 

most of this unit with the Rest Spring Shale appears 

warranted (fig. 2).

Ora-venoceratoides, described for the first time from 

the Western Hemisphere and illustrated here, has been 

identified by the writer from the upper part of the 

Diamond Peak Formation near Eureka, Nev., as noted 

by Nolan, Merriam, and Williams (1956, p. 61). In 

Great Britain, C. nititoides (Bisat), to which the California species appears to be referrable or is at least 

very closely related, is a very late form occurring in 

the Nuculoceras nucufaim subzone at the top of the 

EumorpJioceras bisidcatum zone of the Lower Namurian. Thus the Inyo Range cephalopods appear to be 

late representatives of the E. ~biaulcatwn assemblage.

PROVIDENCE MOUNTAINS

The Providence Mountains is the name of a small 

north-northeast-trending range in the eastern part of 

the Mojave Desert in San Bernardino County, Calif., 

a few miles southeast of Kelso, a settlement on the Union 

Pacific Railroad. Hazzard (1938, 1954) mapped the 

geology of the northern part of the range, In an abstract (1938, p. 240) he listed, but did not describe, the

units of a 10,000-foot measured section of well-exposed 

Paleozoic rocks in this range. For the 825 feet of rocks 

that is Permsylvanian in age, he introduced the name 

Providence Mountains Limestone but did not elaborate 

on it. Later Hazzard (1954, p. 28) referred the same 

rocks to the lower part of the Bird Spring Formation.

A loose block of moderately dark gray limestone in 

the collection of Stanford University was collected in 

the Providence Mountains by Hazzard and is presumably from the Bird Spring Formation, as it contains 

the imprint of a large ammonoid of Pennslyvanian age 

(SU fossil register 23147). This fossil was listed by 

Hazzard (1954, p. 28) in a table as Gastrioceras cf. G. 

ccmcellat'um. Additional locality data that he has 

kindly provided the writer show that this specimen 

came from the west slope, of the Providence Mountains 

about 1,800 feet southeast of the bottom of Long Canyon, 5,500 feet west of Sheep Spring and 6,700 feet 

north by east of a point where Vulcan Mine Canyon 

joins the road from Kelso to Essex.

This specimen is referred with question to Parcdegoceras teyamim, (Shumard), the closest species with regard to superficial ornament, an ammonoid that occurs 

in rocks of Middle Pennsylvanian (Atoka) age in the 

American midcontinent.

REGISTER OF LOCALITIES

The material studied in preparing this paper came 

from the collections of Stanford University, California, 

and of the U.S. Geological Survey in Washington, D.C. 

The types have been deposited in the Stanford University paleontological type collection and the type collection of the U.S. National Museum. Most of the 

Stanford University collecting localities in the Quartz 

Spring area, Panamint Range, are recorded under McAllister^s field numbers. Abbreviations used in the text 

are SU for Stanford University, USGS for U.S. Geological Survey, and USNM for U.S. National Museum.

STANFORD UNIVERSITY COLLECTIONS

FL 5. Tihvipali Limestone, outlier capping hill, 2,300 ft N. 31° 

 W. of Burro Spring and 7,200 ft N. 9° W. of Rest Spring, 

Cottonwood Mountains, Panamint Range, Inyo County, Calif. 

Collector, J. F. McAllister, July 15, 1937.

FL 15. Perdido Formation, top 10 feet, on top of round hill 

with cliff, forming south side of Bighorn Gap, 4,200 ft N. 58° 

W. of Rest Spring, Cottonwood Mountains, Panamint Range, 

Inyo County, Calif. Collector, J. F. McAllister, Aug. 26, 1937.

FL ISA. Same locality and horizon as FL 15. Collector, J. F. 

McAllister, Sept. 26, 1938.

FL 23. Perdido Formation, top limestone bed. Poor fossils 

from east slope of West Crest, north of Bighorn Gap, about 

5,300 ft N. 61° W. of Burro Spring and 9,000 ft N. 29° W. of
CALIFORNIA CARBONIFEROUS CEPHALOPODS A7

Rest Spring, Cottonwood Mountains, Panamint Range, Inyo 

County, Calif. Collector, J. F. McAllister, Oct. 7, 1938.

FL 27. Perdido Formation, top limestone bed. Blocks of 

fossiliferous limestone in gully on east side of low ridge, 

2,300 ft S. 53° W. of Rest Spring, Cottonwood Mountains, 

Panamint Range, Inyo County, Calif. Collector, J. F. McAllister, Nov. 23,1938.

FL 36A. Perdido Formation, platy limestone just below top 

limestone bed, 2,200 ft S. 29° W. of Rest Spring, Cottonwood 

Mountains, Panamint Range, Inyo County, Calif. Collector, 

J. F. McAllister, Nov. 23,1938.

FL 36B. Perdido Formation, float block from top limestone 

bed. Same locality as FL 36A.

FL 36C. Rest Spring Shale, concretion from basal few feet. 

Same approximate locality as FL 36A.

FL 38. Perdido Formation, top limestone bed, float blocks with 

goniatites on east side of road, a short distance north of 

upper end of narrow gorge through which road passes, about 

2,100 ft S. 3° E. of Rest Spring, Cottonwood Mountains, Panamint Range, Inyo County, Calif. Collector, J. F. McAllister, 

Oct. 29, 1938.

10 E8. Perdido Formation, top limestone bed. Float block 

from same approximate locality as FL 38. Collector, J. F. 

McAllister, Sept. 8, 1938.

SU 2776 (Stanford University locality register). Same locality 

and horizon as FL 38. Float blocks. Collectors, J. F. McAllister and S. W. Muller, July 18,1947.

SU 23137 and 23145 (Stanford University fossil register). 

White Pine Shale (Chainman Shale), Spring Trail, Cerro 

Gordo, Inyo Range, Calif. Collector, J. F. Mason.

SU 23146 (Stanford University fossil register). White Pine 

Shale, 2^4 miles north of Cerro Gordo mine, Inyo Range, 

Calif. Collector, J. F. Mason.

SU 23147 (Hazzard loc. P-1767) Bird Spring Formation. Providence Mountains, Mojave desert, San Bernardino County, 

Calif. Collector, J. C. Hazzard.

U.S. GEOLOGICAL SURVEY COLLECTIONS

10403-PC (field No. C6). White Pine Shale (Chainman Shale), 

Cerro Gordo Spring trail, iy2 miles north of Cerro Gordo 

mine, Inyo Range, Calif. Collector, E. Kirk.

15334-PC (field No. 1-136)'. Chainman Shale, 250-300 ft above 

base. On pipeline trail to Cerro Gordo Spring, iy2 miles 

north of Cerro Gordo mine. Presumably the same locality as 

10403-PC. Collector, C. W. Merriam, Oct. 11, 1946.

15335-PC (field No. 118-G). Same locality and bed as 15334- 

PC. Collector, M. W. Ellis, Oct. 10,1948.

15782-PC (field No. U643). Same locality and horizon as FL 15. 

Collector, R. F. Johnson, Aug. 16, 1949.

15783-PC (field No. U644). Perdido Formation, uppermost 10 

ft and probably lower 5 ft of Rest Spring Shale; 9,000 ft N. 

83%° E. of bench mark 5257 at Quartz Spring, near long 

117°29' W., lat 36°47' N., Cottonwood Mountains, Panamint 

Range, Inyo County, Calif. Collector, J. F. McAllister, 1946.

19804-PC (field No. U377). Tihvipah Formation, upper part, 

above fusulinid bed of collection F-7078. On hill about 1,500 

ft due east of Rest Spring, Cottonwood Mountains, Panamint 

Range, Inyo County, Calif. Collector, E. M. Mac Kevett, 

Nov. 5, 1944.

19806-PC (Merriam loc. 2001). Large orthoconic cephalopod 

from unknown locality and horizon in the Cottonwood Mountains; camped at Gold Belt Spring. Presumably from the

uppermost Perdido Formation, near Rest Spring, Quartz 

Spring area, Panamint Range, Inyo County, Calif. Collector, 

Lawrence Dietz, March 1950.

LATE MISSISSIPPIAN SPECIES

Genus RAYONNOCERAS Croneis, 1926

Rayonnoceras aff. R. solidiforme Croneis

Plate 1, figures 1, 5

Rayonnoceras solidiforme Croneis, 1926, p. 343-350, pi. 1, figs. 

1-4, 6; pi. 2, figs. 4, 5.

Two specimens of Rayonnoceras are considered under 

this taxon. Both are illustrated on plate 1. They are 

believed to represent a species, probably new, but closely 

related to the type species of the genus. Study of 

further material will be necessary to determine the 

limits of this species.

The smaller specimen exposes a natural transverse 

section (pi. 1, fig. 1). It is approximately 30 mm long 

and expands to a width of 27.5 mm at the broad end, at 

a rate of 1 in 9 mm. The siphuncle is subcentral and 

its center is a little more than 14 mm from the slightly 

flattened presumed dorsal margin of the shell. At the 

narrow end, the connecting rings measure 8.9 mm wide 

and 5 mm long, giving a length/width ratio of 0.59. 

The sutures are straight and appear to be inclined shallowly dorsorad. The connecting rings are inclined 

more strongly ventrorad. As seen on the exposed cross 

section, rather thin episeptal and hyposeptal deposits 

coat the septa.

The large specimen is 148 mm long and reaches a 

width of about 124 mm at the wide end. It has been 

sawed longitudinally to expose the ventrodorsal section 

(pi. 1, fig. 5). The camerae are 21 to 22 mm long, about 

5% occurring in the space of one diameter of the conch. 

The depth of the septa, from where they curve into 

the shell margin, is about 40 mm. The shell and septa 

are crushed on one side, presumably the ventral, owing 

to lack of strength due to thinness of the cameral deposits. The shell is constricted at right angles to the 

siphuncle at one place, but this may have occurred after 

burial. The shell material adheres to the phragmocone 

in some places and averages about 1.2 mm thick. The 

surface is smooth.

The siphuncle is iiummuloiclal as in other species of 

this genus, and the rather widely expanded connecting 

rings are vertically grooved on the outside. The siplumcle is partly filled with thick annular deposits and 

between them are rayoiiettes (Croneis, 1926) and an 

irregular endosiphmicle that ranges in width generally 

from 9 to 15 mm but possesses scattered apophyses. It 

is filled with recrystallized light-gray calcite that locally
A8 CONTRIBUTIONS TO PALEONTOLOGY

extends into and around the dark siphuncular deposits 

and even penetrates the rayonnettes at some points. The 

dimensions, in mm, of the siphuncle and septal necks 

are as follows:

Width of septal aperture______________________ 21.0 

Length of connecting ring______________ ____ 20.8 

Width of connecting ring_____________________ 44.5 

Length of septal neck_______________________ 3.0 

Width of septal brim_________________________ 3.2

The length/width ratio of the connecting rings in this 

specimen is 0.46.

Fibrous episeptal and hyposeptal deposits fill most 

of the camerae on the dorsal side, normally being deposited on the septa to depths of 7 mm. The spaces 

between them have been filled with dark-gray calcareous 

mud. On the ventral side the cameral deposits have a 

maximum thickness of about 3 mm but most are about 

2 mm thick.

This species appears to be intermediate between R. 

soUdiforme Croneis and R. vaughanianum (Girty). It 

resembles the former in depth of the camerae, proportions of the mature connecting rings, and the sparseness 

of the cameral deposits on what is presumed to be the 

ventral side. It resembles the latter in its subcentral 

siphuncle. R. solidforme has a rather strongly eccentric 

siphuncle.

Figured specimens: USNM 120614,120615.

Occurrence: Perdido Foundation and basal Rest Spring Shale, 

USGS loos. 15783-PC, 9000 ft. north of Bench Mark 5257 at 

Quartz Spring: Perdido Formation, (?) 19806-PC, unknown locality, probably near Rest Spring ; Cottonwood Mountains, Panamint Range, Inyo County, Calif.

Genus BACTBJTES Sandberger, 1843 

Bactrites? cf. B. carbonarius Smith

Plate 1, figures 10-12 

Bactrites carbonariits Smith, 1903, p. 31, 32, pi. 6, figs. 9-11.

Bactrites ? is represented by several fragments from 

two localities in the Panamint Range. The one figured 

consists of three camerae broken from the narrow end 

of a longer imperfectly preserved slightly compressed 

incomplete phragmocone, which is 70 mm long and consists of 11 camerae. At the apicad end of this fragment 

a single camera is 8.5 mm high, 7.9 mm wide, and 9.0 

mm long (6.1 mm between sutures). The phragmocone 

expands to diameters of 9.1 by 8.6 mm in the space of 

two camerae, a distance of 12.2 mm, or 1 in 24 mm. 

There are 1.5 camerae in a space equal to the dorsoventral diameter, but this proportion varies somewhat as 

some camerae are longer than others. The sutures are 

straight and normal to the shell axis. The siphuncle is 

marginal, tubular, and 0.7 mm wide.

A fragment of a body chamber from locality SU 2776 

shows on one side the poorly preserved smooth shell 

surface and on the other the imprint of wavy transverse 

lirae that ornament the interior of this part of the shell. 

These are approximately at right angles to the shell axis 

at one end but curve diagonally about 20° at the other. 

