Biostratigraphy of the 

Phosphoria, Park City, and 

Shedhorn Formations

GEOLOGICAL SURVEY PROFESSIONAL PAPER 313-D

Work done partly on behalf of the 

U.S. Atomic Energy Commission

Biostratigraphy of the 

Phosphoria, Park City, and 

Shedhorn Formations

By ELLIS L. YOCHELSON 

With a Section on Fish

By DIANNE H. VAN SICKLE

GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

GEOLOGICAL SURVEY PROFESSIONAL PAPER 313-D

Work done partly on behalf of the 

U.S. Atomic Energy Commission

Distribution of megafossils in more than 

collections, mainly from measured sections^ and 

their paleoecological interpretation

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1968
UNITED STATES DEPARTMENT OF THE INTERIOR 

STEWART L. UDALL, Secretary

GEOLOGICAL SURVEY 

William T. Pecora, Director

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

Washington, D.C. 20402 - Price 60 cents (paper cover)
CONTENTS

Abstract., ________________________________________

Introduction.______________________________________

Stratigraphic setting.___________________________

Previous work..________________________________

Acknowledgments ______________________________

Pr ocedures_ ________________________________________

Identification__ _ _ _____________________________

Abundance.___________________________________

Arrangement of summary data.____-__________---

Ecological considerations.___________________________

Fauna! elements._______________________________

Protozoa_________________________________

Porif era_ __________________________________

Coelenterata_ ______________________________

Echinodermata_ ____________________________

Bryozoa_ __________________________________

Brachiopoda_ ______________________________

Inarticulata. ___________________________

Articulata.____________________________

Moil us ca __________________________________

Pelecypoda_ ___________________________

Protobranchs_ ____________________

Pectenoids and mytiloids____________

Other pelecyods.___________________

Scaphopoda_ ______ _ ___________________

Gastropoda. ____________________________

Cephalopoda.__________________________

Arthropoda_ _______________________________

Fish, by Dianne H. Van Sickle-______________

Associations of the fauna._______________________

Fossil categories ____________________________

Interpretation of categories._________________

Paleoecological interpretations______________________

Park City Formation__________________________

Grandeur Member.____ ____________________

Franson and Ervay Members.__________-_--_

Phosphoria Formation_________________________

Meade Peak and Retort Phosphatic Shale Members., ___________________________________

Lower chert, Rex, and Tosi Chert Members.__.. 

Shedhorn Sandstone.___________________________

Age of the Phosphoria and correlative formations.______

Phosphoria Formation_________________________

Meade Peak and Retort Phosphatic Shale Members... __________________________________

Lower chert, Rex, and Tosi Chert Members.___ 

Park City Formation__________________________

Grandeur Member._________________________

Franson and Ervay Members._______________

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Age of the Phosphoria and correlative formations Con.

Shedhorn Sandstone.__________-____----------__ 626

Summary of age relationships,___________________ 627

Geographic distribution of collections-________-___---- 630

Grandeur Member of Park City Formation-------- 630

Idaho-__________________________________ 631

Montana.____--____-__________---___--_-_- 631

Utah ______--_-------_---_----_----- 932

Wyoming. _____________________--__-------- 632

Lower chert member of Phosphoria Formation. _ _ _ _ 632

Meade Peak Phosphatic Shale Member of Phosphoria Formation.. _ __________________________ 633

Idaho___________ -_ ---_ 633

Montana.------_-----_----_---------_----- 633

Utah_____-______-____--_____-__--_--.--- 633

Wyoming. ____________________--_-____-_--- 634

Franson Member of Park City Formation.-_ _______ 634

Idaho._____________________________ 635

Montana. _______^_-_-_______-_--__-------- 635

Utah__________________________________ __ 635

Wyoming- ____________________-_-_-_-_--__- 636

Rex Chert Member of Phosphoria Formation-_____ 638

Idaho-_--_--_-----_---_----_---------___ 638

Montana.__-_---_-___--_-__---.----.------ 639

Utah___________________________-_____-_--- 639

Wyoming. _________________________________ 639

Lower member of Shedhorn Sandstone.___________ 640

Montana.---______--___-_-__--_---_--_--_- 640

Wyoming- _________________________________ 640

Retort Phosphatic Shale Member of Phosphoria

Formation _-___________________--_-_-_____--- 640

Idaho._____-_______---____------_-_----_-- 641

Montana._________________________________ 641

Wyoming. __-________________-----_---__-_- 641

Cherty shale member of Phosphoria Formation....- 642

Ervay Carbonate Rock Member of Park City

Formation. _ _--______---_____-________----- 642

Utah_-___.________-__-___--___---_----_--- 642

Wyoming. ______________-__-___--_-___--__- 642

Tosi Chert Member of Phosphoria Formation._____ 643

Montana._________________________________ 643

Wyoming..... _____________ ________________ 643

Upper member of Shedhorn Sandstone.___________ 643

Montana._________________________________ 643

Wyoming__________________----__--_____- 644

Register of localities._______________________________ 644

Unstudied and discarded collections.._________________ 653

References.________________--_-__-____-_--__-_---_- 654

Index ____-______-_--___-__-_-----_-___--_--__---_- 657

m
IV CONTENTS

ILLUSTRATIONS

Figure 157. Distribution of sections from which fossils were collected. _______________-___________-__---_-_------- 578

158-166. Position of collections in sections of Meade Peak Member from 

158. Mud Spring to North Wooley Range, Idaho_______________________ 603

159. Ballard Trench to Conda mine, Idaho____-__-_-_-_--__-____---_---_----------_-------_- 604

160. Trail Canyon to West Dairy, Idaho___________________________________ ____ 605

161. Swan Lake Gulch to Hot Spring, Idaho_________________________ 606

162. Little Brush Creek to Strawberry Valley, Utah__________________ _ 607

163. Hobble Creek to Laketown Canyon, Utah__________________________________ 608

164. Cumberland to Basin Creek, Wyo_____________-_-_-_-_____-_______.________-- 609

165. Fall Creek, Idaho, to Wheat Creek, Wyo___________________________________-__ 610

166. Fall Creek, Idaho, to Bull Lake, Wyo_.__________________________________. 611

167, 168. Position of collections in sections of Retort Member from 

167. Kelley Gulch to Little Sheep Creek, Mont___ -_-___._ . . 612

168. Big Sheep Canyon to Canyon Camp, Mont-____________________-____-___-_--______-__-_- 613

TABLES

Page 

TABLE 1. Occurrences of fossil categories in the Park City Formation__ _ _____________________________________________ 597

2. Occurrences of fossil categories in Phosphoria and Shedhorn Formations..______________________-_----__---.-_ 601

3. Occurrence by State and stratigraphic member of coelenterates, echinoderms, bryozoans, arthropods, vertebrates, 

and generically identifiable brachiopods and mollusks within the Phosphoria, Park City, and Shedhorn Formations. ________________________________________________________________________________________ 618

4. Stratigraphic occurrence of brachiopods and mollusks in the Phosphoria rock complex_______________________ 627

5. Distribution and preliminary identification of fish remains in Wyoming________________________-___---__--- 629
GEOLOGY OF THE PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

BIOSTRATIGRAPHY OF THE PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS

BY ELLIS L. YOCHELSON

ABSTRACT

During fieldwork on the Phosphoria, Park City, and Shedhorn 

Formations, 1,509 collections of fossils were obtained. This 

report is concerned (1) with the identity and stratigraphic and 

geographic distribution of these fossils, (2) with paleoecological inferences which may be drawn from these fossils, and 

(3) with the age of the formations collectively termed the 

Phosphoria rock complex, for the sake of convenience.

The Phosphoria rock complex consists of three formations: the 

Shedhorn Sandstone, divided into a lower and upper member; 

the Phosphoria Formation, divided in ascending order into the 

lower chert member, Meade Peak Phosphatic Shale Member, 

Rex Chert Member, cherty shale member, Retort Phosphatic 

Shale Member, and Tosi Chert Member; and the Park City 

Formation, divided in ascending order into the Grandeur Member, Franson Member, and Ervay Carbonate Rock Member.

Fossils were obtained from 107 measured sections and 15 

additional localities. The area sampled includes parts of Idaho, 

Montana, Utah, and Wyoming and is comparable in size to 

England and southern Scotland. Abrupt changes in composition 

of the fauna occur in most sections and reflect the abrupt lithologic changes caused by complex intertonguing of members and 

by lateral change within members.

Fossil collections are not uniformly distributed. Of all fossil 

localities, more than 25 percent are in southeastern Idaho, and 

more than 30 percent of all collections come from the Meade 

Peak Member in that area. More than 50 percent of the collections are from the Meade Peak Member. About 15 percent 

come from the Park City Formation; the Shedhorn Sandstone 

yielded less than 3 percent.

Almost all fossils here treated in the Phosphoria rock complex have been described previously. In this work species have 

been assigned to genera currently recognized, but no formal 

taxonomic revisions are undertaken. Most of these fossils are 

not well preserved, and their detailed study would not advance 

systematics.

The fossils of the Phosphoria rock complex are of limited 

diversity when compared with those in slightly older rocks of 

the midcontinent region and strikingly limited when compared 

to faunas of equivalent age from western Texas. Fusulinids and 

echinoids are absent. No trilobites are found in rocks unequivocably assigned to the units studied; only two indisputable 

occurrences of horn corals are known. Crinoid remains are 

scarce and of limited distribution. Most of the fossils are 

mollusks, brachiopods, and bryozoans, in that order of abundance. A few species of mollusks and brachiopods constitute 

the preponderate number of individuals. The fauna is remarkable in that it contains many sponge spicules locally and 

unusually abundant inarticulate brachiopods, cephalopods, and 

fish fragments. The deviations from a more normal fauna 

might be due to the effects of sea water rich in silica and 

phosphate but slightly reduced in salinity.