They appear to form an orad bow, but as the taper of 

the shell is so slight and the preservation leaves something to be desired, it is difficult to distinguish the orad 

from the apicad end of this fragment. One cannot be 

certain, therefore, if the transverse internal lirae form 

a bow or a sinus. A patch of shell adhering to the side 

of another piece of a phragmocone from the same locality shows faint wavy striae. The striated surface apparently represents a layer within the shell itself. The 

striae are inclined dorsorad about 72° to the shell axis.

The proportions of the phragmocone of these shells 

agree in general with those of B.? carbonarius Smith. 

Only two species are known to the writer to possess 

wavy lirae on the inner surface of the body chamber. 

These are B. ? carbonarius Smith and B. ? quadrilineatus Girty. Those of B. 1 carbonarius are approximately 

normal to the shell axis, whereas those of B. ? quadrilineatus are strongly inclined. Our specimens are intermediate in this respect but resemble more strongly those 

of B. ? carbonarius. Diagonal incised striae are also 

preserved in some specimens of B. 1 quadrilineatus on 

the surface of the internal mold of the phragmocone. 

Nothing precisely like these can be seen in the California 

specimens.

Figured specimen: SU 9150.

Occurrence: Perdido Formation, top limestone bed, Iocs. FL 38, 

10 E8, and SU 2776, 2,100 ft S. 3° E. of Rest Spring; FL 15, 

4,200 ft N. 58° W. of Rest Spring, Cottonwood Mountains, 

Panamint Range, Inyo County, Calif.

Genus MITORTHOCEKAS Gordon, 1960

Mitorthoceras cf. M. perfilosum Gordon

Plate 1, figures 2-A

Mitorthoceras perfilosum Gordon, 1960, p. 136, 137, pi. 27, figs.

1-4, 8.

A small orthoconic cephalopod that resembles Mitorthoceras perfilosum is represented by four specimens 

from three localities in the Panamint Range. The shells 

are similar to the type lot of M. perfi.losum but expand a 

little more rapidly with growth. The slightly distorted 

fragmental phragmocone figured on plate 1, figures 2 

and 3, expands about 1 in 8 mm, and the shorter one 

shown in figure 4 on the same plate expands 1 in 7 mm. 

The conch is subcircular in section and 1.9 to 2.2 camerae occur in a space equal to one diameter of the conch. 

The septa are concave orad and shallowly bowl shaped.
CALIFORNIA CARBONIFEROUS CEPHALOPODS A9

The siphuncle is slightly eccentric. Where the diameter of the conch is 5.3 nun the siphuncle is 0.7 mm in 

diameter, and its center is 1.9 mm from what is presumed to be the dorsal margin of the shell (by anology 

with M. elinatum n. sp.). The shell surface is ornamented by prominent raised slightly recurved transverse lirae that have subequal interspaces, of which 12 

to 13 occur in the space of 2 mm. Hyposeptal and episeptal cameral deposits are present and can be seen at 

the weathered orad end of one of the specimens (USGS 

loc. 15783). The paucity and partial distortion of the 

specimens precludes their being sectioned, so description 

and comparison of the internal characters is not 

presently possible.

Figured specimens: SU 9151, 9151A.

Occurrence: Perdido Formation, top limestone bed, SU loc. 

2776 (2 specimens) 2,100 ft S. 3° E. of Rest Spring; USGS Iocs. 

15782-PC, 4,200 ft N. 58° W. of Rest Spring; 15783-PC, 9,000 

ft. N. 83%° E. of bench mark 5257 at Quartz Spring; Cottonwood Mountains, Panamint Range, Inyo County, Calif.

Mitorthoeeras elinatum Gordon, n. sp. 

Plate 1, figures 13-18, 22, 23

Diagnosis. Mitorthoeeras with conch expanding at 

moderate rate; sutures inclined moderately ventrorad; 

siphuncle rather strongly eccentric dorsad; six to nine 

gently sinuous transverse lirae in the space of 1 mm.

Description. This species is represented by several 

fragments of phragmocones from two localities in the 

Panamint Range. The holotype, however, is an exceptionally well preserved fragment of an internal mold 

of two camerae, from the Burbank Hills, Utah. The 

holotype is circular in cross section, has a diameter of 

9.2 mm at the apicad suture, and expands 1 in 9 mm. 

The first camera is 9.3 mm long (6.5 mm between sutures) and 1.5 camerae occur in a space equal to the 

diameter of the conch. The sutures are straight and 

inclined ventrorad 83° to the axis of the conch. The 

surface of the internal mold is polished and shows both 

the ventral furrow (conchial furrow of Flower, 1939) 

as a slightly raised rectilinear thread along the venter 

(pi. 1, fig. 18), and the dorsal furrow (septal furrow 

of Flower, 1939) as an interrupted pair of striae along 

the dorsum (pi. 1, fig. 15). The siphuncle is 1.0 mm in 

diameter in the plane of the apicad septum and its center is 3.3 mm from the dorsal margin of the conch, or 

two-sevenths of the way from the center to the dorsum 

of the conch. The shell is recrystallized internally and 

does not show internal characters. Two small patches 

of shell material adhere to the internal mold and bear 

raised transverse lirae with subequal or slightly narrower interspaces, of which 14 occur in the space of 2 

mm.

The best preserved California paratype is a moderately large specimen of three camerae, 40 mm long, that 

expands at a rate of 1 in 9.3 mm. The inclination of 

the sutures is the same as in the holotype and the cameral 

length proportionally the same. The dorsal furrow can 

be seen, but the ventral one is not preserved.

Other California specimens, mostly of a single 

camera, show variation in surface sculpture from 12 

to 18 lirae in the space of 2 mm. On one of these (SU 

9152A), enough shell material is preserved on the dorsal 

side to show that the transverse lirae are shallowly 

sinuous and form a gentle orad bow over the dorsum.

Comparisons and affinities. Mitorthoeeras elinatum 

can be distinguished from all other known species of 

the genus principally by its moderately inclined sutures 

and relatively long camerae, as well as by the rather 

markedly eccentric siphuncle. The common preservation of the dorsal furrow also appears to be characteristic. The dorsal furrow has not been seen on M. perfilosum, from which the surface shell material is much 

less prone to peel. The holotype was found in a bed 

with Cravenoceras merriami Youngquist and the California paratypes in association with Cravenoceras hesperium Miller and Furnish and thus belong in the same 

broad goniatite zone, the EunwrpJioceras bisulcatum, 

zone.

Holotype: USNM 120616. Paratypes SU 9152, 9152A.

Occurrence: Chainman Shale, upper part, USGS loc. 17024 

PC (holotype), 5 miles east and 1 mile north of the Foote Ranch, 

Confusion Range, Millard County, Utah. Perdido Formation, 

top limestone bed Iocs. SU 2776 (paratypes) and FL 38, 2,100 

ft. S. 3° E. of Rest Spring, Cottonwood Mountains, Panamint 

Range, Inyo County, Calif.

Genus SCYPHOCERAS Ruzhentsev and Shimansky, 1954 

Scyphoceras ef. S. eessator (Hall and Whitfleld)

Plate 1, figures 6-9 

Cyrtoceras cessator Hall and Whitfield, 1877, p. 278, pi. 6, fig. 15.

A rapidly expanding annular nautiloid, which appears to be very slightly cyrtoconic and is represented 

by four fragmental specimens from two Panamint 

Range localities, is referred to Scyphoceras. The 

figured specimen, an incomplete phragmocone of four 

camerae about 16 mm long, is the most rapidly expanding one, averaging 1 in 2.3 mm; other specimens (one 

from the same locality as the figured one) average approximately 1 in 4 mm. The conch is rounded trapezoidal in cross section, becoming squarish with growth; 

the ventral side is a little wider than the dorsal. The 

figured specimen is 13.4 mm high and 13.6 mm wide at 

the annulation near the orad end. Annulations are 

spaced 3.5 mm apart and are inclined very slightly dor70r -592 O-64 2
A10 CONTRIBUTIONS TO PALEONTOLOGY

sorad; they are slightly sinuous. Septa are bowl 

shaped, of moderate concavity, and spaced 3.1 mm apart. 

The sutures are nearly straight and approximately at 

right angles to the shell axis. About 3% camerae occur 

in a space equal to the mean dorsoventral diameter of 

the conch. The shell surface is covered with fine 

threadlike lirae that are irregularly spaced but tend 

to be bunched over the annuli; 18 to 20 occur normally 

between crests of annuli, but locally there are more. 

The transverse lirae have approximately the same configuration as the annuli.

The siphuncle is located close to the margin. In 

the plane of the apicad septum, where the dorsoventral 

diameter is 9.2 mm, the siphuncle is 0.7 mm wide and its 

center is 2.1 mm from the margin. On the septum at 

the wide end, it is 1.1 mm wide and its center is 2.7 mm 

from the margin. The shape of the connecting rings 

and the nature of the siphnncular and cameral deposits 

have not been determined.

This shell is closely related to and perhaps identical 

with Cyrtoceras cessator Hall and Whitfield described 

from the White Pine Shale (Chainman Shale) in central Nevada, and appears to belong in Scyphoceras. 

The rate of expansion of the conch of 8. cessator is 1 

in 3 mm, which falls well within the range of the California specimens, and the spacing of the annuli is the 

same. The septa are reportedly a little more widely 

spaced in the holotype of S. cessator than in the California shells, but for the present it seems best to consider that the range of variation in 8. cessator includes 

these California specimens.

Figured specimen: SU 9153.

Occurrence: Perdido Formation, top limestone bed, Iocs. 

SU 2776 and FL 38, 2,100 ft S. 3° E. of Rest Spring, Cottonwood 

Mountains, Panamint Range, Inyo County, Calif.

Genus LIROCEHAS Teichert, 1940 

Liroceras? sp.

Plate 2, figures 1-4

A single coiled iiautiloid consisting only of the first 

volution of the phragmocone with parts of the shell of 

the second volution adhering to it is referred here questionably to Liroceras. It expands rapidly about 1 in 

3.5 mm measured along the lateral zones and by the end 

of the first volution is depressed elliptical in cross section; the greatest diameter is near the middle of the 

whorl. The conch is perforate, the perforation with a 

diameter of 3 mm. Surface ornament consists of strong 

raised longitudinal subequally spaced cords with wider 

interspaces, of which about 15 occur over the venter 

between the rounded lateral zones. They are crossed 

by somewhat wavy transverse lirae that swing apicad

on the umbilical slope to cross the lateral zones. Where 

the shell is missing, the cords can be seen faintly expressed on the surface of the internal mold. The center 

of the venter in the initial part of the phragmocone is 

occupied by a faint shallow longitudinal depression in 

which two additional cords are intercalated between 

the others at either side of the central one. This depression and the subsidiary cords die out within threequarters of the beginning of the volution.

Part of the umbilical w^all of the succeeding volution 

can be seen at one side and bears four longitudinal cords 

crossed by nearly straight transverse lirae. The cords 

die out at the end of the first third of the second volution, indicating that the shell is nearly smooth in its 

mature stages. The sutures are nearly straight across 

the venter. Nineteen camerae compose the first volution.

The dimensions of the shell, in mm, are as follows: 

diameter (D) 16.0; height of last whorl (H) 7.0; width 

of last whorl (W) 10.8; and width of umbilicus (U) 

7.8. These give the following proportions: U/D=0.49, 

W/D-0.68, and W/H= 1.55.

It is difficult to determine what an adolescent specimen like this will become with growth, but the most 

mature part appears to resemble Liroceras more closely 

than any other genus.

Figured specimen: SU 9154.

Occurrence: Perdido Formation, top limestone bed, loc. FL 38, 

2,100 ft S. 3° E. of Rest Spring, Cottonwood Mountains, Panamint Range, Inyo County, Calif.

Genus HEMATITES Flower and Gordon, 1959

Hematites? sp. 

Plate 1, figures 19-21

A small fragment of a phragmocone of bactritid aspect is considered under this taxon. It was mentioned 

by Flower and Gordon (1959, p. 835) in their discussion 

of Mississippian belemnoid phragmocones. It is 7 mm 

long and exposes four septa. The cross section is subcircular, slightly compressed, measuring 6 by 7 mm at 

the adoral end and expanding 1 in 4.9 mm. The septa 

are shallowly bowl shaped, 1.7 mm deep, and are spaced 

1.4 mm apart; 4% camerae occur in the space of one 

dorsoventral diameter of the conch. The sutures appear to lack lateral lobes but slope gently dorsorad. 

The siphuncle is marginal but cannot be clearly discerned on the specimen.

This fragment is somewhat similar to Bactritesl 

nevadensis Youngquist but is a little more broadly 

rounded in cross section, has very slightly more closely 

spaced septa, and is slightly more rapidly expanding. 

As Flower and Gordon pointed out, its phragmocone
CALIFORNIA CARBONIFEROUS CEPHALOPODS All

has most of the features typical of their belemnoid genus 

Hematites. It is devoid of rostral material, and though 

some shell material is found on the phragmocone wall, 

this has a smooth faintly granular surface. One cannot tell, therefore, whether this shell belongs with the 

bactritids or the belemnoids, though its closely spaced 

gently sloping sutures indicate that it is not part of the 

normal Late Paleozoic bactritid line typified by Bactrites 1* carbonwrms Smith.

Figured specimen: SU 9155.

Occurrence: Perdido Formation, top limestone bed, loc. SU 

2776, 2,100 ft S. 3° E. at Rest Spring, Cottonwood Mountains, 

Panamint Range, Inyo County, Calif.

Genus CRAVENOCERAS Bisat, 1928 

Cravenoceras hesperium Miller and Furnish 

Plate 3, figures 3-5, 14-17, 21-33; text figures 4A, D, E

Cravenoceras hesperium Miller and Furnish, 1940, p. 374, 375,

pi. 49 figs. 1-8, text figs. 15B, 16B. 

[part] Youngquist, 1949a, p. 291, pi. 59, figs. 4-11, 14-16;

pi. 60, figs. 1, 2, 8-15; pi. 61, figs. 1-3; pi. 62, figs. 1-6,

16-18 [not pi. 59, figs. 12, 13; pi. 61, figs. 10-12] ; text

fig. IB ; 1949b, p. 613, 614, pi. 100, figs. 1-7. 

Cravenoceras nevadense [part] Ycungquist, 1949a, p. 295, 296,

pi. 58, figs. 7-11; pi. 59, figs. 1, 17, 18; pi. 60, figs. 3, 4( ?) ;

pi. 62, figs 11-15; pi. 64, figs. 13-16 [not pi. 59, figs. 2, 3].

This species is by far the most common fossil in the 

limestone bed that marks the top of the Perdido Formation in the Panamint Range. It exhibits a considerable 

range of variation in shape, shown in the scatter diagrams (figs. 5 and 6) along with variation in G. inyoense 

n. sp. Two forms are recognizable, a typical rather 

involute relatively narrow form and a broader less involute one. These two forms are recognized also in 

other parts of the Great Basin region, in Nevada and 

Utah. Although there is a tendency toward intergradation, they do not appear to merge completely. Although only one or the other form is represented in 

some of our collections, this may be due to the accident 

of haphazard collecting, incomplete exposure of the 

containing beds, or of thanatocoenosis. The reason for 

the presence of two distinct forms is not certain at 

present, but the most obvious explanation that comes 

to mind is sexual dimorphism. These forms do not 

appear to represent distinct species, as the pattern of 

ornament is the same and the;y occur together at many 

localities.

The typical form is shown on plate 3, figures 21-33. 

This agrees in general shape and degree of involution 

with the type lot from the Chairman Shale in the Egan 

Range, Nev. (Miller and Furnish, 1940, p. 374, pi. 49, 

figs. 1-8). The original lot consists of 6 figured

(USNM 98935) and 22 unfigured (USNM 98934) syntypes. The large specimen illustrated by Miller and 

Furnish (1940) on plate 49, figure 1, is hereby designated the lectotype (USNM 120617) and the rest paralectotypes. Cross sections of a paralectotype (USNM 

98934) are shown in figure 4J., D.

The specimen shown on plate 3, figures 24-26, belongs 

with the typical form but is more loosely coiled than 

normal so that the width of its umbilicus is equal to a 

little more than one-third the diameter of the conch. 

Looser coiling is a common character in late mature 

and gerontic shells of Cravenoceras. It is particularly 

characteristic of Cravenoceras Jcingi (Hall and Whitfield), which is probably an ancestor of C. hesperiwn. 

Some shells at the same diameter as the one shown on 

plate 3, figures 24-26, however, still retain the tighter 

coiling of the typical early mature conch.

The characteristic transverse sculpture of Cravenoceras is particularly well developed on some of the California specimens, as for example those illustrated on 

plate 3, figures 21-23, 30-33. In early maturity, the 

shinglelike transverse lamellae form a prominent broad 

arch across the venter, bowing markedly orad. Over 

the ventrolateral shoulders is a correspondingly prominent though narrower sinus and on the flanks near the 

umbilical area a small gentle orad bow. The umbilical 

shoulder is marked by a single raised spiral cord on top 

of the transverse lamellae. Internal varices are developed, generally about four to a volution and have approximately the same configuration as the transverse 

lamellae. At maturity the ventral orad bow of the 

transverse sculpture becomes flattened in the center, and 

in some specimens a faint ventral sinus is developed.

The suture of the typical form of C. hesperium, as 

illustrated by Miller and Furnish (1940, text fig. 15B) 

and by Youngquist (1949a, text fig. IB), needs a very 

slight modification. It has a relatively narrow ventral 

lobe shallowly divided by a subtriangular median saddle 

into two narrow pointed prongs. The sides of the ventral lobe are shown as straight and subparallel in the 

illustrations cited. Actually they are gently sigmoidal, 

bulged slightly apicad, and pinched in orad. This part 

of the suture is difficult to see in the specimen used for 

its illustration by Miller and Furnish, but the slightly 

sigmodial shape of the side of the ventral lobe can be 

made out on close inspection. This character is well 

shown on many of the California specimens and the 

suture of one of them is illustrated in figure 4E. The 

first lateral lobe is fairly broad, with convex sides, and 

is pointed.
A12 CONTRIBUTIONS TO PALEONTOLOGY

D

FIGURE 4. Cravenoceras cross sections and sutures. A, D, E, Cravenoceras hesperium Miller and Furnish, 

cross section of a paralectotype (USNM 98934) X 1% and X 5, respectively; suture of a California specimen (SU 9156) X 3 at a whorl height of 9.5 mm. B, C, Cravenoceras merriami Youngquist, external sutures of an Inyo Range specimen (SU 9161) X 3, at a whorl height of approximately 10 mm; of a 

Panamint Range specimen (USNM 120619) X 3, at a diameter of 18.5 mm and whorl height of 10 mm. 

F, Q-, Cravenoceras Inyoense n. sp., external suture of the holotype, X 2, at a diameter of 33 mm and 

whorl height of 13.5 mm; suture of a paratype (SU 9158) at a whorl height of 4.2 mm.

The dimensions and proportions of the typical form 

are given in the following table. All come from SU 

locality 2776.

Dimensions and proportions

Diameter (D).. _ mm

Height of last whorl (H) do

Width of last whorl (W) __ do__ _ Width of umbilicus (U) do_

U/D

W/D____ _ W/H _ .

A

38.7 

14. 7 

26. 0 

13. 4 

.35 

. 67 

1. 77

B

29. 2 

13. 7 

20.4 

6. 4 

. 22 

. 70 

1. 49

C

19. 7 

9. 0 

14. 4 

5.3 

. 27 

. 73 

1. 60

D

13. 0 

5. 4 

10. 8 

3. 4 

. 26 

. 83 

2. 00

B

3. 3 

1. 2 

2. 2 

2. 0

. 60 

. 67 

1. 83

Dimensions and proportions

Diameter (D) _ .mm

Height of last whorl (H)__do

Width of last whorl (W)__do_ - _ _

U/D______-______-_---------

W/D _ __- ---

W/H_____-___ _______________

A

29.8 

11. 3 

23. 7 

11.0 

.37 

. 80 

2. 10

B

17.5 

5. 5

1 14. 4 

8.3 

.47 

.82 

2. 62

C

11. 4 

4. 2 

9. 6 

5. 7 

. 50 

.84 

2. 29

D

10. 8 

4.0 

8.9 

4. 5 

. 41 

. 82 

2. 23

B

9. 6 

3.6 

2 8. 6 

3. 7 

.40 

. 91 

2. 29

i Twice the half width. 

2 Adjusted for slight distortion.

The wide form has a broader venter and less elevated

The wide form is illustrated on plate 3, figures 3-5. 

Other individuals have been described and illustrated 

as Cmvenoceras nevadense Miller and Furnish by 

Youngquist (1949a, p. 295, 296, pi. 58, figs. 7-11; pi. 59, 

figs. 1, 17, 18; pi. 60, figs. 3, 4?; pi. 62, figs. 11-15; pi. 

64, figs. 13-16) and also as 0. hesperium (Youngquist, 

1949b, p. 613, 614, pi. 100, figs. 4-7).

The dimensions and proportions of several specimens 

of the wider form are given in the following table. 

Data from these and other specimens are plotted in the 

scatter diagrams (figs. 5, 6) where they are compared 

with those of the typical form and of C. inyoense n. sp.

 - - - */ JL / < > **

spherical throughout much of its growth. The umbilicus is wider than in the typical form, averaging about 

two-fifths of the diameter of the conch in early maturity. The transverse striae and internal varices bow 

orad across the venter as in the typical form, but the 

arching is shallower and the sinuosity more subdued. 

The spiral cord along the umbilical shoulder is present 

in these shells but is easily lost when the shell is broken 

free from the enclosing rock. The suture shows no appreciable difference from that of the typical form.

Comparisons and affinities. C. hesperium is probably most closely related to the earlier species C. Jcingi
CALIFORNIA CARBONIFEROUS CEPHALOPODS A13

35« 

30

25

20

a:

UJ

ti 15

10

o A

O

D

O

A

O

D

O

o o 

o

o 

o 

QD

n

o

n

n

n

A A 

A

A'

A

O

D

cP°

O 

O

O

n°

n

A

D

A

A

A

O Cravenoceras hesperium, typical form

D Cravenoceras hesperium, widely umbilicate form

A Cravenoceras inyoense n. sp.

10

WIDTH OF UMBILICUS, IN MILLIMETERS

15 20

FIGURE 5. Scatter diagram showing relative Involution of the conch (diameter/width of umbilicus ratio) for California specimens of

Cravenoceras from a single bed.

(Hall and Whitfield), which is similarly ornamented 

by a single cord along the umbilical shoulder and which 

differs principally in the much greater evolution of the 

mature conch. Young shells of C. Mngi resemble those 

of the broader, more evolute form of C. hesperium, but 

well preserved ones possess fine longitudinal lirae over 

the surface of the shell that die out in early maturity; 

these are absent in C. hesperium.

C. neradense Miller and Furnish, as was noted 

earlier, has been confused by some authors with thewider, more evolute form of G. hesperium. It is, however, a distinct species. Its early mature shell is narrower than that of C. hesperium and the umbilical 

shoulder is ornamented by four or five fine spiral lirae,

instead of a single cord as in G. hesperium. The writer 

has not seen any shells other than the type lot that he 

would identify as C. nevadense.

G. merriami Youngquist likewise is a distinct species 

and occurs generally a little higher stratigraphically 

than C. hesperium, although the two species are associated at the type locality of the former. Though 

strongly involute and thus resembling extreme examples 

of the typical form of G. hesperium, it lacks any sort of 

spiral ornament in the region of the umbilical shoulder 

and its suture has a slightly wider ventral lobe that becomes more deeply divided at maturity than that of G. 

hesperium. Differences of G. hesperium from C. inyon. sp. are given in the discussion of that species.
A14 CONTRIBUTIONS TO PALEONTOLOGY

351 

30

25

-t 20

15

10

o

O A

O

D 

O O

o 5b0

OA A

D

CD'

A " ( 

CP °

o Cravenoceras hesperium, typical form

n Cravenoceras hesperium, widely umbilicate form

A Cravenoceras inyoense n. sp.

10 15 

WIDTH OF LAST WHORL, IN MILLIMETERS

20 25

FIGURE 6. Scatter diagram showing relative width of conch (diameter/width ratio) for California specimens of Cravenoceras from a

single bed.

Hypotypes: SU 9156, USNM 120617.

Occurrence: Perdido Formation, top limestone bed. Iocs. FL 38, 

10 E8, and SU 2776, 2,100 ft S. 3° E. of Rest Spring; FL 15 and 

USGS loc. 15782-PC, 4,200 ft N. 58° W. of Rest Spring; FL 27, 

2,300 ft S. 53° W. of Rest Spring; FL 36A, B, 2,200 ft S. 29° W. 

of Rest Spring; and USGS loc. 15783-PC, 9,000 ft N. 83° E. of 

bench mark 5257 at Quartz Spring; Cottonwood Mountains, 

Panamint Range, Inyo County, Calif.

Cravenoceras inyoense Gordon, n. sp.

Plate 2, figures 5, 6; plate 3, figures 1, 2, 6-13, 18-20; text 

figures 4 F, G

Diagnosis. Exceedingly evolute Oraven-ocera^s lacking longitudinal ornament on umbilical shoulder.

Description. This species is based on 38 specimens 

from 2 localities in the same general area. The holotype 

is an internal mold of a phragmocone nearly 34 mm in 

diameter. Only small patches of the shell are preserved, but surface sculpture is well preserved on several of the paratypes, which also show characters of the 

adolescent conch. These features are particularly well 

exhibited on the specimens figured on plate 3, figures 

6-13. The conch is subglobose to broadly thick discoidal; the venter is broadly rounded and merges imperceptibly with the flanks. The umbilical shoulder is 

subangular.

The protoconch and the early part of the first postnuclear whorl, as seen in the best preserved paratype, 

are broader than the second postnuclear whorl; the 

whorl narrows markedly in the latter half of the first 

volution. The conch is coiled planorbitally for four to 

five volutions, remaining subdiscoidal in shape, and then 

the whorl begins to broaden more rapidly, and the sides 

of the umbilicus begin to steepen. By the eighth volution the conch is barrel shaped and subspherical. The 

surface sculpture at this stage consists of transverse 

striae that form a very shallow moderately narrow 

ventral sinus, flanked by faint, shallow broad rounded 

orad bows. Outside of these, near the lateral zone are 

slightly more prominent lateral sinuses. The transverse striae swing rather strongly orad to cross the subangular lateral zone that can be said also to constitute 

the umbilical shoulder. They continue on to the umbilical wall, where they are approximately radial. The
CALIFORNIA CARBONIFEROUS CEPHALOPODS A15

umbilical wall and shoulder in these immature shells is 

also ornamented by a few small scattered rounded nodelike swellings, 3 to 10 to a whorl but difficult to count 

owing to nonuniformity of their development. Some 

of the more prominent ones are adjacent to transverse 

constrictions of growth.