The brachiopods can be divided into two main groups by 

occurrence. In one group, found only in limestones and calcareous shales, the brachiopods have three main modes of 

life: cemented, attached by a pedicle, and free living. The other 

group, found only in phosphatic shales, contains generally 

smaller specimens that were both free living and attached by a 

pedicle. The mollusks show this division with swimming forms, 

cephalopods, that are characteristic of the "claystones facies" 

and shallow burrowers, scaphopods, that are characteristic of 

"limestone facies." The pelecypods in particular are divided into 

very shallow burrowers and free-living forms. A restricted 

molluscan fauna also occurs south of the brachiopod-bearing 

limestones.

The fossils are associated in 60 characteristic groups. Some 

groups are clearly transported, but most are considered to 

be essentially natural assemblages in situ. There appears to be 

a close correlation between the gross lithologic aspects of the 

matrix and the fossil group present. These observations suggest 

that the distribution of various kinds of animals within stratigraphic units was closely related to the nature of the bottom 

sediments. The distribution of the living organisms as members of epifauna or infauna, as surmised from the interpreted 

functional morphology of the fossil brachiopods and pelecypods, 

further supports this conclusion.

Faunas of the Franson and Ervay Members are similar. The 

few differences noted suggest that the Ervay sea may have had 

a firmer bottom and quieter water. Each member shows an 

eastern or southern restricted molluscan facies. This assemblage 

of bellerophontacean gastropods, shallow burrowing pelecypods, 

and scaphopods is interpreted as an extremely shallow water 

fauna that lived on a calcareous or quartz sand, possibly in 

hypersaline water. Another shallow-water marginal facies of 

large orbiculoid brachiopods and small nuculoid pelecypods is 

found in claystones; possibly the brachiopods clung to seaweed. 

Further west the fauna is more typically marine and shows 

a definite upward progression from bryozoan colonies, through 

cementing and attached brachiopods, into free-living productoid 

brachiopods. This progression is interpreted as reflecting increasing depth and a somewhat softer bottom. The Grandeur

571
572 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

fauna is less well known but seems to have lived in slightly 

turbulent water of normal salinity. It is most similar to the 

free-living productoid fauna of the younger limestone units.

The faunas of the Meade Peak and Retort Members are also 

similar, although the Meade Peak fauna is both more widespread 

and diverse than the Retort fauna. The shale fauna is more 

limited than that of the limestone units, but specimens are much 

more abundant. Orbiculoid brachiopods and small nuculoid peleeypods are found in the marginal facies of the members. 

Thicker sections show a characteristic fauna of nine common 

genera of brachiopods and mollusks. The genera do not all 

occur together, but no clear pattern of distribution can be 

ascertained; the variations may be caused by slight differences 

in the original character of the bottom. The lithology is much 

more uniform than at the margin of the basin; in general, the 

bottom fauna was thought to have been similar to that of a 

Recent mudfiat except that there was a large epifauna and a 

small infauna. The fauna was preyed upon by cephalopods and 

fish, both of which are found in abundance. The fossils are 

extremely well preserved and indicate quiet-water conditions. 

No precise depth figures can be given for this fauna, but a 

maximum of 300 feet is suggested because of the necessity of a 

large volume of shallow water for high organic productivity to 

support the large fauna.

The three chert members contain few fossils except sponge 

spicules. The sponges are interpreted by M. W. de Laubenfels 

as having lived on an ooze bottom at less than 150 feet deep, 

an interpretation being in full accord with the limited additional 

fauna. Locally, near the Idaho-Utah boundary, the Rex Chert 

Member contains lenses of bioclastic limestone rich in crinoid 

debris; several lenses also contain a limited brachiopod fauna. 

These lenses are interpreted as shallow-water banks rising 

above the general level of the Rex sea floor. The banks may 

have restricted water circulation so that the sea to the east 

developed some of the characteristics of a barred basin.

The Shedhorn Sandstone contains few fossils. Most are resistant fish teeth and pelecypod shells, commonly in coquinas. 

The presence of these fossils supports the interpretation of 

the Shedhorn as a beach or near-beach deposit.

In spite of all the fossils examined, the precise age of some 

of the units in the Phosphoria rock complex still cannot be satisfactorily determined; most are common, long-ranging genera. 

There is fairly good evidence that the Grandeur Member is 

equivalent to the Kaibab Limestone, and, through it, the 

Leonard Formation of the standard sequence. There is some 

evidence that the rocks called Grandeur in Montana are older, 

and it may be that some of the rocks called Grandeur in Idaho 

and Wyoming also are not equivalent to the type Grandeur.

In a broad sense the remainder of the Phosphoria rock complex seems to be equivalent to the Word Formation of western 

Texas. The faunas of the Meade Peak and Retort Phosphatic 

Shale Members are virtually identical, and the faunas of the 

Franson and Ervay Members are virtually identical. In all four 

members, the available information on mollusks, particularly 

gastropods and cephalopods, suggests correlation with the upper 

part of the Leonard and the lower part of the Word Formations. 

In all four members, evidence from the brachiopod fauna suggests correlation with the upper part of the Word Formation. 

There is no evidence of Oapitan equivalents in the Ervay, but 

this possibility cannot be ruled out.

The lower chert, Rex Chert, and Tosi Chert Members do not 

contain fossils that may be used to determine age and correlation. Fossils from lenses in the Rex Chert Member suggests 

correlation with the Word Formation. The few mollusks in the

Shedhorn Sandstone suggest correlation with the upper Leonard-lower Word sequence, virtually the same seeming paradox 

as previously mentioned.

More precise information on the age of the various stratigraphic units must await final studies of the western Texas 

faunas. Pelecypods and fish remains are not as well known as 

other groups in the Phosphoria complex rocks, and attention 

should be directed to them as a possible means of clarifying the 

age relations.

INTRODUCTION

This paper is concerned with the geographic and 

stratigraphic distribution of fossils within the Permian 

Phosphoria and related formations cropping out in 

parts of Idaho, Montana, Utah, and Wyoming. Because 

it contains economically important minerals, the Phosphoria Formation has been studied by members of the 

U.S. Geological Survey for over half a century. That 

attention should be directed to the fossil content of the 

beds as well as to detailed measurement and chemical 

analysis has long been recognized.

As a matter of historical interest, the close coordination of section measuring and fossil collecting in the 

Phosphoria Formation preceded the formal beginnings 

of the modern detailed studies (Phosphoria project) 

by about 5 years. Shortly before the entry of the United 

States into World War II, W. W. Rubey, U.S. Geological Survey, recognized the occurrence of vanadium in 

the middle part of the Meade Peak Phosphatic Shale 

Member of the Phosphoria Formation in the so-called 

disturbed belt near Afton, Wyo. During Kubey's investigations, several trenches were dug by hand, and 

later others were dug by bulldozer, to supplement natural exposures. The ephemeral nature of these artificial 

excavations necessitated prompt collection of fossils 

from the trenches. In 1942 and 1943, the late W. H. Hass 

collected in trenches between Cokesville and Afton, 

Wyo. His collections have been examined but are not 

included in this report because they are duplicated by 

later collections and because measured sections of these 

trenches have not been published as yet.

Collections made during fieldwork on the Phosphoria 

project followed this earlier established pattern. Most 

of the fossils were obtained from nonresistant shale 

units. For several years studies were concentrated in 

southeastern Idaho. Most of the emphasis was placed 

on the phosphatic shale members, and few fossils were 

collected from adjacent beds. In later years, adjacent 

limestone, chert, and shale were examined for fossils 

over a larger area.

The bulk of the fossils were collected between 1947 

and 1953, when most of the stratigraphic sections were 

measured. Preliminary stratigraphic data were published on 183 measured sections between 1953 and 1956. 

Fossils were obtained from 107 of these measured sec-
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 573

tions and 15 additional localities. Of the remaining sections, some were never examined by paleontologists, 

others were examined but no fossils were collected, and 

still others were found to be unfossiliferous. A few were 

in well cores and could not be readily collected. After 

the reduction of fieldwork on the Phosphoria project, 

few collections were made from 1954 to 1959.

As a result of this collecting, 1,509 fossil collections 

have been obtained from the Phosphoria and related 

formations. In addition, fossils obtained earlier by W. 

T. Lee, D. D. Condit, Eliot Blackwelder, C. J. Hares, 

and G. R. Mansfield were examined. Faunal lists for 

many of these collections have been published by the 

respective authors. These older collections did not contribute to the taxonomic diversity or add new information regarding the age of the Phosphoria and correlative formations. Because some question must always 

remain about the precise stratigraphic position of these 

earlier collections, they were omitted from this re-' 

port. Also, most of these earlier collections are from, 

areas east of the Wind River Mountains in Wyoming, 

and are thus far removed from the main region studied 

for this report.

The fossil collections on which this report is based 

were made during the fieldwork supported in part by 

the U.S. Atomic Energy Commission.

STRATIGRAPHIC SETTING

The term "Phosphoria rock complex" is convenient 

both for designating the Phosphoria Formation, Park 

City Formation, and Shedhorn Sandstone combined 

and for calling attention to the intertonguing relationships within and among the formations. Because of 

changes in lithology and the intertonguing of the strikingly different rock types, each formation has been divided into two or more members. The formations and 

members are arranged with relation to the central area 

of phosphate deposition in southeastern Idaho.