The growth constrictions are generally more strongly 

developed in shells more than 10 mm in diameter and are 

roughly parallel to the transverse striae. They are weak 

or absent on the umbilical shoulder. On the holotype 

they are spaced three to four to a volution.

In shells more than 15 mm in diameter, the umbilicus 

becomes stepped; this occurs in the last 41/4 volutions 

of the holotype. The typical straplike transverse 

lamellae of Cravenoceras, each bounded by a stria on 

the adoral edge, are well developed in the adult phragmocone and preserve in a subdued manner the ventral 

and lateral sinuses and intervening bows of the adolescent conch. In some specimens the ventral sinus is not 

apparent.

The suture (fig. 4F, G-} is like that of Cravenoceras 

hesperium, having a moderately narrow ventral lobe 

with gently convex sides, divided to almost half its 

length into two hastate prongs by an inverted gobletshaped median saddle. The first lateral saddle is slightly narrower than the ventral lobe, asymmetrically 

roimded-spatulate in shape. The first lateral lobe is 

about the same width as the first lateral saddle, acuminate, slightly constricted orad. The second lateral saddle arches asymmetrically across the umbilical shoulder 

to the moderately short narrowly pointed umbilical 

lobe. The internal suture consists of three hastate, 

sharply pointed lobes separated from each other by 

fairly narrow rounded saddles and from the umbilical 

lobes by broader asymmetrically rounded saddles. 

Twenty sutures occur on the final volution of the holotype, which does not appear to represent a complete 

phragmocone, as there is no tendency for the last several 

sutures to be spaced closer together. Another paratype 

(USNM 120618), a phragmocone partly distorted by 

crushing, which probably reaches a diameter about 5 

mm greater than the holotype, does show crowding of 

the septa at the orad end and represents a nearly 

complete phragmocone.

Comparisons and affinities. Cravenoceras inyoense is 

the most evolute species of this genus found in the 

American Carboniferous. It recalls the earlier species 

C. scotti Miller and Youngquist, but that species has 

fine spiral lirae ornamenting the umbilical region, a 

character shared with C. nevadense Miller and Furnish 

and is less evolute than C. inyoense. It also recalls C. 

kingi (Hall), another earlier evolute form, but that

709-592 O-64 3

Dimensions and proportions 

f Holotype A and para types B, C, E, and F are from SU loc. 2776. Paratype D is from McAllister loc. FL 38]

Diameter (D) ________ mm_ _ 

Height of last whorl (H)____ 

do_.__ 

Width of last whorl (W) 

do_.__ 

Width of umbilicus (U) 

do____ 

U/D

W/D__. __________________

W/H_____________________

A

33. 7 

10. 6 

23. 0

17. 8 

. 53 

. 68 

2. 17

B

25. 0 

9. 3 

19. 8

13. 0 

. 52

.79 

2. 11

C

14. 8

4. 7 

10. 2

8.9 

. 60 

. 69 

2. 17

D

10. 8 

3. 2 

8. 0

6. 4 

. 60 

. 74 

2. 50

E

9. 7 

3. 0 

7. 2

5. 9 

. 61

. 74 

2. 40

F

5. 2 

1. 3 

2. 5

4.0

. 77 

. 48 

1. 92

species differs in its much less evolute early stages, its 

strong spiral cord along the umbilical shoulder, and 

its having nne longitudinal lirae in young shells, a 

character it shares with C. leion Bisat.

C. inyoense is easily distinguished from C. hesperium 

with which it occurs by its much wider umbilicus and 

lack of a spiral cord along the umbilical shoulder and, 

in young stages, by the absence of a strong orad bow of 

the transveres sculpture over the venter, as well as by 

its planorbital coiling and subdiscoidal shape (on pi. 

3 compare figs. 18-20 with 27-29). Comparison of the 

shape of the conch and width of the umbilicus of the 

two species is shown graphically in figures 5 and 6.

Primary types: Holotype SU 9157. Paratypes SU 9158- 

9158D, 9159, 9160, USNM 120618, 143889.

Occurrence: Perdido Formation, top limestone bed, Iocs. FL 

38 (10 specimens), 10 E8 (7 specimens), and SU 2776 (20 specimens), 2,100 ft S. 3° E. of Rest Spring; loc. FL 36B (1 specimen) 2,200 ft S. 29° W. of Rest Spring; USGS loc. 15783-PC 

(3 specimens) 9,000 ft N. 83° E. of bench mark 5257 at Quartz 

Spring; Cottonwood Mountains, Panamint Range, Inyo County, 

Calif.

Cravenoceras merriami Youngquist 

Plate 2, figures 11, 12 ; text figure 4 B, 0

Cravenoceras hesperium [part] Youngquist, 1949, Jour. Paleontology, v. 23, no. 3, p. 291, pi. 59, figs. 12, 13; pi. 61, figs. 

10-12 [not pi. 59, figs. 4-11, 14-16; pi. 60, figs. 1, 2, 8-15; 

pi. 61, figs. 1-3; pi. 62, figs. 1-6, 16-18; text fig. 1 B].

Cravenoceras merriami Youngquist, 1949, Jour. Paleontology, 

v. 23, no. 3, p. 291-295, pi. 61, figs. 4-7; pi. 63, figs. 9-12; 

text figs. 1 C, D.

This species commonly has a subglobose shape in early 

maturity and becomes thick discoidal with growth. 

Characteristic features are: strong involution, lack of 

longitudinal sculpture in the umbilical region, and 

transverse cravenoceratid lamellae that are fairly 

straight across adolescent and immature shells and 

gradually deepen with growth to form a shallow sinus 

over the venter in mature shells. On the largest of 

three shells from the Best Spring Shale (loc. FL 38C),
A16 CONTRIBUTIONS TO PALEONTOLOGY

a constriction on the outer volution shows such a sinus 

well developed over the venter.

Characteristic also of this species is the external suture, which has been figured by Youngquist, (1949, text 

figs. 1C, D). Sutures, two of which are illustrated here 

(figs. 45, (7), are exposed in some of the California 

specimens. The ventral lobe is rather broad and its 

prongs are more inflated, that is, wider than in G. hesperium. The ventral lobe of G. hesperium normally has 

the sides slightly convex apicad and pinched in orad. 

The ventral lobe of C. merriami has rather straight 

sides, never pinched in orad. This results in the first 

lateral saddle of G. merriami having a more open appearance than that of G. hesperium. The width of the 

first lateral lobe has about the same range of variation 

in both species and cannot be used to distinguish them.

Dimensions and proportions of four California specimens from the Quartz Spring area, Panamint Range, 

are given as follows:

Dimensions and proportions

Width of last whorl (W)_ _ _ do_

U/D______________ ___________ _____

W/D_ ____________________________

W/H_ ____________________________

A

37. 4

21. 0

J24. 5

5. 2

. 14

. 66

1. 17

B

32. 6

16. 4

21. 6

4. 7

. 14

.66

1.32

C

22. 2

10. 0

16. 9

23.0

. 14

. 76

1.69

D

21. 8

10. 0

16. 8

3.0

. 14

. 77

1. 68

1 Estimated.

2 Approximate.

Comparisons and affinities. -In general shape of the 

conch and in the lack of spiral ornament on the umbilical region, G. merriami is close to G. richardsonianum 

(Girty), an American midcontinent species. Its main 

differences from G. richardsonianum are the spherical 

to subspherical shape of young shells of three or four 

volutions in contrast to the discoidal to subsidcoidal 

shape of shells of this size of G. richardsonianum and 

the ventral lobe of the adult suture that develops much 

longer prongs than that of G. richardsonianum.

G. merriami can be confused with involute specimens 

of G. hesperium. How the two are distinguished by 

suture characters has already been discussed. In addition, the shell of G. hesperium is less involute, its transverse elements of ornament do not form a well-defined 

ventral sinus but bow strongly orad in immaturity and 

early maturity and also form lateral sinuses; and, most 

important, a spiral cord is present at the umbilical 

shoulder in C. hesperium.

Both species occur in the same bed at the type locality 

of G. merriami, but studies by the writer and by R. K. 

Hose in the Confusion Range of western Utah have 

shown that they commonly occupy separate parts of the

section, and C. merriami is stratigraphically above G. 

hesperium. This relation is borne out by the specimens 

of G. merriami from McAllister locality FL 36C that 

occur slightly higher stratigraphically than the beds 

having abundant G. hesperium. Whether the two species occur in the same bed at USGS locality 15783-PC is 

open to question as all of the specimens of G. merriami 

show areas of caliche indicating that they were picked 

up loose and thus could have come from the Rest Spring 

Shale. Moreover, they do not have chunks of dark-gray 

limestone matrix adhering to them as do most of the 

specimens of C. hesperium in the same collection.

Figured specimens: SU 9161, USNM 120619.

Occurrence: Base of Rest Spring Shale or top of Perdido Formation USGS loc. 15783-PC (4 specimens) 9,000 ft N. 83y2 ° E. of 

bench mark 5257 at Quartz Spring; Cottonwood Mountains, 

Panamint Range. Rest Spring Shale, concretions in the lower 

few feet, loc. FL 36C (3 specimens) about 2.200 ft S. 29° W. of 

Rest Spring, Cottonwood Mountains, Panamint Range, Inyo 

County, Calif. Chainman Shale, SU 23137 (Stanford University 

fossil register) (2 specimens) Spring Trail, Cerro Gordo, Inyo 

Range, Calif.

Genus CRAVENOCERATOIDES Hudson, 1941

Cravenoceratoides cf. C. nititoides (Bisat)

Plate 4, figures 18-23

Cravenoceras nititoides Bisat, 1932, p. 35, pi. 2, fig. 2. 

Cravenoceratoides nititoides Hudson, 1941, p. 282.

The most common cephalopod in the Chainman Shale 

in the Cerro Gordo area of the Inyo Range is a form 

originally identified by Girty in a fossil list published 

by Kirk (1918, p. 39) as Gastrioceras aff. G. richardsonianmn Girty. It is represented largely by fragmental remains of shells flattened on surfaces of the grayish-black slightly altered shale. Young individuals, 

however, occur fairly commonly as partly distorted 

party limonitic casts in the shale, locally weathered out 

in part to leave molds. This form is extremely close 

to, if not identical with, Gravenaceratoides nititoides 

(Bisat) originally described from the Arnsbergian 

(Lower Sabdenian) stage of Pace Gate Beck, Blubberhouse Moore, Yorkshire, England. Enough specimens 

are preserved to permit the following description of 

the California form.

The conch is subspherical and moderately evolute in 

young shells, rapidly becoming involute and developing somewhat wide flanks with growth. In early maturity the conch has a rather well rounded venter that 

merges into the more gently rounded flanks and rather 

sharply rounded umbilical shoulders. The diameter of 

the umbilicus of a specimen with a conch diameter of 

a little more than 4 mm (pi. 4, figs. 18-20) is nearly 

two-fifths that of the conch. In another specimen at a 

conch diameter of 13 mm (pi. 4, figs. 22, 23) it is be-
CALIFORNIA CARBONIFEROUS CEPHALOPODS A17

tween one-sixth and one-seventh that of the conch. A 

crushed and distorted example, flattened to a diameter 

of 39 mm is shown on plate 4, figure 21. Fragments of 

other shells show that the diameter of some specimens 

exceeds 60 mm.

The surface of the conch bears rather strong transverse lirae, most of which bifurcate on the flanks near 

the umbilical shoulders, though locally a single cord 

crosses without bifurcation. These lirae in young and 

immature shells form a broad orad bow across the whorl 

over the venter, but in more mature specimens the forward swing of the transverse lirae near the umbilical 

shoulder is taken up in a lateral bow orad outside of 

which the lirae extend across the venter in a nearly 

straight line. In young shells the lirae are moderately 

sharp and elevated, with slightly wider interspaces. 

In mature shells the lirae are flattened into gently canted 

lamellae, slightly raised along the orad edge and separated by narrow grooves.

The suture is not known. The specimens are too 

crushed for specimens to be determined, except for 

those less than 5 mm in diameter.

The holotype of Cra/venoceratoides nititoides, a specimen likewise crushed in shale, has been figured by Bisat 

(1932, pi. 2, fig. 2) and by Hudson (1946, pi. 21, fig. 8). 

It agrees with the California shells in its small umbilicus and asymmetrical (canted) lirae in the adult, 

which are protractive at the umbilical shoulder but 

curve back gently and cross the venter in a nearly 

straight line. In the absence of English specimens for 

comparison, as well as of better preserved California 

material, it seems best for the present merely to point 

out the general agreement of the California shells with 

the British species.

Figured, specimens: USNM 120620, 120621.

Occurrence: Chainman Shale, USGS Iocs. 10403-PC, 15334- 

PC, 15335-PC, Cerro Gordo Spring trail, about 1% miles north 

of Cerro Gordo mine, Inyo Range, Inyo County, Calif.