The Shedhorn Sandstone, primarily the northern 

and northeastern sandstone f acies, is divided into lower and upper members. The Park City Formation, primarily the eastern, southeastern, and southern carbonate facies, is divided in ascending order into the 

Grandeur Member, Franson Member, and Ervay Carbonate Rock Member. The central Phosphoria Formation is divided into a series of interbedded cherts and 

phosphatic shales. In ascending order these are: lower 

chert member, Meade Peak Phosphatic Shale Member, 

Rex Chert Member, cherty shale member, Retort 

Phosphatic Shale Member, and Tosi Chert Member, 

Summaries of the stratigraphy and suggested correlations have been published elsewhere (McKelvey and 

others, 1956,1959).

Because of intertonguing relationships, the stratigraphic terminology is necessarily involved. The member names carry a general lithic connotation, but no 

member has exactly the same lithology throughout its 

outcrop area.

With so many lithologic changes between sections 

and within any one section, the precise stratigraphic 

position of a collection is important. Every attempt has 

been made to relate the fossils accurately to the sections. 

In a few places, there is discrepancy between the presumed lithologic unit of the collection and the matrix 

adhering to the specimens. These variations are indicated in the section "Geographic distribution of 

collections."

Preliminary data on stratigraphic sections are given 

in U.S. Geological Survey Circulars prepared during 

fieldwork (Cheney and others, 1953; Cheney and others, 1954; Cressman and others, 1953; Davidson and 

others, 1953; Klepper and others, 1953; McKelvey, 

Armstrong, and others, 1953; McKelvey, Davidson, 

and others, 1953; McKelvey, Smith, and others, 1953; 

O'Malley and others, 1953; Peterson and others, 1954; 

Sheldon, Waring, and others, 1953; Sheldon, Warner, 

and others, 1953; Sheldon and others, 1954; Smart and 

others, 1954; Smith and others, 1952; Swanson, Cressman, and others, 1953; Swanson, Lowell, and others, 

1953, Swanson and others, 1956), and for part of this 

area, these are the only published sources of information. The circulars do not contain all the member 

names subsequently published, but rarely has there 

been difficulty in equating the informal designations 

used therein with these members.

For other parts of the area, summary reports are 

available. Cheney (1957) has described the stratigraphy of the Phosphoria rock complex in the Uinta 

Mountains and northern Wasatch Mountains of Utah. 

Sheldon (195Y) has described it in northwestern 

Wyoming and Cressman (1955), in part of southwestern Montana. In more detailed works, Sheldon (1963) 

discussed the rock complex in most of western 

Wyoming and a small part of southeastern Idaho, and 

Cressman and Swanson (1964) discussed the rock complex in southwestern and southern Montana. In the last 

two works, the position of collections is indicated in 

descriptions of measured sections and, where possible, 

on columnar sections.

PREVIOUS WORK

For the outcrop area considered, only six earlier 

papers describe or illustrate the more common elements 

of the Permian invertebrate fauna. Of these, Girty's 

(1910) description of fossils, mostly obtained from the 

"cap lime" of the Meade Peak Phosphatic Shale Mem-
574 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

ber of the Phosphoria Formation near Montpelier, 

Idaho, and Branson's work (1930) on fossils from the 

Park City Formation, mostly from the Bull Lake area 

in the Wind Elver Mountains, Wyo., are the most inclusive. White (1876) described a few fossils from the 

Permian of the Uinta Mountains, Utah. Girty (in 

Boutwell, 1912, p. 54, pi. 7") illustrated some species 

from the Park City district, Utah, and subsequently 

described a few others from elsewhere in Utah (Girty, 

1920). Girty (1927) also illustrated and described a few 

species from southeastern Idaho.

Prior to World War II, the late J. S. Williams became interested in problems of the Phosphoria fauna. 

During the war and immediately thereafter, he visited 

and collected with several field parties concerned with 

the formation or its correlatives. Poor health prevented 

his taking an active part in subsequent fieldwork, but he 

had overall supervision of the fossil collecting. He is 

responsible for the age assignments given in recent literature (McKelvey and others, 1959, p. 35-39), but he 

was not able to begin a comprehensive study of the 

fauna before his death.

Since a draft of this manuscript was prepared, 

Ciriacks (1963) instituted a study of the pelecypod 

fauna. Several short papers on minor elements of the 

fauna are cited in the appropriate parts of the text.

ACKNOWLEDGMENTS

I would be remiss if I did not acknowledge the contributions of the geologists who obtained fossils while 

measuring stratigraphic sections. Many of the sections 

studied are not accessible by road, and greater effort 

than normal was required to collect the fossils. In addition to the four associates mentioned in the following 

paragraph, the collectors are K. P. McLaughlin, J. H. 

Peterson, W. R. Record, H. A. Saunders, R. A. Smart, 

J. E. Smedley, R. G. Waring, and Helmuth Wedow.

During the 1959 field season, T. M. Cheney, E. R. 

Cressman, R. W. Swanson, and R. P. Sheldon guided 

me to various measured sections so that I could gain 

some idea of the geography and geology of the area. 

The manuscript has benefited by discussion and criticisms by these and other colleagues, including V. E. McKelvey, who organized and supervised the Phosphoria 

project.

Other colleagues aided in identification of fossils or 

discussed their significance with me. These include 

Richard Cifelli, U.S. National Museum (foraminifers); R. M. Finks, Queens College (sponge spicules); 

K. W. Ciriacks, Pan American Petroleum Corp. 

(pelecypods); J. T. Dutro, U.S. Geological Survey 

(brachiopods); and D. H. Dunkle, U.S. National Museum (fish). R. E. Peck, University of Missouri, kindly

lent specimens described by C. C. Branson for comparison.

Finally, gratitude is expressed to Mrs. Dianne H. 

Van Sickle, who for more than 2 years energetically 

devoted herself to this study. She assisted in all 

phases of the work from the first preparation of fossils 

to the final compilation of data and aided in identification of fish remains. Without her continued effort and 

her meticulous attention to details, this report would 

have been long delayed.

PROCEDURES 

IDENTIFICATION

A major facet of any ecologic study is identification 

of the taxa present. For this study identifications below 

the class level have been confined to brachiopods and 

mollusks; the occurrence of other invertebrates in the 

individual collections is indicated. Preliminary identification of fish remains from Wyoming by D. H. Dunkle 

and D. H. Van Sickle are given elsewhere in this report; 

those from other States have not been studied. The presence of microf ossils has been indicated where they have 

been observed, but no attempt has been made to prepare 

samples to search for them. Unpublished work by K. P. 

McLaughlin suggests that microf ossils are rare; even 

among those that are present, only occasionally are 

specimens well preserved. About a dozen samples of 

dark shale from the Meade Peak and Retort Members 

were examined for pollen by Frank L. Staplin; the 

results were negative (R. P. Sheldon, written commun. 

1961).

Identification of fossils is limited by the state of 

paleontologic knowledge and the preservation of available fossils. Considerable effort has been devoted to 

insuring that each fossil name has been used consistently 

throughout this report. Fossils within each collection 

have been examined a minimum of four times. The fossils were examined twice before preliminary identifications were made. Then more definitive identifications 

were made on the individual specimens. These identifications were then checked by systematically examining 

all fossils thought to belong to the same taxon in order 

that consideration could be given to some of the more 

subjective factors which enter into an identification. 

Finally, fossils which appeared to have anomalous 

stratigraphic ranges were examined for a fifth time.

Four faunal distribution charts for the Phosphoria 

Park City, and Shedhorn Formations in Wyoming, 

Idaho, Utah, and Montana have not been included in 

this paper. The charts have been released for open 

file and may be consulted at the U.S. Geological Survey 

Library in Denver, Colo. Distribution data presented 

in the charts are summarized in table 3 of this paper.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 575

On each of the faunal distribution charts, fossils are 

arranged by phylum and class. Within each zoologic 

class, taxa are listed in inferred phylogenetic sequence 

rather than in alphabetical order. Many of the generic 

names employed by Girty (1910,1920,1927) and Branson (1930) are no longer treated in the broad sense as 

they were by those authors. The generic names currently 

in use have been applied, but beyond that, no effort has 

been made to describe the species or discuss their possible synonymies. A detailed morphologic study might 

lead to the identification of a few more species, but the 

large number of fossils and their generally poor quality 

seem to indicate that such a study is not warranted 

at this time.

Poor specimens seldom advance basic taxonomic information about a fossil group and at the same time are 

more difficult to identify than well-preserved specimens. Unfortunately, the bulk of the specimens from 

the Phosphoria rock complex are of uniformly poor 

quality, so many specimens can be generically identified 

only with question.

The level to which identification has been carried 

provides rough measure of the quality of preservation. 

To cite an example, all the following taxa have been 

used: Cancrinellal sp. indet., Cancrinella sp. indet., 

Cancrinella cf. O. phospTiaticus (Girty) and C. phosphatica (Girty). All the specifically identifiable specimens of Cancrinella have been referred to a single 

species, and probably all the less well preserved specimens also belong to this single species. It seems important to indicate the limits of accuracy of the fossil 

identifications and not to identify fossils to a more precise degree than is warranted. The question mark is 

employed throughout to indicate the quality of preservation, not to question the placement of a species in a 

particular genus.

ABUNDANCE

The abundance of the various taxa of coelenterates, 

brachiopods, and mollusks in each collection is shown 

by standard symbols on these faunal distribution charts. 

Eare (R} indicates from 1 through 5 individuals of a 

taxon; common (6% from Q through 15 individuals; 

and abundant (A), 16 or more individuals. The presence of other taxa in a collection is indicated by an "X" 

because of the obvious difficulty of estimating the number of individuals represented by such incomplete remains as sponge spicules or fish scales.

'More strictly quantitative information on the abundance of the various invertebrates cannot be derived 

from the collections at hand. No general sampling 

scheme was followed for the collecting. Indeed, there is 

as yet no satisfactory scheme for quantitative sampling

269-09-2 68 2

of larger invertebrates in the field. Estimates of abundance, therefore, are based entirely on the collections. 

E. P. Sheldon (written commun., 1961) indicates that 

it is possible for a fossil coquina to be represented by a 

single shell in the fossil collections.

It is not feasible to catalog all the various factors 

that can influence the occurrence of fossils at an outcrop, 

but some of the more obvious ones may be worth noting, 

as they have direct bearing on this study. Not only is the 

kind of fossil present related to the lithology, but there 

is an intimate relationship between the recovery of the 

fossil and the lithology. In general, better and more 

abundant fossils are obtained by collecting those that 

weather free from the matrix than from collecting fossils in pieces of fresh rock. Weathering in turn is influenced by such features as past and present climate, 

chemical constitution of the rocks, and attitude of the 

outcrop.

Some of the most prolific fossil localities in the late 

Paleozoic of North America are in flat-lying argillaceous and calcareous rocks, which are exposed at low altitudes in a moderately moist climate. The Phosphoria 

rock complex meets none of these conditions. At most 

measured sections, the rocks have been intensely folded 

and faulted. Most sections lie at high altitudes where 

climate is severe. Many of the shales are weathered, and, 

as noted earlier, most collections were taken from artificial exposures. Samples of weathered and fresh shale 

look entirely different and are difficult to compare. Furthermore, fresh rock is difficult to prepare, as commonly 

the matrix will not part from the fossil.

Another important factor in collecting is local geography. Not only does this influence the amount of time 

that can be spent at an outcrop, but it bears on what 

samples can be transported from the outcrop. Several 

sections measured and collected are reached conveniently only by horseback. Much smaller fossil collections 

were obtained from these sections than from those 

accessible by car.

Finally, the human factor cannot be discounted. 

Geologists show considerable individual variation in 

their ability to observe fossils at an outerop and to collect them. It has been repeatedly demonstrated that 

even trained paleontologists collecting at the same time 

on the same outcrop will obtain quite different samples of 

the fauna, the selection of the different samples being 

governed in some measure by the collector's interest in 

a particular fossil group. Collecting limestone blocks 

containing silicified fossils is a more objective way of 

sampling the fauna, but even in this procedure, personal bias may influence the collecting. Even if all other 

factors were equal, the variation in collecting technique 

among the several collectors of the Phosphoria rock
576 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

complex fossils would be enough to cast doubt on any 

precise mathematical expression of abundance.

At the same time, there are so many collections available that some of the possible sources of error tend to 

cancel each other. Because the relative abundance of 

the various fossils tends to remain constant among collections from similar stratigraphic sections, considerably more reliance may be placed on the relative abundance of the taxa than might be anticipated from the 

preceding discussion.

ABBANGEMENT OF SUMMABY DATA

To present the fossil identifications, the collections 

have been divided into four unequal groups. Collections 

from Idaho, Montana, Utah, and Wyoming, respectively, are listed in the faunal distribution charts. Preliminary arrangements of collections were attempted by 

using at first the approximate limits of depositional 

basins and later the areas included in geologic reports 

(Sheldon, 1963; Cressman and Swanson, 1964; Cheney, 

1957). These arrangements were rejected finally in 

favor of an arbitrary geographic arrangement, which 

seems to be the most useful method of recording and recovering the data.

The locations of the measured sections or other localities from which fossils were obtained and the arrangement of the sections on each of the four faunal distribution charts is shown in figure 157. Most of the sections 

are identified by numbers corresponding to the lot numbers used in preliminary descriptions of the measured 

sections given in U.S. Geological Survey Circulars 

208-211, 260, 262, 301-307, and 324-327. For parts of 

Wyoming and Idaho, two numbers are given for each 

section. The smaller number corresponds to that used by 

Sheldon (1963, p. 54 56). Localities which are not 

measured sections are indicated by letters. The name 

and number or letter of the locality is given on each 

faunal distribution chart above the fossil collection 

numbers.

Within each section on the distribution charts, collections are arranged in stratigraphic order, the oldest 

to the left and the youngest to the right. Although most 

sections show the collection numbers in numerical order, a few deviate markedly from a simple sequence. In 

some sections, this is a reflection of structural complications observed after permanent numbers had been assigned to the individual collections. In others, it is an 

indication that the section has been sampled more than 

once. At a few sections fossils apparently have been collected from the same bed on more than one occasion; 

each collection bears a separate number. N"o attempt has 

been made to identify these possible re-collections on the 

faunal distribution charts; only where the subsequent

collection was made by the writer is this mentioned in 

the text.

Throughout this report the section number or letter 

is in parentheses after the section name. Section numbers can be distinguished from collection numbers, 

which are also in parentheses, by the fact that, where 

both numbers are given, the collection number follows 

the section number or letter.

The stratigraphic member from which the collection 

was obtained is also shown on the faunal distribution 

charts. For the Montana collections, the member designation of the collections was taken from Cressman 

and Swanson (1964). For many of the Wyoming collections and two of the Idaho sections, the member designations were taken from Sheldon (1963). For some 

of the Utah collections, the member designation is that 

used by Cheney (1957), who (written commun., 1959) 

subsequently indicated the position of the collections 

on the columnar sections. A few member designations of 

a collection given in the measured section published 

earlier in a Geological Survey circular differ from those 

used in these later works, but in this paper the later 

designation was the one used. For the remaining sections 

in Idaho, Utah, and Wyoming, the member designations 

are those given in the section presented in the Geological 

Survey circulars. When no formal member designation 

was given in a section published in a circular, the member was inferred from the informal stratigraphic subdivisions, A through E, used in the circulars. Information on the precise stratigraphic position of each collection is in the register of localities (p. 644), or a source 

is cited there where this information may be obtained. 

A letter abbreviation directly above the collection 

number is used to indicate the stratigraphic member. 

The abbreviations are as follows: W?, Wells Formation 

(in Idaho), G or G?, Grandeur Member of Park City 

Formation; F, Fransoii Member of Park City Formation; UF, upper part of Fransoii Member (in Utah); 

E, Ervay Carbonate Rock Member of Park City Formation; LC, lower chert member of Phosphoria Formation; M, Meade Peak Phosphatic Shale Member of 

Phosphoria Formation; E, Rex Chert Member of Phosphoria Formation; GS, cherty shale member of Phosphoria Formation; Rt, Retort Phosphatic Shale Member of Phosphoria Formation; T, Tosi Chert Member 

of Phosphoria Formation; LS, lower member of Shedhoni Sandstone; US, upper member of Shedhom Sandstone.

Directly above the letter abbreviation of the stratigraphic unit is the number of the fossil category to 

which that particular collection has been assigned. These 

fossil categories consist of 60 different assemblages of 

fossils which are discussed in more detail on p. 591.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 577

The fossil category assigned depends on the faunal content of that particular collection; the numbers assigned 

to adjacent collections naturally may show wide 

variance.

Many details regarding the individual collections 

which may be of interest to those particularly concerned 

with the Phosphoria rock complex are presented near 

the end of this paper. The sections following on ecological, geographical, and geological distribution of the fossils thus contain some generalizations, the reasons for 

which are given subsequently. Details on other collections which have been mentioned by assigned number 

in earlier reports are also discussed near the end of this 

report.

ECOLOGICAL CONSIDERATIONS

The study of past environments is becoming increasingly important in geology. Many diverse observations 

have been successfully applied to interpretation of former environments. Other interpretative methods, particularly in geochemistry, remain to be tested but offer 

promise for the future.

In this paper the two principal approaches to the 

problem of interpretation of former environments are 

through interpretation of presumed functional morphology of the various kinds of animals and through 

characteristic animal assemblages. These approaches 

naturally are colored by other data from observations 

based on stratigraphy, paleogeography, and sedimentation, but such observations are not within the scope 

of this paper. A summary of conclusions has been 

published (Yochelson, 1963).

The general comments on lithology are based almost 

entirely on the matrix adhering to the fossils. Some 

limestones were examined during the 1959 field season, 

but because of the paucity of natural shale outcrops, 

practically no observations were made. Similarly, 

almost all the observations of more strictly sedimentological features the ratio of disarticulated valves to 1 

bivalved specimens, wear of shells, and deformation by 

compaction are based solely on the collected material.

One of the flaws in the suggested interpretations is 

the difficulty of developing a truly quantitative 

approach. The fossils were gathered by several different 

collectors, under a variety of field conditions, from 

many diverse lithologies, and during a time span of 

nearly two decades. Because of the wide variation in 

sampling procedures among the collections and because 

of the lack of a basic theory of fossil sampling, no real 

precision in abundance determination is possible. Instead, it has been necessary to use the standard terms, 

"rare," "common," and "abundant."

On the faunal distribution charts, abundance terms 

are used with numerical values as indicated on page

575. They are used as terms of overall aspect both 

when discussing assemblages and when considering 

abundance of various taxa; the terms should be construed as only semiquantitative expressions. Remarks 

on abundance must be interpreted in the light of the 

limitations under which the collections were made.

At least two different methods may be employed in 

establishing relative abundance among various kinds 

of fossils. One is taxonomic diversity; the second is the 

abundance of individuals in a particular taxon. 