Genus EUMORPHOCERAS Girty, 1909

Eumorphoceras bisulcatum Girty

Plate 2, figures 13, 14

Eumorphoceras bisulcatum Girty [part], 1909, p. 68-70, pi. 11,

figs. 15, 17-19a [not figs. 16-16b]. 

Bisat [part], 1924. p. 97, 98, pi. 6, fig. 5 [? not pi. 6, figs.

1-4, pi. 10, fig. 12].

Schmidt, 1925, p. 584, 585, pi. 22, fig. 5, pi. 25, figs. 2, 3. 

[part], 1929, in Gtirich, p. 70, 71, pi. 19, fig. 5 [not fig. 6]. 

Delepine, 1930, in Dorlodot and Delepine, p. 57, 58, pi. 1.

figs. 1-5.

Mailleux, 1933, pi. 10, fig. 139. 

Schmidt, 1933, p. 455, text fig. 12. 

Delepine, 1985, p. 184, 185, pi. 8, figs. 5, 6. 

Demanet, 1936, pi. 2 fig. 5. 

Plumnier and Scott [parti, 1937, p. 175, 176 [not pi. 38, figs.

4-7, text fig. 37].

Demanet and Van Straelen, 1938, in Renier and others, p.

175, pi. 130, figs. 6-9. 

Demanet, 1941, p. 137, 138, pi. 5, fig. 15. 

Delepine, 1941, p. 79. 

Shinier and Shrock [parti, 1944, p. 571, [not pi. 233, figs.

16-18].

E. W. J. Moore [part], 1946, p. 430, 431, 433, pi. 22, fig. 3, pi. 

23 fig. 7, pi. 25, figs. 5a-d, text fig. 29 [not pi. 27, figs. 

1, 2, text fig. 5]. 

R. C. Moore, 1948, p. 399, fig. 17. 

Miller and Youngquist [part?], 1948, p. 622-225 [not p. 100,

figs. 9-17, text fig. 2B1.

Youngquist, 1949a, p. 299-301, pi. 58, figs. 4, 5. 

Elias, 1956, pi. 6, fig. 6. 

'iPericucltts impressus Koninck [part] Hind, 1918, p. 449, pi. 16,

fig. 10, [not figs. 8, 9,121. 

Eumorphoceras bisvlcatum var. varicata Schmidt, 1933, p. 455,

text fig. 29. 

Eumorphoceras bisulcatum mut. /3 Schmidt, 1933, p. 455, text

fig. 50. 

Van Lechwijck, Stockmans, and Williere, 1955, pi. A, fig. 24,

pi. D, fig. 7. 

fSaffittoceras sp. Delepine, 1937, in Delepine and Menchikoff,

p. 82, 83, pi. 5, fig. 10, text figs. 9,10. 

Eumorphoceras bisulcatum varicatntn [Schmidt] Demanet, 1941,

p. 138, 139, pi. 5, figs. 16,17. 

Schmidt, 1952, p. 215, pi. 13, fig. 14. 

Eumorphoceras bisulcatum mut. grassingtonensis Dunhani and

Stubblefield, 1945, p. 258, 260, pi. 11, figs. 4a-c. 

Eumorphoceras bisulcatum aff. grassingtonensis Currie, 1954,

p. 582, 583, pi. 4, fig. 6. 

Eumorphoceras bisulcatum aff. varicatum Currie, 1954, p. 583,

pi. 4, fig. 7.

Eumorphoceras bisulcatum s. 1. (tending to varicatum) Currie, 

1954, p. 583.

Ribbed involute goniatites from the Inyo Range, many 

of them juvenile, are referred to the type species of 

Eumorphoceras. They are preserved in slightly altered 

fissile to slaty grayish-black shale and tend to be compressed slightly more than is normal and otherwise distorted. Most are ornamented by 30, or slightly more, 

sickle-shaped ribs that curve orad near the prominent 

narrow sulcus that borders the outer edge of the flanks. 

The figured specimen is 15.5 mm in diameter and its 

umbilicus is 3.2 mm wide. It is imperfectly preserved 

and shows 21 ribs in approximately three-quarters of a 

volution. Another specimen, an external mold 11 mm 

in diameter collected at the same locality, has nearly 40 

ribs. Shells in early maturity with 30 to 40 ribs per 

volution are typical of E. bisulcatum.

Figured specimen: SU 9162.

Occurrence: Chainman Shale, lower part, SU 23145 (2 specimens) Spring Trail, Cerro Gordo, Inyo Range; USGS Iocs. 

10403-PC, 15334-PC, 15335-PC, Cerro Gordo Spring trail, 1% 

miles north of Cerro Gordo mine, Inyo Range, Calif.

Eumorphoceras paucinodum Gordon, n. sp.

Plate 2, figures 7-9; text figure 7

Diagnosis. Eumorphoceras ornamented in late adolescent phragmocone with a prominent sulcus bordering
A18 CONTRIBUTIONS TO PALEONTOLOGY

each flank and 11 to 12 broad weak sickle-shaped ribs, 

each terminating dorsad in a prominent umbilical node 

and dying out gradually ventrad.

Description. This species is based on only two internal molds of incomplete phragmocones, but its 

distinctive sculpture separates it easily from other described species. The larger specimen, taken as the holotype, is slightly compressed by crushing along the venter 

anteriorly. Originally this part of the phragmocone 

would have had a diameter of slightly more than 20 

mm. The conch at this stage is subdiscoidal and the 

venter well rounded. Marking the line where the flanks 

meet the ventrolateral shoulder is a prominent longitudinal sulcus 1 mm wide. The flanks are slightly convex 

though nearly flat and slope outward very slightly so 

that the greatest width is at the subrounded umbilical 

shoulders. The umbilical wall is convex and approximately perpendicular to the flank. The diameter of the 

umbilicus is roughly one-third that of the conch.

The sculpture consists of weak sickle-shaped ribs on 

the flanks, most of which terminate in a prominent 

rounded bluntly pointed node at the umbilical shoulder. 

The ribs do not encroach on the umbilical wall but extend radially or very slightly protractively across the 

inner part of the flanks, dying out rapidly ventrad. 

Some appear to curve orad on the outer part of the 

flanks near the sulcus and some appear to split in two, 

but they are so weak in this region that it is difficult 

to determine their shape. On both the holotype and 

paratype an occasional lone weak rib is intercalated 

between the others and fails to reach the umbilical 

shoulder and form a node. Twelve ribs terminatingo

in nodes occur on the final volution of the holotype 

and 11 on the paratype. A few patches of shell material 

adhere to both specimens but show only a smooth 

granular surface.

The external suture (fig. 7) as seen in the holotype 

is typical of Eumorphoceras, having a broad ventral 

lobe that occupies the entire ventral region of the 

conch. The ventral lobe has straight sides sloping at

FIGURE 7. Eumorphoceras paucinodum n. sp., external 

suture X 4 of the holotype at conch diameter of 

16.5 mm.

angles of roughly 40° to the center of the venter and 

is divided to less than half its length into two 

broad pointed prongs by a subtriangular median saddle 

that in turn is notched adorally by a short lobelike protuberance over the siphuncle. The subtriangular first

Diameter (D)_______ _ _ _ __mm

Height of last whorl (H)_ _ _ _do__ _ Width of last whorl ( W) _ do

Width of umbilicus (U) _ _ _ _ do_ _

W/D

W/H

Holotype

1 16.7

7.5

7.8

5.6

.33

.47

1. 04

Paratype

15. 6

7.3

7. 6

4.6

.29

.49

1.04

lateral saddle is rounded orad and centers on the outer 

part of the longitudinal sulcus. The first lateral lobe is 

less than half as wide as the ventral lobe and is pointed, 

with gently convex sides. The second lateral saddle 

curves asymmetrically across the umbilical shoulder. 

The umbilical lobe is short, broad, and rounded. The 

internal suture is not exposed.

Dimensions and proportions

1 The holotype was measured at the widest diameter of no distortion.

Discussion,. Presumably, as in other species of 

Eumorphoceras and in the closely related genus 

Girtyoceras, the phragmocone of E. paucinodum becomes more discoidal with growth and acquires an acute 

to subacute venter, and the ribs and longitudinal sulci 

die out. Further collecting will have to determine 

whether this is so in this species. Meanwhile it should 

be emphasized that the present specimens show only 

the characters of the late adolescent phragmocone.

Comparisons and affinities. This species is distinguished from all previously known species by its sparse 

evanescent ribs that are strengthened at the umbilical 

shoulder to form about a dozen prominent nodes, hence 

its trivial name. The form with the fewest ribs previously know^n from America is Eumorphoceras girtyi 

Elias from the Caney shale of Oklahoma. That species 

has 18 to 21 ribs per volution that are stronger and 

sharper than those of E. paucinodum, and do not terminate in prominent nodes on the umbilical shoulder. E. 

Msulcatum, which gives its name to the stratigraphic 

zone in which E. paucinodum occurs, has 30 to 40 ribs. 

The two species have not yet been found together in 

the same bed.

Primary types: Holotype SU 9163. Paratype SU 9164.

Occurrence: Perdido Formation, top limestone bed, McAllister 

loc. FL 38, 2,100 ft S. 3° E. of Rest Spring, Cottonwood Mountains, Panamint Range, Inyo County, Calif.

Genus ANTHRACOCERAS Frech, 1899 

Anthracoceras macallisteri Gordon, n. sp.

Plate 4, figures 1-3, 7-9; text figure 8 

Diagnosis. Anthracoceras with well-rounded venter 

and an external suture with broad pointed lobes; sides 

of ventral lobe concave dorsad.

Description: This species is based on three incomplete phragmocones from the Panamint Kange. The
CALIFORNIA CARBONIFEROUS CEPHALOPODS A19

conch is subdiscoidal to discoidal, involute; the whorl 

sublenticular in cross section, with a well-rounded narrow venter and very slightly convex flanks. The umbilical shoulders round gently to the narrow umbilicus. 

Patches of shell adhering to one of the paratypes show 

that its surface is smooth; the growth-line pattern is 

not preserved.

The external suture (fig. 8) consists of a broad ventral 

lobe with sloping sides concave dorsad, more strongly 

Founding about a third of the distance orad, divided to 

a little less than half its length by a broad subtriangular 

median saddle into two pointed triangular prongs. The 

first lateral saddle is broad, a little less so than the 

ventral lobe, and very asymmetrically rounded orad. 

The first lateral lobe is rather narrow, roughly as wide 

as either prong of the ventral lobe, rather straight-sided 

ventrad with a shallow sigmoidal bend near the middle 

and convex dorsad. The second lateral saddle is broad, 

shallow, and asymmetrically rounded.

FIGURE 8. AntTiracoceras macallisteri n. sp., external suture 

X 4 of the holotype at whorl height of 9.5 mm.

Dimensions and proportions 

[A is the holotype; B and C are paratypes]

Diameter (D) __ _ _ __ _ mm_

Height of last whorl (H) __ __do _ Width of last whorl (W) _____ _do. _ _ _ Width of umbilicus (U) _ _ _ _ _ _ do _ _ -

U/D_____. ________________________

W/D_ _________ ___________________

W/H_______ _______________________

A

10.6

7.2

1.7

.68

B

U Q

7.3

5. 7

1. 4(?)

nqm

4Q

.78

c

12. 2

6. 7

5. 7

1. 2

. 10

. 43

.78

Comparisons and affinities. Anthracoceras macallisteri is distinguished from A. paucilobum (Phillips) 

of northwestern Europe by its well-developed pointed 

asymmetric first lateral lobe and from A. glabrum Bisat 

by its narrow well-rounded venter.

Primary types: Holotype SU 9165. Paratype SU 9166.

Occurrence: Perdido Formation, uppermost member, McAllister loc. FL 38, 2,100 ft. S. 30° E. of Rest Spring, Cottonwood 

Mountains, Panamint Range, Inyo County, Calif.

Genus DELEPINOCERAS Miller and Furnish, 1954

Delepinoceras californicum Gordon, n. sp. 

Plate 2, figures 10, 15-22; text figures 9A-C

Diagnosis. Delepinoceras with sutures less advanced 

than in type species; prongs of ventral lobe more 

strongly trifid than first lateral lobe. Surface of adolescent conch with about 70 longitudinal lirae.

Description. Six incomplete specimens are available 

for study. The holotype is an internal mold, representing an incomplete phragmocone, with parts of the two 

outer volutions missing but with the inner volutions 

preserved. With the missing parts present, the phragmocone at this stage must have reached a diameter of 

slightly more than 60 mm. The conch is subdiscoidal, 

with a well-rounded venter and gently convex flanks 

sloping outward at an angle of about 25° to one another, 

the greatest width occurring at the rather abruptly 

rounded umbilical shoulders. The umbilicus is narrow, 

its diameter equal to %-%o that of the conch. It has 

rather straight in ward-sloping sides. The shell surface 

is not preserved on the holotype and the large paratypes 

so one cannot tell if the surface is longitudinally lirate 

in the adult as it is in young specimens.