Although the first method may be more precise, the 

second commonly is more meaningful but more difficult 

to establish.

It is characteristic of most of the collections studied 

that two or three kinds of fossils form the bulk of the 

material. Probably less than 5 percent of the total 

number of specimens represent 50 percent of the taxonomic diversity. To count specimens and thus provide 

proof of such a statement, however, would consume an 

inordinate amount of time.

FAUNAL ELEMENTS

Even though a few closely related Recent species live 

in strikingly different habitats, most living animals 

that are closely related occupy similar ecological niches. 

This fact provides one of the main supports for three 

interpretations of paleoecology: (1) The former ecology may be directly interpreted from the ecology of 

closely related living species and genera, (2) the former ecology may be inferred from the presence of fossils similar to, though not closely related to, Recent 

forms, and (3) although it may not be possible to 

interpret directly the ecological requirements of the 

fossils, distribution of the different kinds of animals 

and other observations can provide comparative data 

which may form the basis for a logical interpretation 

of ecology.

In the following discussion miscellaneous observations within these three general categories of interpretation are compiled. Because the intent is to focus 

attention on the individual genera where possible, the 

information is presented in approximate phylogenetic 

order by phyla and classes.

The overall fauna of the Phosphoria rock complex 

is somewhat unusual. The fauna is dominated by 

brachiopocls and mollusks which have remarkably little 

taxonomic diversity; relatively few genera are present 

and most are represented by many specimens of a single 

species. Bryozoans, an important subsidiary constituent, have not been studied, but again one gains the 

impression from the external appearance of the colonies 

that there is only limited diversity. Fusulinids and 

trilobites appear to be absent from the fauna. Corals
578

114 C 113 C 112 C 111' 110° 109° 108°

40

20 10 0 20 40 60 80 100 MILES 

i i i____i____i____i______i____i
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 579

are scarcely represented. Echinoids are absent and 

crinoid debris is limited.

The fauna is clearly unbalanced in favor of brachiopods and mollusks when compared with the slightly 

older fauna from Kansas (Mudge and Yochelson, 1962) 

that must have lived under 'conditions 'somewhat similar 

to those found in the marginal deposits of the Phosphoria rock complex. The limited diversity is in striking contrast to the rich faunas known from rocks of 

similar age in western Texas.

Other differences from more characteristic late Paleozoic faunas should be noted. Inarticulate brachiopods 

are extremely abundant and cephalopods are fairly

FIG DKB 157. Distribution of sections from which fossils were collected 

for this report. Within each State the sequence of sections used on 

faunal distribution charts is shown by arrows. Numbers and letters 

refer to the following sections and localities: 2(1368) Red Creek, 

Wyo.; 4(1369) Forellen Peak, Wyo.; 37(1353) Bear Creek, Idaho; 

39(1338) Fall Creek, Idaho; 41(1327) Togwotee Pass, Wyo.; 42 

(1326) Gros Ventre Slide, Wyo.; 44(1323) Crystal Creek, Wyo.; 

47(1375) Hungry Creek, Wyo.; 49(1370) Teton Pass, Wyo.; 50(1335) 

Flat Creek, Wyo.; 56(1333) Tosi Creek, Wyo.; 57(1324) Hoback, 

Wyo.; 60(1332) Buck Creek, Wyo.; 66(1334) Bartlett Creek, Wyo.; 

67(1352) Steer Creek, Wyo.; 68(1329) Burroughs Creek, Wyo.; 75 

(1325) Dinwoody Lakes, Wyo.; 79(1336) South Fork of Gypsum 

Creek, Wyo.; 82(1328) Bull Lake, Wyo.; 107 (1380) Deadline Ridge, 

Wyo.; 108(1379) Fontenelle Creek, Wyo.; 110(1378) Wheat Creek, 

Wyo.; 124(1330) Conant Creek, Wyo.; 147(1346) Cumberland, Wyo.; 

1200 Conda mine, Idaho; 1201 Coal Canyon, Wyo.; 1202 Layland 

Canyon, Wyo.; 1203 Brazer Canyon, Utah; 1204 North Fork of Pine 

Creek, Wyo.; 1205 Middle Fork of Pine Creek, Wyo.; 1206 Trail Canyon, Idaho ; 1207 Montpelier Canyon, Idaho ; 1208 West Dairy, Idaho ; 

1209 Johnson Creek, Idaho; 1210 Mabie Canyon, Idaho; 1211 South 

Dry Valley, Idaho; 1219 Brush Creek Gorge, Utah; 1220 Rock Canyon, Utah ; 1221 Little Brush Creek, Utah; 1222 Dalys Spur, Mont.; 

1224 Big Sheep Canyon, Mont.; 1228 Upper Brazer Canyon, Utah; 

1229 Dry Canyon, Utah; 1230 North Wooley Range, Idaho; 1231 

Wolf Creek, Utah; 1232 South Rasmussen, Idaho; 1233 North 

Rasmussen Valley, Idaho; 1234 Sheep Creek, Mont.; 1235 Lake 

Fork, Utah; 1241 Sawtooth Mountain, Mont.: 1246 Wadhams 

Spring, Mont.; 1249 Kelley Gulch, Mont.; 1256 Cedar Creek, 

Mont.; 1257 Cave Creek, Mont.; 1258 Kendall Canyon, Idaho; 

1259 North Dry Valley, Idaho; 1260 Caldwell Canyon, Idaho; 

1261 Blackfoot Narrows, Idaho; 1262 Woodall Creek, Idaho; 

1264 West Georgetown Canyon, Idaho ; 1265 Swan Lake Gulch, Idaho ; 

1266 Paris Canyon, Idaho; 1267 East Georgetown Canyon, Idaho; 

1268 Deer Creek, Idaho; 1270 Wanrhodes Canyon, Utah; 1271 Right 

Fork of Hobble Creek, Utah; 1289 Cokeville, Wyo.; 1290 Laketown 

Canyon, Utah; 1292 North Crawford, Utah; 1293 Dingle, Idaho; 

1294 Little Sheep Creek, Mont.; 1296 Crooked Creek, Mont.; 1298 

Lone Pine Springs, Idaho; 1299 Hogback Mountain, Mont.; 1300 

Warm Springs Creek, Mont.; 1301 Sliderock Mountain, Mont.; 1302 

West Fork of Blacktail Creek, Mont.; 1303 Pole Canyon, Idaho; 1304 

Rocky Canyon, Idaho; 1306 South Stewart Canyon, Idaho; 1307 

Alpine Creek, Mont.; 1308 Gravel Creek Divide, Idaho; 1309 Henry, 

Idaho; 1310 Timber Creek, Idaho; 1311 Canyon Camp, Mont.; 1314 

Enoch Valley, Idaho; 1316 Ballard Trench, Idaho; 1317 Hot Spring, 

Idaho; 1322 Wolverine Canyon, Idaho; 1331 Poison Creek, Wyo.; 

1339 Horseshoe Canyon, Utah ; 1341 Little Water Canyon, Mont.; 1345 

Devils Slide, Utah ; 1347 Franson Canyon, Utah; 1350 Fort Douglas, 

Utah; 1351 Mud Spring, Idaho; 1355 Jefferson Canyon, Mont.; 1357 

Sappington Canyon, Mont.; 1358 North Big Hole Canyon, Mont.; 

1359 Canyon Creek No. 3; Mont.; 1363 Cinnabar Mountain, Mont.; 

1366 La Marche Gulch, Mont.; 1367 Logan, Mont.; 1371 Strawberry 

Valley, Utah ; 1372 Snowdrift Mountain, Idaho; 1381 Basin Creek, 

Wyo.; 1385 Waterloo Phosphate pit, Idaho; A, Crawford Mountains, 

Utah ; B, Dry Bread Hollow, Utah; C, Cephalopod Gulch, Utah; D, 

Mill Creek, Utah; E, Geneva Steel Company Pit, Utah; F, Blind 

Stream, Utah; G, Bennett Ranch, Utah; H, Coulter Ranger Station, 

Utah; J, Split Mountain, Utah; K, divide between Trail and Wood 

Canyons, Idaho; L, South Fork of Sage Creek, Idaho; M, Big Timber, 

Mont.; N, Grizzly Creek, Idaho; O, North Stewart, Idaho.

common. Disarticulated fish remains have been preserved in remarkable profusion. Sponge spicules are 

present locally in astronomical numbers. Thus, the 

fauna of the Phosphoria rock complex is unusual because of the presence or absence of certain fossils.

Such differences are difficult to interpret. The uniform nature of the fauna over such a large area suggests that these differences might be caused by some 

differences in the sea water. An abundance of silica 

and phosphate, or a slight reduction in salinity, which 

would be returned to normal salinity by evaporation 

in shallower waters, might explain the differences. 

Similarly, the fauna might have been limited because of 

low water temperature. Although the faunal evidence 

does not allow one to discriminate between these two 

possibilities, the paleogeographical evidence tends to 

substantiate the latter alternative (R. P. Sheldon, 

written commun., 1961). In Recent faunas, lack of diversity but abundance of individuals is taken to indicate 

less than optimum conditions for life; certainly these 

are the principal attributes of the Phosphoria fauna.

PROTOZOA

Although a discussion of microscopic fossils is not 

within the scope of this paper, two observations are 

worth noting. The first is that the few occurrences of 

benthonic foraminifers noted in the faunal distribution chart in no way indicate the relative abundance of 

these animals. Emigh (1958, p. 17) and Cressman and 

Swanson (1964) remark that in certain areas of phosphate accumulation, foraminifers commonly are the 

nuclei for phosphate oolites.

The second point is a negative one. During 1959, the 

locality near Three Forks, Mont., from which fusulinids were reported by Frenzel and Mundorff (1942), 

was reexamined by R. W. Swanson and the writer who 

found no specimens. Because the thin conglomerate from 

which Frenzel and Mundorff gathered their specimens 

was interpreted as being below the base of the Phosphoria interval, the only reported occurrence of fusulinids in the Phosphoria Formation was exempted from 

consideration. Dr. Alan McGugan (oral commun., 

1965), however, indicates that fusulinids may occur 

about 15 feet above this conglomerate.

Because of the stratigraphic importance of the fusulinids, considerable time was devoted to a search for 

them when sections were measured and collected. Later, 

some of the limestone matrix was examined for fusulinids by means of a binocular microscope. During identification almost all larger fossils were examined with 

the aid of a hand lens, and another search was made for 

fusulinids. In spite of close examination of the matrix 

rock, no fusulinids were found. Their absence to date 

thus can be taken as significant.
580 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

Fusulinids are abundant elsewhere in Permian rocks 

of equivalent age both to the northwest in British 

Columbia and the southeast in Trans-Pecos, Tex. Their 

absence from the Phosphoria rock complex is in someway related to local conditions of deposition.

PORIFERA

The abundant sponge spicules in the Rex Chert Member have been discussed in detail by Cressman and 

Swanson (1964, p. 315-317). In addition to the common 

lithistid spicules reported by M. W. de Laubenfels (in 

Cressman and Swanson (1964, p. 371), Dr. R. M. Finks 

(oral commun., I960), Department of Geology, Queens 

College, has reported the presence of hexactinellid 

sponge spicules in the Rex chert.

The single specimen of Haplistion, the only complete sponge found within the collections studied is believed to be from beds older than the type locality of 

the Grandeur Member. Finks, Yochelson, and Sheldon 

(1961) have reported the occurrence of Actinocoelia 

maeandrina at one locality in the Franson Member 

near DuBois, Wyo. Except for this occurrence, complete sponges are not known from the Phosphoria rock 

complex.

On the one hand, the profusion of isolated spicules 

within the cherts is unusual when compared with the 

number of isolated spicules in other cherts in North 

America. On the other hand, the absence of complete 

sponges is almost as remarkable because large diverse 

faunas have been found in western Texas (Finks, 1960).

COELBNTERATA

Two of the four occurrences of solitary corals are 

from beds that may be older than the type Grandeur. 

However, at Sawtooth Mountain, Mont. (1241) (10854), 

a single coral occurs with abundant bryozoan and pelecypod fragments in the Franson Member. At the 

South Fork of Sage Creek (L) (19532), three small 

corals are associated with a large fauna of brachiopods 

and crinoid columnals, in the limestone lens within the 

Rex Chert Member. A few small corals also occur in 

northeastern Nevada.

As is true of the sponges, the virtual absence of corals 

is remarkable. Corals are common in some limestones 

lithologically similar to the Franson and of slightly 

older age in the midcontinent region, but they are by no 

means rare in rocks of equivalent age in western Texas. 

The rarity of corals in the Phosphoria rock complex 

has 'been commented on by Duncan (1961).

Conularids, currently placed with the coelenterates, 

are equally rare in the collections listed. Collections 

not reported on here show that they are more abundant, 

but still rare, in the Meade Peak Member. A few specimens occur in both older and younger limestones to

the east. None of the specimens are complete enough to 

determine whether they were attached or free floating 

during life.

ECHINODERMATA

Crinoid steins are widely distributed throughout the 

Phosphoria Formation and its equivalents. Within the 

Grandeur Member in Montana and Idaho they are 

common to abundant in rocks which appear to be older 

than the type Grandeur, but they do occur sparsely in 

the type section in Utah and in other nearby sections.

There are four known occurrences of crinoid stems 

in the Meade Peak Member south of Salt Lake City, 

Utah, but only a few isolated ossicles are involved. Recent crinoid ossicles will float for some time (A. L. 

Bowsher, oral commun., 1960), and it is possible that 

these drifted in from another area. A single report of 

crinoid remains in the Retort Member in Wyoming 

is based on a collection which may actually have come 

from the Ervay Member.

Crinoid remains are sparse in the Franson Member in 

Montana and Utah but are more common in Wyoming, 

particularly in the Wind River Mountains area. The 

few listings of crinoid stems in the Rex Chert Member 

are based on occurrences within limestone lenses. In the 

"upper Franson" * of Utah and the Ervay Member of 

Wyoming, crinoid stems are present. Although in 

Wyoming the Ervay specimens occur at fewer localities 

than in the Franson, they are numerically almost as 

common.

If one ignores the pre-Grandeur occurrences, the only 

places where crinoid stems are abundant are in the 

limestone lenses within the Rex Member in Idaho and 

Montana. Cursory field examination of some of these 

lenses indicates that they are significant rock formers 

and constitute as high as 50 percent of the total rock 

volume. Some of these limestone lenses contain only 

crinoid ossicles and were not sampled. Others, such as the 

South Fork of Sage Creek, Idaho (L), also contain an 

abundant brachiopod fauna.

At almost all localities where they occur, the crinoids 

are represented by isolated ossicles. Stem fragments as 

much as 1 centimeter long are rare; most of these longer 

fragments are in the Ervay Member on the east flank 

of the Wind River Mountains. Only one calyx plate was 

found in the "upper Franson" (12623) at the Right 

Fork of Hobble Creek, Utah. Branson (1930, p. 24) reported a partial calyx from Bull Lake, Wyo.

Branson (1930, p. 24) also reported a single echinoid 

spine and a single plate from the upper part of the 

Franson Member at Bull Lake, Wyo. No echinoid re1 The informal term "upper Franson" is used here to denote the upper 

part of the Franson Member of Utah, which may include equivalents 

of younger members distinguished elsewhere in the report area. (See 

p. 635.)
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 581

mains have been found in any of the collections studied. 

Branson's specimens were not figured, and his report 

cannot be confirmed.

Although the absence of specimens of other classes 

of echinoderms is not surprising because of their rarity 

elsewhere in the upper Paleozoic, the absence of echinoids is unexpected. In rocks of equivalent age in westem Texas, echinoids are locally abundant. They are 

widespread in Kansas (Mudge and Yochelson, 1962, 

p. 73) in rock types that resemble the eastern facies of 

the Franson and Ervay Members. Though negative 

evidence never can have the force of positive evidence, 

the many collections examined allow one to attach considerable significance to the absence of echinoids. Some 

significance can be attached to the rarity and limited 

distribution of crinoid remains.

Hyman (1955, p. 564) remarks "echinoids have 

practically no power of ionic regulation * * * ." Living echinoderms as a whole are virtually limited to 

waters of normal salinity. The echinoids in particular 

seem almost never to be found in situations that vary 

from normal salinity. Because of the uniform physiological reactions of the Recent animals, it seems logical to postulate that fossil forms were equally restricted. 

Living crinoids are also restricted to marine waters 

(Hyman, 1955, p. 11-115).

BRYOZOA

No attempt was made to study the Bryozoa except 

to record the presence of specimens in two general 

growth forms. It is recognized that several genera are 

included within each growth form. Branson (1930, 

p. 24) distinguished five genera in the Wind River 

Mountains area without making an exhaustive study 

of the group.

The fenestrate growth forms occur at about onefourth of the localities at which the ramose forms occur. At most localities fenestrate forms occur with 

ramose forms and are in the minority. At a few 

localities, some of which may be older than the 

type Grandeur, fenestrate forms are in the majority 

or are the only bryozoans present. Although there are 

a few scattered occurrences in other States and in other 

stratigraphic units, most fenestrate bryozoans occur in 

the Franson and Ervay Members in the Wind River 

Mountain area of Wyoming. Fenestrate forms are more 

common in the latter unit and at some localities are almost as abundant as the ramose forms. When one compares the number of collections available from each 

unit, fenestrate forms are much more common in the 

Ervay than in the Franson. Large fragments of fenestrate colonies occur locally in the Ervay Member; small 

pieces occur mostly in the Franson.

The ramose growth form includes, among other kinds, 

both thin, twiglike rhomboporoid bryozoans and more 

massive stenoporoid forms. Casual observation suggests that most bryozoans of the Ervay Member are 

more massive than those of the Franson. Within the 

Franson Member, ramose bryozoans are most abundant 

in Wyoming, less common in Montana, even less common in Utah, and rare in Idaho. They are more abundant in the "upper Franson" of Utah than in the Ervay 

of Wyoming. Some occurrences of rhomboporoids in 

the Ervay appear to be in growth position. Conversely, 

many of the smaller bryozoans in the Franson, particularly in collections where brachiopods are abundant, 

are small fragments.

Bryozoans are characteristic of the Franson and 

Ervay Members, but practically none occur in the type 

area of the Grandeur Member. In Montana some bryozoans occur where the rocks are thought to be older 

than type Grandeur. Of the few pre-Meade Peak occurrences, some in Wyoming and Idaho may be preGrandeur. There are a few bryozoans in the limestone 

lenses of the Rex Chert Member.

In chert and phosphatic shale, the sporadically scattered bryozoans occurrences are invariably found as 

small fragments or in a limestone matrix. Small fragments suggest transportation from another area, and 

the limestone matrix suggests that the stratigraphic unit 

is incorrectly designated. Similarly, none of the few 

occurrences of bryozoans in the Shedhorn Sandstone 

give convincing evidence of being buried in place. Several samples are such small fragments that they almost 

certainly have been transported.