The mature suture (fig. 9A) has the ventral lobe divided to nearly its full length by an inverted long-stemmed goblet-shaped median saddle into two stout trifid 

prongs. The middle lobelet of each prong is long and 

narrowly acuminate; the ventrad one is extended but 

short, narrow, and blunt and the dorsad one merely 

an angulation. The first lateral saddle is narrower 

than either prong of the ventral lobe and is asymmetrically rounded spatulate orad. The first lateral lobe is 

about as wide as either prong of the ventral lobe but 

more weakly trifid; the middle extension narrowly acuminate, the ventrad one rather sharply angular and the 

dorsad one abruptly rounded. The second lateral saddle is broad and asymmetrically rounded. The umFIGURE 9. Delepinoceras californicum n. sp. external suture. 

A, the holtotype X 1 at a whorl height of 30 mm; B, 

inner part of the holotype X 3 at a diameter of 19 mm 

and whorl height of 9 mm ; and C, specimen illustrated 

on plate 2, figure 10, X 4, at a diameter of 13.4 mm and 

whorl height of 6.3 mm.
A20 CONTRIBUTIONS TO PALEONTOLOGY

bilical lobe is moderately short, with an extended point. 

The internal suture consists of a long narrow dorsal lobe 

extended to a point and separated by narrow asymmetrically rounded saddles from a pair of shorter pointed 

hastate lateral lobes. These are joined to the umbilical 

lobes by a broad asymmetrically rounded second lateral 

saddle on either side.

Young stages are represented by a weathered specimen (pi. 2, fig. 10) with a narrowly subspherical conch 

at a diameter of 13 mm. The venter and the umbilical 

shoulders are well rounded. The surface of the shell 

where preserved is ornamented by fairly strong raised 

longitudinal lirae, separated by wider interspaces, of 

which roughly TO occur over the flanks and venter between the umbilical shoulders. The lirae are crossed 

by faint growth lines and by internal varices, spaced 

about one-third of a volution apart on this specimen. 

These bow very slightly orad over the venter and are 

flanked by correspondingly shallow lateral sinuses on 

the veiitrolateral areas.

The external suture at this stage (fig. 90) is goniatitid, with the ventral lobe divided to only slightly more 

than half its length by a snbtriaiigular median saddleThe first lateral saddle is asymmetrically bell shaped. 

The first lateral lobe is slightly less than half the width 

of the ventral lobe, with an acuminate tip and a subangulation at either side.

The inner part of the holotype represents the phragmocone up to a diameter of 23 mm and is thick discoidal. 

Longitudinal lirae are preserved on patches of shell 

material as well as on parts of the internal suture of 

the succeeding volution. The lobes of the external suture (fig. 9#) begin to assume a trifid aspect at diameters greater than 20 mm.

Dimensions and proportions

[B is the inner part of the holotype from U8G8 loc. 15782; A is a paratype from 

McAllister loc. FL 27 and C a paratype from McAllister loc. 10 E8]

Diameter (D) _ mm

Height of last whorl (H) do

Width of umbilicus (U) _ . _ do _

U/D

W/H

A

167

35

28

8

. 12

. 42

. 80

B

22. 5

11. 5

14.3

3.0

. 13

. 64

1. 24

C

13. 2

6.7

10. 1

1. 5

. 11

. 76

1. 51

1 Estimated by extending curvature.

Comparisons and affinities. Delepinoceras calif ornicum is the third species of this genus to be described. 

It differs from the type species D. thalassoide (Delepine) from Haci-Diab on the Algeria-Morocco frontier 

principally in its somewhat less advanced suture. 

Delepine (in Delepine and Menchikoff, 1937, text fig. 

12) illustrated the suture of the type species at a shell 

diameter of 18 mm where it already has a decidedly

trifid aspect. In contrast is the figure of the holotype 

of D. californicum (fig. 9B) at a diameter of 19 mm.

The Russian species D. bressoni Ruzhentsev (1958, p. 

490-492, text figs. 1, 2) is similar to D. calif ornicum in 

shape and has a suture very slightly more advanced than 

that of D. calif arnicum and less advanced than that of 

D. thalassoide. The principal difference is in the sculpture of the adolescent conch. Whereas that of D. calij"ornicum has about 70 strong lirae, the young shell of 

D. bressoni has approximately twice that number, judging from Ruzhentsev's figures, and the transverse sculpture is about as strong as the longitudinal, giving the 

surface of the conch a finely cancellate appearance.

The three species may not represent precisely the 

same stratigraphic horizon, judging from differences in 

the degree of development of the sutures, but all three 

are within the Eumorplioceras ~bhidca~tum zone and 

therefore roughly equivalent in age.

Primary types: Holotype USNM 120622. Paratypes USNM 

120623, SU 9167, 9168.

Occurrence: Perdido Formation, uppermost member, USGS 

loc. 15782-PC, 4,200 ft N. 58° W. of Rest Spring; McAllister 

loc. FL 27, 2,300 ft S. 53° W. of Rest Spring; Cottonwood Mountains, Panamint Range, Inyo County, Calif.

Genus DOMBAROCANITES Ruzhentsev, 1949

Dombarocanites Ruzhentsev, 1949, Akad. Nauk SSSR Doklady,

torn 67,110. 4, p. 738. 

Prolecanites [part] Miller, Furnish, and Schindewolf, 1957, in

Moore, Treatise on Invertebrate Paleontology, p. L70.

Ruzhentsev gave the following diagnosis of the genus,

The conch is discoidal, evolute, with a somewhat wide umbilicus 

and with an elongate elliptical cross section of the whorls. 

The suture line consists of siphonal, antisiphonal and four 

lateral lobes on the exterior. One lateral lobe is present on 

the internal side of the conch. The siphonal lobe is short but 

with a long narrow extension. The first lateral lobe is considerably longer than the wide part of the siphonal lobe. (Free 

translation by S. W. Muller.)

Do'inbarocanites clianclia-rensis Ruzhentsev, 1949, was 

designated the "typical species" and is the only species 

thus far referred to the genus. Its suture is shown in 

figure WB.

Ruzhentsev pointed out that although Dombarocanites has the same number of lobes in its suture as 

Proleca.nites, it is distinguished from that genus by the 

siphonal (ventral) lobe, the wide part of which is considerably higher than the base of the first lateral lobe. 

In Prolecanites the ventral lobe is as long as the first 

lateral (fig. 10O). Miller, Furnish, and Schindewolf 

(1957, p. L70), however, regarded Dombarocanites as a 

synonym of Prolecanites.

At first the writer believed it was necessary to erect 

a new genus for the new Californian species described 

below because of its distinctive trilobate ventral lobe.
CALIFORNIA CARBONIFEROUS CEPHALOPODS A21

Consideration of available names, however, has convinced him that its difference from Dombarocanites 

chancharensis is mainly one of degree in the width of 

the bulges of the ventral lobe. Considering also that c:y ~

such a distinctive ventral lobe occurs with lateral lobes 

of a slightly different shape than those in typical Prolecanites, that it is limited to Russian and Californian 

species that have an approximately equivalent stratigraphic position, and that this position is two major 

cephalopod zones higher than the highest known typical Prolecanites, it would appear reasonable and warranted to recognize Ruzhentsev's genus as distinct and 

assign to it the new species described below.

Dombarocanites masoni Gordon, n. sp. 

Plate 4, figures 4-6,14 ; text figure 104

Diagnosis. Dombarocanites with trilobate ventral 

lobe pinched in orad.

Description. This species is based on three fragmental specimens from the Inyo Range. The holotype 

is the fragment of an internal mold of a phragmocone 

that shows the most complete suture. The mature whorl 

section in this species is elongate-elliptical, the height 

increasing with growth. The venter is strongly rounded, and the flanks are gently rounded. No trace of the 

shell material remains in any of the specimens.

The suture consists of 12 lobes. The ventral lobe of 

the external suture (fig. 1(L4.) is trilobate, pinched in 

orad, with a short rounded prong bulging at either side 

and a long narrow median prong extending apicad, a 

little farther in some sutures than in others. The lateral 

lobes are elongate spatulate, bluntly rounded apicad

or terminating in weak points; all are slightly pinched 

in orad. The lateral saddles are well rounded orad and 

increase regularly in depth from the first to the third, 

the fourth being considerably shorter, and the fifth still 

shorter. The internal suture consists of three lobes, a 

simple dorsal one of moderate length, flanked by an internal lateral lobe at either side, each about the same 

size and shape as the fourth lateral lobe of the external 

suture, separated by narrow rounded saddles.

Dimensions and proportions

Diameter (D) _ __ __ _ mm _

Height of last whorl (H) do

Width of last whorl (W) __ do _

Width of umbilicus (U) _ _ _ _ do

W/H

A

16. 7

9. 1

. 55

B

8. 3

6. 4

. 77

c

6. 7

5.2

. 78

Comparisons and affinities. Dombarocanites masoni 

differs from the only other known species in the genus, 

D. chancharensis Ruzhentsev, principally in the ventral 

lobe of the suture, which is pinched in orad to give it a 

trilobate aspect. The ventral lobe of D. chancharensis 

(fig. 1(15) has nearly straight sides along the thick part.

The only other American prolecanitid, Prolecanites 

americanus Miller and Garner, from beds of Meramec 

age in Indiana, differs by having a rounded subquadrate 

whorl section and by its suture (fig. lO^), which has a 

long narrow undivided ventral lobe, the first three lateral lobes pointed hastate and the fourth narrow, short, 

and pointed.

This species is named for the collector of the type lot, 

J. F. Mason.

FIGURE 10. External sutures of Dombarocanites and Prolecanites. A, Dombarocanites masoni 

n. sp. from the holotype X 5, at a whorl height of 8.4 mm. B. Dombarocanites chancliarensis 

Ruzhentsev from the holotype X 5, at a whorl height of 8.5 mm, after Rozhentsev. C, Prolecanites americanus Miller and Garner from the holotype X 3, at whorl height of 16 mm, from 

Miller and Garner. D, ProcUcanites (Riphaecanites) ? sp., from the only specimen X 10, at 

a diameter of 4.6 mm and whorl height of 1.7 mm.
A22 CONTRIBUTIONS TO PALEONTOLOGY

Primary types: Holotype SU 9168. Paratype SU 9169. 

Occurrence: Chainman Shale, trail 2*4 miles north of the 

Cerro Gordo mine, Inyo Range, Inyo County, Calif.

Genus PROLECANITES Mojsisovics, 1882

Prolecanites (Rhipaecanites) ? sp. 

Plate 4, figures 15-17, text figure 10Z)

A juvenile specimen of a subdiscoidal goniatite with 

a primitive prolecanitid suture was found associated 

with Gravenoceras hesperium Miller and Furnish in the 

Quartz Spring area. Only a little more than 6 mm in 

diameter, the conch of this specimen has a compressed 

oval whorl section, with slightly flattened flanks. The 

umbilicus is not quite half the diameter of the conch.

The suture is exposed on the inner whorls and part of 

the outer volution. It has an undivided U-shaped ventral lobe with a moderately long protuberance apicad 

along the siphuncle. The ventral lobe is separated by a 

moderately well rounded first lateral saddle from the 

U-shaped first lateral lobe, about the same size as the 

main part of the ventral lobe but set a little farther 

orad. The very deep rounded second lateral saddle is 

followed by a shorter narrower second lateral lobe, 

bluntly rounded apicad. Narrower shallower third lateral saddle and lobe follow, then the suture line is fairly 

straight for the short distance to the umbilical seam.

The dimensions of this shell are as follows: diameter 

(D) 6.2; height of last whorl (H) 2.5; width of last 

whorl (W) 2.2; width of umbilicus (U) 2.8 mm. These 

give the following proportions: TJ/D=0.47, W/D = 0.35, 

and W/H = 0.79.

The suture is not maturely developed and although it 

possesses only three lateral lobes, possibly with growth 

at least one more lateral lobe would have been added. 

No fully mature prolecanitids with less than four lateral lobes are known this high up in the section. The 

shape of the ventral lobe does not appear trifid as in the 

genus Epicanites Schindewolf, 1926 or any of the daraelitid stock. The fact that the wider part of the ventral 

lobe extends further apicad than the first lateral lobe 

would appear to exclude the possibility of this shell 

being a Dotnbarocanites; however, it is such a young 

individual that one cannot be sure. The suture appears 

to be closest to that of Rhipaecanites Ruzhentsev (1949, 

p. 737), which has been put into synonymy with 

Prolecanites by Miller, Furnish, and Schindewolf (1957, 

p. L70).

Figured specimen: USNM 120624.

Occurrence: Perdido Formation, top limestone bed, USGS 

loc. 15783-PC, 9,000 ft N. 83%° E. of bench mark 5257 at Quartz 

Spring, Panamint Range, Inyo County, Calif.

MIDDLE PENNSYLVANIAN SPECIES

Genus PARALEGOCERAS Hyatt, 1884

?Paralegoceras texanum (Shumard)

Plate 4, figure 24

Goniatites texanus Shumard, 1863, p. 109. 

Paralegoceras texanum, Smith, 1903, p. 104.

An external mold in a loose block of limestone from 

the Providence Mountains is that of a paralegocerid 

ammonoid that agrees in shape and in ornament with 

Paralegoceras texanum (Shumard). The conch has a 

diameter of 108 mm near the end, and here the whorl is 

32 mm high and the umbilicus 62 mm in diameter. The 

umbilicus/diameter ratio is 0.57. The shell ornament 

consists of approximately 35 transversely elongate umbilical nodes per volution that split into transverse cords 

over the flanks and venter; about four cords emanate 

from a single node and one or two intercalated between. 

The cords are fairly straight across the flanks, swing 

forward slightly to form a broad bow over the ventrolateral shoulders and backward over the venter to form 

a broad rounded ventral sinus. Subequally spaced 

longitudinal cords of equal weight to the transverse 

ones give the shell surface a weakly cancellate appearance on the venter and ventrolateral shoulders.

The suture is not preserved on this specimen, so one 

cannot ascertain whether it was like that of Paralegoceras texanum or of the closely related Diaboloceras 

varicostatum, Miller and Furnish, which is almost as 

evolute but generally lacks umbilical nodes on the outer 

volution. The strength of the umbilical nodes in this 

specimen suggests the former species, rather than the 

latter, but the fact that it was found several hundreds of 

miles farther west than any paralegocerid has heretofore been reported, demands caution in its identification. It is referred here to the species that agrees most 

closely in shape and surface sculpture and this identification is questioned in the absence of evidence as to the 

nature of its suture. An Atokan age for the containing 

beds is likely but a very late Morrow age is a remote 

possibility.

Figured specimen: SU 9170.

Occurrence: Bird Spring Formation, loose black limestone, 

west slope of Providence Mountains 5,500 ft west of Sheep 

Spring, a few miles southeast of Kelso, San Bernardino Courty, 

Calif.

Genus BISATOCERAS Miller and Owen, 1937 

Bisatoceras cf. B. greenei Miller and Owen

Plate 4, figures 10-13 ; text figure 11 

Bisatoceras greenei Miller and Owen, 1939, Jour. Paleontology,

v. 13, no. 2, p. 155, 156, pi. 20, figs. 1-7, text fig. 6. 

A silicified phragmocone from a gray sandy limestone bed in the Panamint Range is comparable to this
CALIFORNIA CARBONIFEROUS CEPHALOPODS A23

species. The conch is subdiscoidal, has a strongly 

rounded venter, and gently rounded flanks. The umbilical shoulders are strongly rounded, nearly subangular, and the umbilicus appears to be closed. No traces 

of shell material or surface sculpture remain.

FIGURE 11. Bisatoceras cf. B. greenei Miller and Owen, 

external suture X 4 from the unique California specimen, at a diameter of 18 mm and whorl height of 

10.5 mm.

The eight-lobed suture has the ventral lobe divided 

to about three-quarters of its length into two large inflated pointed prongs. The first lateral saddle is somewhat asymmetrically rounded and spatulate. The first 

lateral lobe is not quite as wide as either prong of the 

ventral lobe, slightly more convex on the ventrad side 

than on the dorsad one and pointed apicad. The second 

lateral saddle is asymmetric and broad. The umbilical 

lobe is short and subrounded. The internal suture consists of three lobes, but their details cannot be ascertained in this specimen.

The dimensions of this shell, in mm, are as follows: 

diameter (D) 19.9; height of last whorl (H) 10.5; width 

of last whorl (W) 9.0; umbilicus closed. These give 

the following proportions: W/D=0.45, W/H=0.86.

This species agrees in its subdiscoidal shape and in 

the general configuration of its external suture with 

Bisatoceras greenei Miller and Owen. Only the lack of 

more and better preserved material precludes a positive 

identification. The stratigraphic position of this specimen is a few feet above fusulinids determined in the 

field by L. G. Henbest as very late Atoka or earliest Des 

Moines in age. The primary types of B. greenei were 

described from beds of Des Moines age in Missouri.

Figured, specimen: USNM 120625.

Occurrence: Tihvipah Limestone, middle part, USGS loc. 

19804-PC, about 1,500 ft due east Rest Spring, Cottonwood 

Mountains, Panamint Range, Inyo County, Calif.

Genus STENOPRONORITES Schindewolf, 1934

Stenopronorites sp.

Text figure 12

A fragment of light-gray fine-grained sandstone 

weathering light brownish gray preserves parts of eight 

slightly distorted sutures of a pronoritid. The most 

complete suture is reproduced in figure 9. It is that

part of the external suture preserved on the flanks of 

the flat-sided pronoritid whorl between the ventrolateral 

and the umbilical shoulders. In the one figured, this 

distance is approximately 16 mm. The suture consists 

of a bifid first lateral lobe and four additional undivided lateral lobes. The number and shape of the 

lateral lobes suggest that this specimen should be 

referred to the genus Stenopronorites.

Figured, specimen: SU 9171.

Occurrence: Tihvipah Limestone, McAllister loc. FL 5, in 

 outlier, 7,200 ft N. 9° W. of Rest Spring, Cottonwood Mountains, 

Panamint Range, Inyo County, Calif.

FIGURE 12. Stenopronorites sp. Part of 

the external suture X 3 of the 

crushed specimen, at a whorl height 

of about 16 mm.

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A24 CONTRIBUTIONS TO PALEONTOLOGY

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 1954, Rocks and structure of the northern Providence 

Mountains, San Bernadino County, California, [Pt.] 4, in 

Chap. 4 of Jahns, R. H., ed., Geology of southern California: 

California Dept. Nat. Res., Div. Mines Bull. 170, p. 27-35, 

3 pis.

Hind, Wheelton, 1918, On the distribution of the British Carboniferous goniatites, with a description of one new 

genus and some new species: Geol. Mag., n. ser., decade 6, 

v. 5, no. 10, p. 434-450, pi. 16.

Hudson, R. G. S., 1941, The Mirk Fell beds (Namurian, E2 ) of 

Tan Hill, Yorkshire: Yorkshire Geol. Soc. Proc., v. 24, pt. 

4, p. 259-289, 6 text figs.

 1946, The Namurian goniatites Cravenoceatoides bisati 

Hudson and Ct. lirifer n. sp.: Yorkshire Geol. Soc. Proc., 

v. 25, pt. 6, p. 375-386, pis. 21, 21A, 1 text fig.

Kirk, Edwin, 1918, Stratigraphy of the Inyo Range, p. 19-48, 

in Knopf, Adolph, A geologic reconnaissance of the Inyo 

Range and the eastern slope of the southern Sierra Nevada, 

Calif., U.S. Geol. Survey Prof. Paper 110, 130 p.

Leckwijck, W. Van, Stockmans, F., and Williere, Y., 1955, Sur 

1'age, la fiore et la faune des formations namuriennes affaissees dans les poches de dissolution du viseen de la 

region de Samson (Meuse namuroise) : Assoc. Etude 

Paleontologie Stratigraphie Houilleres, Pub. no. 21, p. 265- 

275, 4 pis., 2 text figs.

Mailleux, Eugene, 1933, Terrains, roches et fossiles de la Belgique : 2e ed., 212 p., 252 figs., 18 pis., Mus. royale histoire 

nat. Belgique, Patrimoine, Bruxelles.

McAllister, J. F., 1952, Rocks and structure of the Quartz Spring 

area, northern Panamint Range, California: California 

Div. Mines, Spec. Rept. 25, 38 p., 3 pis., 13 text figs.

Merriam, C. W., and Hall, W. E., 1957, Pennsylvanian and Permian rocks of the southern Inyo Mountains, California: 

U.S. Geol. Survey Bull. 1061-A, p. 1-13.

Miller, A. K., and Furnish, W. M., 1940, Studies of Carboniferous ammonoids: Jour. Paleontology, pts. 1-4, v. 14, no. 

4, p. 356-377, pis. 45-49, 17 text figs.; pts. 5-7, v. 14, no. 

6, p. 521-543, pis. 62-65, 7 text figs.

 1954, The classification of the Paleozoic ammonoids: 

Jour. Paleontology, v. 28, no. 5, p. 685-692, 2 text figs.

Miller, A. K., Furnish, W. M., and Schindewolf, O. H., 1957, 

Paleozoic ammonoidea, in Moore, Treatise on invertebrate 

paleontology, Pt. L (Mollusca 4), p. L11-L79, text figs. 

1-123.

Miller, A. K., and Owen, J. B., 1937, A new Pennsylvanian 

cephalopod fauna from Oklahoma: Jour. Paleontology, v. 

11, no. 5, p. 403-422, pis. 50-52, 5 text figs.

Miller, A. K., and Youngquist, Walter, 1948, The cephalopod 

fauna of the Mississippian Barnett formation of central 

Texas: Jour. Paleontology, v. 22, no. 6, p. 649-671, pis. 

94-100, 3 text figs.

Miller, A. K., Youngquist, Walter, and Nielsen, M. L., 1952, 

Mississippian cephalopods from western Utah: Jour. 

Paleontology, v. 26, no. 2, p. 148-161, pis. 25, 26, 5 text figs.

Moore, E. W. J., 1946, The carboniferous goniatite genera Girtyoceras and Eumorphoceras: Yorkshire Geol. Soc. Proc., 

v. 25, pt. 6, p. 387-445, pis. 22-27, 31 text figs.

Moore, R. C., 1948, Paleontological features of Mississippian 

rocks in North America and Europe, in Weller, J. M., ed., 

Symposium on problems of Mississippian stratigraphy and 

correlation: Jour. Geology, v. 56, no. 4, p. 373--402, illus.

Nolan, T. B., Merriam, C. W., and Williams, J. S., 1956, The 

stratigraphic section in the vicinity of Eureka, Nevada: 

U.S. Geol. Survey Prof. Paper 276, 77 p., 2 pis., 2 text figs.

Plummer, F. B., and Scott, Gayle, 1937, Upper Paleozoic ammonites in Texas: Texas Univ. Bull. no. 3701, 516 p., 41 

pis., 88 text figs.

Ruzhentsev, V. E., 1949, Nekotorye novye namiurskie ammonity 

iz Aktyubinskoy oblasti: Akad. Nauk SSSR Doklady, v. 

67, no. 4, p. 737-740, 3 text figs.

 1958, O nakhozhdenii na yuzhnom urale roda Delepinoceras (Otryad goniatitov) : Akad. Nauk SSSR Doklady,

V. 122, no. 3, p. 489-492, 2 text figs. 

Schmidt, Hermann, 1925. Die carbonischen Goniatiten Deutschlands : Preuss. geol. Landesanstalt, Jahrb. 1924, v. 45, p. 489-

609, pis. 19-26.

 1929, Tierische Leitfossilien des Karbon : in Giirich, Leitfossilien, Lief. 6, p. 57-77 (Cephalopoda), pis. 15-20, Berlin.

 1933, Cephalopodenfaunen des alteren Namur aus der 

Umgegend von Arnsberg in Westfalen: Preuss. geol. Landesanstalt, Jahrb. 1933, v. 54, p. 440-461, 86 text figs.

 1952, Prolobitcs und die Lobenentwicklung bei Goniatiten :

Palaeont. Zeitschr., v. 26, no. 3/4, p. 205-217, pi. 13, 4 text 

figs.

Shinier, H. W., and Shrock, R. R., 1944, Index fossils of North 

America : New York, John Wiley & Sons, 837 p., 303 pis.

Shumard, B. F., 1863, Descriptions of new Paleozoic fossils: 

St. Louis Acad. Sci. Trans., v. 2, p. 108-113.

Smith, J. P., 1903, Carboniferous ammonoids of North America: 

U.S. Geol. Survey Mon. 42, 211 p.. 29 pis.

Spencer, A. C., 1917, The geology and ore deposits of Ely, Nevada : U.S. Geol. Survey Prof. Paper 96, 189 p., maps.
CALIFORNIA CARBONIFEROUS CEPHALOPODS A25

Youngquist, Walter, 1949a, The cephalopod fauna of the White 

Pine shale of Nevada: Jour. Paleontology, v. 23, no. 3, 

p. 276-305, pis. 56-t>4, 2 text figs.

 1949b, The cephalopod fauna of the White Pine shale of 

Nevada, Supplement: Jour. Paleontology, v. 23, no. 6, p. 

613-616, pi. 100,1 text fig.
INDEX

Page

Acknowledgments_______________ A^

americanus, Prolecanites...................... 21

Anthracoceras... _____-..___-_____ 18

glabrum.................................. 19

macallisteri---- ...................18, 19; pi. 4

paucilobum.-............................. 19

Bactrites..-........................ _..__. _..__ 8

carbonarius......._________. 5,8; pi. 1

nevadensis..--............................ 10

quadrilineatus............................. 8

Bird Springs Formation____________ 6,7

Bisatoceras.................................... %%

greenei---.---...................... SS, 23; pi. 4

bisulcatum, Eumorphoceras........5, 6, 9, 17, 20; pi. 2

grassingtonensis, Eumorphoceras........... 17

mut. 0, Eumorphoceras ................. 17

varicata, Eumorphoceras................... 17

varicatum, Eumorphoceras................. 17

bressoni, JDelepinoceras........................ 20

californicum, JDelepinoceras............ 19, 20; pi. 2

cancellatum, Gastrioceras...................... 6

carbonarius, Bactrites...................... 5,8; pi. 1

cessator, Cyrtoceras............................ 9,10

Scyphoceras......................... 9, 10; pi. 1

Chainman Shale____________ 1,2,6, 7,16,17 

chancharensis, Dombarocanites................. 20,21

clinatum, Mitorthoceras................... 9; pi. 1

Cravenoceras................................. 2,6,11

hesperium .... 2,3,6, 9, 11, 12,13,15,16, 22; pi. 3

inyoense............... 11,12,13,^,15; pis. 2, 3

kingi................................ 11,12,13,15

leion...................................... 15

merriami.............. 2,3,6,9,13,^5,16; pi. 2

nevadense........................... 11,12,13,15

richardsonianum.......................... 16

scotti...................................... 15

Cravenoceratoides............... _____.... 6

nititoides........................ 5,6, 16, 17; pi. 4

Cyrtoceras cessator............................ 9,10

Delepinoceras bressoni......................... 20

californicum......................... 19,20; pi. 2

thalassoide.. _______________.. 20 

Diaboloceras varicostatum...................... 22

Diamond Peak Formation___.__.__.. 2,6 

Dombarocanites............................... HO

chancharensis....-........................ 20,21

masoni.............................. 6,21; pi. 4

Ely Limestone. 