Most bryozoans in the formations here considered 

occur in dense limestones. For the most part, they are 

distributed in a rudely semicircular belt of outcrop 

intermediate in position between cherts and phosphatic 

shales which occupy the center of the basin and the 

shoreward Flagioglypfa-bearing limestones. They are 

most abundant in the Crawford Mountains of Utah and 

the Wind River Mountains of Wyoming. Available collections indicate that bryozoans are relatively more 

abundant in the Ervay Member and its equivalents than 

in the Franson.

Duncan (1957, p. 783-790) in a summary article points 

out that bryozoans are most common in impure calcareous clastic facies, the manner characteristic of their distribution in the Phosphoria complex. These animals are 

marine and require either a hard nonshifting bottom or 

a well-anchored hard object in a soft or shifting bottom 

for attachment of larvae. Many fossil bryozoans are 

thought to have lived in less than 200 feet of water.
582 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

BRACHIOPODA

Brachiopods as a group are almost as abundant as 

the mollusks, although they are slightly less diversified 

taxonomically. Although inarticulate brachiopod individuals are about as abundant as the articulates, the 

taxonomic diversity of the articulates is about 10 times 

greater.

INARTICULATA

Lingula and Orbiculoidea have been recognized in 

the Phosphoria rock complex. Because Lingula has persisted to the Eecent and its life habitat can be studied, 

considerable importance is often attached to its occurrence as a fossil. It has been thought to be an indicator 

of warm shallow water (Allan, 1936, p. 383-385). 

Depth ranges of 0-10 fathoms are recorded, but most 

Eecent occurrences are in less than 20 feet of water. 

Lingula^ unlike most other brachiopods, is a member of 

the infauna that moves up and down its burrow by use 

of its large pedicle.

Lingula^ occurring in about 40 collections, is quite 

rare in the Phosphoria. Seldom is it represented by 

more than a few specimens. A few specimens of Lingula 

occur in sandstone suggestive of a beach or near-shore 

deposit. A few others occur as minor faunal elements 

in an epifauna composed of small brachiopods and 

pectenoid pelecypods. Most Lingula are found in the 

Meade Peak Phosphatic Shale Member. They are commonly associated with Orbiculoidea but are represented 

by only one or two specimens at a locality. These sporadic occurrences in the Meade Peak Member are more 

common in Utah than they are in Wyoming or Idaho.

Orbiculoidea is in marked contrast to Lingula. 

Whereas Lingula is one of the rarest fossils, Orbiculoidea is the most abundant fossil in the collections. In 

more than 10 percent of the collections this fossil is 

the exclusive or predominate faunal element; in many 

other collections it is abundant.

Orbiculoidea occurs in three somewhat different geologic settings. Probably the largest number of shells 

occur in the "fish-scale marker bed," a phosphorite commonly a few inches to a foot thick near the base of 

the Meade Peak Member. This bed occurs throughout 

most of the commercially productive phosphate area in 

Idaho and Utah. Most of the rock is composed of organic debris, virtually all of which is fragments of 

Orbiculoidea. At Bear Creek, Idaho, this bed is about 

11 feet thick and is the richest phosphorite found averaging 34 percent P2O5 (E. P. Sheldon, written commun., 1961). Fish scales occur in the marker bed, but 

they are not common. The number of Orbiculoidea involved is impossible to estimate but is astronomical. 

Scattered occurrences in sandstone should be mentioned 

here because almost all of them are fragments. Most

specimens are too incomplete for identification, but the 

large size of occasional fragments suggests that some 

of the specimens might be O. (Roemerella] utahensis.

Orbiculoidea occurs in fewer numbers elsewhere in 

the Meade Peak and Eetort Members. In this second 

geologic setting, it is scattered throughout much of the 

shales. It is found both alone and in association with 

Crurithyris, Chonetes, and Leiorhynchus but almost 

invariably is less abundant than any of the articulate 

brachiopods with which it may occur. It is also common 

in dark fine-grained limestones such as the "cap lime" 

within the Meade Peak Member. In the limestones, 

Orbiculoidea most commonly is associated with 

Streblochondria or Babylonites but again usually is not 

the most abundant fossil.

The orbiculoids that can be specifically identified in 

the phosphatic shales and fine-grained limestones have 

been referred to O. (O.} missouriensis, a smaller and 

higher species than O. (Roemerella) utahensis. Both 

valves are preserved at many of the localities where 

Orbiculoidea is abundant.

The third general environment for Orbiculoidea is 

marginal to the area of thick phosphate deposition. In 

the Wind Eiver Mountains area of Wyoming and the 

Uinta Mountains area and central Wasatch Mountains 

area of Utah, Orbiculoidea is common in thin claystone 

beds occasionally associated with small nuculoid pelecypod and gastropod steinkerns. The rocks are commonly 

light colored and shaly weathering. These occurrences 

are typical of the Franson, but a few are known from 

the Ervay. Although the total number of specimens is 

less than in the second type of occurrence within the 

phosphatic shales, there are more specimens of Orbiculoidea than of any other single brachiopod genus within the limestone sequence.

The majority of specimens in the Franson Member 

have been identified as O. (Roemerella) utahensis. Most 

specimens are about the size of a quarter. As the 

brachial valve is almost invariably missing, the large 

subcentral pedicle slit is readily observable, and the fossil can be readily identified.

The circular shape and position of the pedicle in 

Orbiculoidea is markedly different from that in Lingula. There seems to be no doubt that Orbiculoidea was 

a member of the epifauna rather than the infauna. 

However, it is difficult to visualize such a flat shell remaining on the bottom without being buried by sediment. Even Chonetes, because of its slightly curved pedicle valve, was raised a few millimeters above the bottom.

Euedemann (1934, p. 33) suggested that many of the 

inarticulate brachiopods found associated with graptolites in black shales were originally attached to floating 

seaweed. He noted that most of the shells were thin and
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 583

fragile, quite in contrast with the Orbiculoidea found 

in the Permian beds. In spite of this difference, the 

hypothesis is worth serious consideration.

Two sedimentological features of the phosphatic 

shale members which seem difficult to explain are the 

relatively high percentage of organic matter and the 

local abundance of rare metals, particularly vanadium. 

Two peculiarities of the fossils in these shales are the 

long vertical range of Orbiculoidea within the members 

and its occurrence with several different mollusks and 

brachiopods. This widespread vertical and lateral distribution does not characterize any of the other fossils 

studied. Dense growths of seaweed floating on the surface or rooted like the modern kelp might be the explanation for several of these seemingly unrelated and 

anomalous features. However, in the absence of seaweed 

remains, the hypothesis can only be tentatively suggested and must be tested by geochemical studies.

It is worth emphasizing that the abundance of Orbiculoidea must be directly related to the abundance of 

phosphate in the sea water from which the animals 

could extract this shell-building material. Abundant 

Orbiculoidea seemingly are the result of phosphate concentration. Only indirectly and to a minor degree, as in 

the "fish scale beds," are they the direct cause of its 

economic accumulation.

ARTICULATA

The articulate brachiopods may be subdivided arbitrarily into two groups on the basis of occurrence. These 

groups are not phylogenetic. One group characteristic 

of the Franson and Ervay Members may be considered 

"limestone" fossils. The fossils of the Grandeur Member, although somewhat different, fit moderately well 

here. The second group, which characterizes the Meade 

Peak Member and to a lesser extent the Retort Member, 

consists of "claystone" fossils. No overlap exists between 

these groups. None of the "claystone-facies" brachiopods 

have been observed in the limestones. The few occurrences of "limestone-f acies" brachiopods in the claystone 

may be explained either as reworked fossils or a fauna 

from a thin limestone tongue that has not been recognized within the claystone. These exceptions have been 

mentioned in the section on geographic distribution.

The few collections from the chert members which 

contain brachiopods are in an atypical nonchert matrix. 

These exceptions are also discussed under geographic 

distribution.

The limestone facies includes essentially all brachiopods taxa except Crurithyris, Leiorhynchus, Cancrinella, and Ghonetes. Some chonetids occur in the Grandeur and pre-Grandeur rocks and a few are present in 

the Franson and Ervay Members, but they are different 

species and are so rare outside of the phosphatic shales

that they can be ignored. The "limestone-facies" fossils 

occur at less than half as many localities as the "claystone-facies" fossils. Less than one-fifth the number of 

specimens are involved in the limestone facies, in part 

because many of the "limestone-facies" fossils are larger 

than those in the claystone.

In this facies the productoids are about as abundant 

as all the other brachiopods combined. Echinauris is 

commonest, Bathymyonia is less common, and most of 

the remaining productoids combined are about as numerous as Bathymyonia. In this third group of productoids, 

Muirwoodm and Sphenosteges are most abundant.

Among the nonproductoids, Derbyia is probably the 

most common, followed closely by Neospirifer. Spiriferina is much less common. Composite, Hustedia, Wellerella, and Rhynchopora occur in about that order of 

frequency but together form only a small part of the 

brachiopod fauna.

Although all "limestone-facies" brachiopods were 

members of the epifauna, at least three fundamentally 

different modes of life are represented by these genera. 

Some of the brachiopods were cemented to one spot during life. The irregular interarea and frequently irregular growth of the body of the shell show that Derbyia 

was directly attached. Sphenosteges early in its life 

was attached and possessed anchoring spines (MuirWood and Cooper, 1960, p. 40). Leptodus, known from 

one locality in Montana (Dutro and Yochelson, 1961), 

attached itself much like a Recent oyster.