Epicanites......

[Italic page numbers indicate descriptions]

Page 

Eumorphoceras.............................. A6, 17

bisulcatum.................... 5,6,9, 17, 20; pi. 2

grassingtonensis....................... 17

mut. j8____________________ 17

varicata.....................____ 17

varicatum............................. 17

paucinodum........................... 17;^\. 2

Gastrioceras cancellatum....................... 6

richardsonianum.......................... 5,16

glabrum, Anthracoceras........................ 19

Ooniatites..................................... 5

texanus................................... 22

grassingtonensis, Eumorphoceras 6isulcatum... 17 

greenei, Bisatoceras......................... ««, pi. 4

Hematites..................................... 10, 11

sp__......................._......... ;0;pl. 1

hesperium, Cravenoceras_____________ 2, 

3,6, 9, 11, 12,13,15,16,22; pl.3

impressus, Pericydus......................... 17

Introduction..._________________ 1 

Inyo Range____ __ _____ __. _ _ 5 

inyoense, Cravenoceras..... 11,12,13,^,15; pis. 2,3

Joana Limestone.

kingi, Cravenoceras- . -.. ... 11,12,13,15

Late Mississippian species..._________ 7 

leion, Cravenoceras............................ 15

Liroceras..................................... 10

sp__.__.... -...- ............... 10; pi. 2

macallisteri, Anthracoceras.............. 18, 19; pi. 4

masoni, Dombarocanites ................ 6,$H;p\. 4

merriami, Cravenoceras....... 2, 3,6,9,13, 15, 16; pi. 2

Mitorthoceras................-................ 8

clinatum................................ 9; pi. 1

perfilosum............................ 8, 9; pi. 1

nevadense, Cravenoceras................. 11,12,13,15

nevadensis, Bactrites..............- ...-... 10

nititoides, Cravenoceratoides.......... 5,6,16,17; pi. 4

Nuculoceras nuculum......................... 6

nuculum, Nuculoceras........................ 6

Orthoceracone. 

Orthoceras.....

Page 

Panamint Range....__..... ...__ A#

Paralegoceras texanum................... §,%%; pi. 4

paucilobum, Anthracoceras.................... 19

paucinodum, Eumorphoceras............... 17; pi. 2

Perdido Formation______________ 1,2,

3, 5,6,7,8,9,10,11,14,15,16,19,20,22

perfilosum, Mitorthoceras.................. 8, 9; pi. 1

Pericydus impressus.......................... 17

Pilot Shale............... ...... ........ 2

Prolecanites................................ 20,21,«

americanus............................... 21

(Rhipaecanites) sp.___ _ ... ««;pl. 4 

Providence Mountains. ___.._ _ _ 6 

Providence Mountains Limestone._.. . 6

quadrilineatus, Bactrites.

Rayonnoceras................................. 7

solidiforme.......................... 3, 7, 8; pi. 1

vaughanianum ........................... 8

Register of localities..... . .. 6

Rest Spring Shale......... 2,3,5,6,7,8,15,16

Rhipaecanites................................. 22

(Rhipaecanites) sp., Prolecanites............ %%; pi. 4

richardsonianum, Cravenoceras................ 16

Gastrioceras............................... 5,16

Sagittoceras sp.. 17 

scotti, Cravenoceras........ 15

Scyphoceras................................... 9, 10

....... .. 9, 10; pi. 1

e, Rayonnoceras................. 3,7;pl. 1

Stanford University Collections......__._ 6

Stenopronorites............................... S3

sp........................................ S3

texanum, Paralegoceras................... 6,2%; pi. 4

texanus, Ooniatites............................ 22

thalassoide, Delepinoceras...................... 20

Tihvipah Formation.__... . . 7 

Tihvipah Limestone. ..._ -__...- 3,5,6,23 

Tin Mountain Limestone... 2

U.S. Geological Survey collections........._ 7

varicata, Eumorphoceras bisulcatum............ 17

varicatum, Eumorphoceras bisulcatum......... 17

varicostatum, Diaboloceras..................... 22

vaughanianum, Rayonnoceras......... 8

White Pine Shale........ 2,5,7

A27
PLATES 1-4
PLATE 1

[All figures natural size unless otherwise indicated on plate]

FIGURES 1, 5. Rayonnoceras aff. R. solidiforme Croneis (p. A7).

1. Fragment of the immature phragmocone broken laterally in longitudinal section to expose septa,

cameral fillings, and fluted connecting rings, X 1, USNM 120615, from USGS loc. 15783-PC. 

5. Longitudinal dorsoventral section X % of a specimen, USNM 120614, from Merriam loc. 2001. 

2-4. Mitorthoceras cf. M. perfilosum Gordon (p. A8).

Side view X 2 and X 1 of an incomplete phragmocone (SU 9151) and view X 2 of the adoral end

of another (SU 9151A), both specimens from SU loc. 2776. 

6-9. Scyphoceras cf. S. cessator (Hall and Whitfield) (p. A9).

Ventral, adoral, and side views X 2 and ventral view X 1 of a specimen SU 9153, from SU loc. 2776. 

10-12. Bactrites! cf. B.I carbonarius Smith (p. A8).

Side view X 1 and adpical and side views X 2 of part of a phragmocone, SU 9150, from McAllister

loc. FL 38. 

13-18, 22, 23. Mitorthoceras clinatum Gordon, n. sp. (p. A9).

13-18. View of adapical end X 2, side view X 1, and views of adoral end and side X 2, view (uncoated)

X 4, and ventral view X 3 of the holotype, USNM 120616 from USGS loc. 17024-PC. 

22, 23. Side and ventral views X 1 of a hypotype, SU 9152, from SU loc. 2776. 

19-21. Hematites'! sp. (p. A10).

Side view X 1 and views of the adapical end and side X 2 of a small fragment of a phragmocone of

a possible belemnite, SU 9155, from SU loc. 2776.

NOTE. The specimen shown in figures 13-18 is from the Chainman Shale, Burbank Hills, Millard County, Utah. The rest 

are from the Perdido Formation, near Rest Spring, Panamint Range, Inyo County, Calif.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 483 -A PLATE 1

ORTHOCONIC NAUTILOIDS OF THE GENERA RAYONNOCERAS, MITORTHOCERAS, AND

BACTRITES1; CYRTOCONIC NAUTILOID OF THE GENUS SCYPHOCERAS; AND A

POSSIBLE BELEMNOID, HEMATITES!
PLATE 2

[All figures natural size unless otherwise indicated on plate]

FIGUKES 1-4. Liroceras! sp. (p. A10).

Front, side, and back views X 2 and side view X 1 of an adolescent specimen, SU 9154, from McAllister

loc. FL 38, Perdido Formation, near Rest Spring, Panamint Range, Calif. 

5, 6. Cravenoceras inyoense Gordon, n. sp. (p. A14).

Front and side views X 1 of a broken paratype, SU 9159, showing profile of umbilicus, from McAllister

loc. FL 38, same as above. 

7-9. Eumorphoceras paucinodum Gordon, n. sp. (p. A17).

Back and side views X 2 and side view X 1 of the holotype, SU 9163, from McAllister loc. FL 38, same

as above. 

10, 15-22. Delepinoceras californicum Gordon, n. sp. (p. A19).

10. Side view X 1 of a juvenile paratype, SU 9168, McAllister loc. 10 E8.

15-17. Front section, side, and back views X 1 another paratype, SU 9167 from McAllister loc. FL 27. 

18-22. Side and ventral views X 1 of the outer volution of the holotype and back, side, and front views 

X 1 of the inner part of the same specimen, USNM 120622, from USGS loc. 15782-PC. Perdido Formation near Rest Spring, Panamint Range, Calif. 

11, 12. Cravenoceras merriami Youngquist (p. A15).

Side and front views X 1 of a specimen, USNM 120619, from USGS loc. 15783-PC probably from the base

of the Rest Spring Shale, Panamint Range, Calif. 

13, 14. Eumorphoceras bisulcatum Girty (p. A17).

Side views X 1 and X 2 of a specimen, SU 9162, Chainman Shale near Cerro Gordo mine, Inyo Range, Calif.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 483-A PLATE 2

$&3i^w ^

12

* ;i* i : '~ i,-"» W . £ H'rt/l

Hi, *

17

19

COILED NAUTILOID OF THE GENUS LIROCERASt AND AMMONOIDS OF THE GENERA 

CRAVENOCERAS, EUMORPHOCERAS, AND DELEPINOCERAS
PLATE 3

[All figures natural size unless otherwise indicated on plate]

FIGUBES 1, 2, 6-13, 18-20. Cravenoceras inyoense Gordon, n. sp. (p. A14).

1, 2. Front and side views X 1 of the holotype, SU 9157, from SU loc. 2776, Perdido Formation,

near Rest Spring, Panamint Range, Inyo County, Calif. 

6-9. Front, view X 2, side view X 1, and side and back views X 2 of a paratype, SU 9158B, from

the same locality as the holotype. 

10-13. Front, side, and back views X 2 and side view X 1 of another paratype, SU 9158C, from

the same locality. 

18-20. Side view X 1 and side and front views X 4 of an adolescent paratype, SU 9158D, from

the same locality. 

3-5, 14-17, 21-33. Cravenoceras hesperium Miller and Furnish (p. All).

3-5. Back, side, and front views X 1 of a broad variant more evolute than the typical form, USNM

120617, from USGS loc. 15782-PC, Perdido Formation, near Rest Spring, Panamint Range, Inyo

County, Calif. 

14-17. Side view X 1 and front, side, and back views X 2 of a small typical specimen, SU 9156

from SU loc. 2776, Perdido Formation, near Rest Spring.

21-23. Back, side, and front views X 1 of another specimen from the same locality as the last. 

24-26. Front, side and back views X 1 of a mature example from the same locality. 

27-29. Side view X 1 and side and front views X 4 of an adolescent specimen from the same locality. 

30-33. Side view X 1 and front, side, and back views X 2 of a specimen from the same locality

showing the typical cravenoceratid sculpture.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 483-A PLATE 3

AMMONOIDS OF THE GENUS CRAVENOCERAS
PLATE 4

[All figures natural size unless otherwise indicated on plate]

FIGUKES 1-3, 7-9. Anthracoceras macallisteri Gordon, n. sp. (p. A18).

1-3. Back and side views X 2 and side view X 1 of the holotype, SU 9165, from McAllister loc. FL 38, Perdido

Formation, near Rest Spring, Panamint Range, Inyo County, Calif.

7-9. Back and side views X 2 and side view X 1 of a paratype, SU 9166 from the same locality. 

4-6, 14. Dombarocanites masoni Gordon, n. sp. (p. A21).

4-6. Side view X 1 and side and ventral views X 2 of the holotype, SU 9168, a fragment of a whorl showing

the suture, Chainman Shale, 2}i miles north of Cerro Gordo mine, Inyo Range, Inyo County, Calif. 

14. Side view X 1 of a larger paratype, a fragmental phragmocone, SU 9169, from the same locality. 

10-13. Bisatoceras cf. B. greenei Miller and Owen (p. A22).

Side view X 2 and back, side, and front views X 1 of a silicified specimen, USNM 120625, from USGS loc. 

19804-PC, Tihvipah Formation, about 1,500 feet due east of Rest Spring, Panamint Range, Inyo County, 

Calif. 

15-17. Prolecanites (Rhipaecanites)'? sp. (p. A22).

Back, side, and front views X 4 of a specimen, USNM 120624 from USGS loc. 15783-PC, Perdido Formation,

top limestone bed (?), near Quartz Spring, Panamint Range, Inyo County, Calif. 

18-23. Cravenoceratoides cf. C. nititoides (Bisat) (p. A16).

18-20. Front, side, and back views X 4 of a small limonitic specimen, USNM 120620, from USGS loc. 15335- 

PC.

21. Side view X 1 of a crushed specimen from the same locality.

22. 23. Oblique view X 3 and X 1 of a specimen, USNM 12062 from USGS loc. 15334-PC. All are from

the Chainman Shale, about 1% miles north of Cerro Gordo mine, Inyo Range, Inyo County, Calif. 

24. ?Paralegoceras texanum (Shumard) (p. A22).

Rubber cast X 1 of an external mold in limestone, SU 9170, from J. Hazzard loc. P-1767, Providence Mountains, San Bernardino County, Calif.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 483-A PLATE 4

&Ky*/$?'m* i/Milfe

^24

AMMONOIDS OF THE GENERA ANTHRACOCERAS, DOMBAROCANITES, BISATOCERAS, 

PROLECANITES (RHIPAECANITES)!, CRAVENOCERATOIDES, AND PARALEGOCERAS?

U.S. GOVERNMENT PRINTING OFFICE : 1964 O 709-592