Attachment implies a hard substrate; mature shells 

indicate a sedimentation rate that did not prevent the 

animal from growing. It is possible that these animals 

were attached to bryozoan colonies, algal growth, biohermal masses, or other bodies some distance above the 

bottom, but there is no evidence to suggest attachment 

other than to the sea floor.

Other brachiopods were attached by a restricting 

pedicle, but the shell may have swayed with the local 

current. /Spiriferina, Composita, Neospirifer, and 

Rhynchopora 'all have moderate to large pedicle foramina and presumably were attached throughout life by 

a pedicle. The living representatives of the rhynchonellids suggest by inference that Wellerella and Hustedia 

were attached throughout life. Attachment by a pedicle 

might require a fairly firm bottom or at least the presence of hard objects such as pebbles on a shifting bottom. However, Cooper (1957a, p. 801) directs attention 

to the possibility that some Paleozoic brachiopods may 

have developed a long, slender pedicle having a frayed 

rootlike end for providing purchase in a soft bottom. 

Other possible adaptations for life on a softer bottom 

are the deeply convex pedicle valve of Composita and 

the strongly plicated shell and small size of WellereUa
584 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

and Rhynchopora, each of which would have helped prevent the shell from sinking into the mud. As long as 

the line of juncture of the valves was above the sediment-water interface, the animal could continue to live.

With the exception of Sphenosteges and possibly 

Sphenalosia, the remaining productoids are thought to 

have been unattached. Muir-Wood and Cooper (1960, 

p. 43^t6) have discussed the ecology of the productoids 

and have demonstrated that many lived free during 

most or all their lives. The spines were adaptations to 

raise the anterior margin of the shell above the bottom. 

Different spine patterns imply slightly different modes 

of life. The long spines on the ears of Kochiproductus 

may have held the shell firmly in one place; the two 

long spines on the ears and two anterior to the point of 

geniculation of Muirwoodia seem to be adaptations for 

life on a muddy bottom. The details of correlation of 

spine pattern and habitat remain to be worked out but 

should provide a useful tool for further ecological investigations. While Muir-Wood and Cooper have shown 

that certain western Texas Permian productoids have 

lived above the bottom with spines entwined in bryozoaus colonies, there is nothing to suggest this in the 

Phosphoria faunas. The productoids, like the pedicleattached brachiopods, were directly influenced by the 

bottom.

Because many individuals of Neospirifer are badly 

worn in contrast to other genera, the shells may have 

been rolled or otherwise abraded or eroded on the sea 

floor after death. There is also the possibility that in 

late stages, they may have lost the pedicle and lived 

free. Neospirifer is further atypical in that a relatively 

large number of shells show spindle-shaped borings. 

Some of these borings are on the interior of the shells; 

possibly all occurred after death of the animal.

Characteristically, the brachiopods only occur in 

generally clear-cut limited assemblages. However, there 

are a few exceptional collections in which almost all 

of the "limestone-facies" brachiopods occur. Some of 

these collections were made through a few feet of strata; 

several include fossils in slightly different matrixes.

The first of these assemblages is that of Derbyia and 

Spiriferina. It is perhaps overstating the case to consider this as an assemblage as the genera also occur 

separately in almost as many collections as they do together. Another assemblage is that of Neospirifer and 

Sphenosteges.

The productoids seldom occur with other brachiopods. Although there is some overlap among them three 

assemblages can be distinguished. Squamaria and Rugatia characteristically occur together. Echinauris, to 

some extent Anidcmthus, and the rare "Liosotella" also* 

seem to be associated. Finally Bathymyonia and Muirwoodia may occur either together or in associated collections. Echinauris frequently is found with these two 

genera. A few collections contain nonproductoids exclusively, but for the most part, they are rare associates 

of the productoids.

Derbyia and Spiriferina seem to occur most commonly in massive limestones; other brachiopods occur in 

more shaly limestones. If one ignores the limestone 

lenses in the Rex Chert and Grandeur Members, there 

appears to be a rough correlation between increasing 

size of productoid brachiopods and increasing shaliness 

of the matrix.

Within the claystoiie facies, all brachiopods are 

abundant in the beds in which they occur. None show 

evidence of current sorting. Chonetes is the most abundant genus, followed in order by Crurithyris, Leiorhynchus, and Cancrinella, the last genus being about half 

as common as the first. That some Chonetes have tiny 

hinge spines preserved indicates virtually no movement 

after death. Other instances of excellent preservation 

are known, but most fossils are poorly preserved because 

of diagenetic changes.

The wide shell and the hinge spines of Chonetes seem 

to be special adaptations to keep this small animal from 

sinking into a soft bottom sediment. The proximity of 

the anterior commissure to the bottom is suggestive of 

clear, sediment-free water throughout most of the life 

of the brachiopod. Occurrences of Chonetes as the only 

articulate brachiopod in a collection, are about as common as its combined occurrences with other articulate 

brachiopods. Chonetes also occurs with Crurithyris 

about twice as commonly as in a Cancrinella-Chonetes 

assemblage.

Because of the large size of its pedicle opening, it is 

likely that Crurithryis was attached by a pedicle at 

maturity. The deeply convex pedicle valve and numerous small spines seem to be excellent adaptations to prevent the animal from sinking into the bottom. In addition to its occurrence with Chonetes, in a few collections 

Crurithyris is associated also with Leiorhynchus. However, it, like Chonetes, is slightly more common as the 

only articulate brachiopod in a collection.

In Leiorhynchus, the pedicle opening is somewhat 

smaller than in Crurithyris. Because the foramen is 

not restricted, it seems likely that this genus was permanently attached by a pedicle. The triangular ribbed 

shell is so fundamentally different from that of Crurithyris that a somewhat different life habit is implied, 

but, it is not clear what this habitat could have been. 

Leiorhynchus occurs with Chonetes about as often as it 

occurs as the only articulate brachiopd in a collection. 

It does occur occasionally with Crurithyris and rarely 

with both genera.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 585

Like the other productoids, Cancrinella at maturity 

was not attached by a pedicle. The relatively large size 

of specimens, the strong curvature of the pedicle valve, 

and the few long spines seem to be excellent adaptations 

toward raising the anterior from the bottom. They are 

suggestive of a bottom which may have been softer than 

that which supported the other brachiopods of this 

facies. Conversely, its occasional occurrence with 

Glionetes suggests a slightly firmer bottom at those 

localities. Cancrinella characteristically is the only articulate brachiopod where it occurs. It does not occur 

with Crurithyris or Leiorhynchus.

The brachiopods of the claystoiie facies are significantly less well preserved than those of the limestone 

facies. Most of the difference in preservation is due to 

the effect of compaction in the claystones. This compaction is related to the finer grain size and larger 

amount of iiiterstital water in the claystones. In general, only the specimens from dense limestones within 

this facies are uncompressed. The overall size of brachiopods in terms of bulk or maximum dimension in the 

claystone is less than half the size of those in the limestone facies. All these observations support the general 

conclusion that the bottom on which the claystone fauna 

lived was significantly softer than the bottom which 

supported the brachiopods in the limestone.

Because of its low slightly curved valves, Chonete* 

must have been the closest of all the brachiopods to 

the sediment-water interface. It was then the least able 

of any of the brachiopods in the claystone facies to 

tolerate a muddy bottom or turbid water. Because of 

its large size and its large spines, Cancrinella was possibly able to tolerate a somewhat softer bottom. In a 

few localities these two genera do occur on the same 

bedding plane. Because of their shape, Orurithyris and 

Leiorhynchus theoretically were able to live on a 

slightly muddier bottom than Chonetes, but it is unlikely that either was able to withstand more than the 

slightest sediment load in water. If Leiorhynchus had a 

thinner and longer pedicle than Crurithyris, it may 

have been slightly better adapted to a softer bottom. 

If one were to attempt to list the genera in terms of 

softness of the bottom on which they may have lived, 

Ghonetes, Cancrinella, Crurithyris, and Leiorhynchus 

seem to be a logical sequence from a harder to softer 

bottom. The evidence is somewhat conflicting, however, 

and no positive opinions can be given. It is equally 

possible that all were almost equally well adapted to a 

moderately soft bottom and that other factors influenced their distribution.

The various associations of articulate brachiopods 

within the Meade Peak collections are difficult to explain and may support the idea that the bottom sediment did not influence distribution. While some of the 

admixtures may be the result of mixing of fossils after 

death, it is unlikely that there was much, if any, transportation. The excellent preservation of fossils where 

the matrix is unweathered, the common occurrence of 

articulated valves in Crurithyris, and the small grain 

size of the matrix are all suggestive of a low-energy 

environment. Unfortunately, in many of the collections 

the shells are dissolved, and it is thus impossible to ascertain the amount of abrasion the shells might have 

undergone.

Some of these apparent associations may be the result 

of collecting from more than one bedding plane. It is 

not now possible to investigate how many times this 

association of the several genera actually occurred in 

nature because slabs of matrix were broken in the field. 

The few larger pieces of rock still available suggest 

that dominance of one form is the rule and that admixtures of genera are less common than are now indicated in the collections.

The rare occurrences of Anidanthus and Wellerella in 

the phosphatic shale members are in the dense limestones and thus have no direct bearing on the ecology of 

the faunas in the claystone.

MOLLUSCA

Mollusks are the most abundant group within the 

collections studied. They are perhaps 1^-2 times as 

abundant as the brachiopods; they are perhaps five 

times as abundant as the articulate brachiopods. Pelecypods form the single largest class both in terms of 

numbers and taxonomic abundance. The gastropods, 

cephalopods, and scaphopods combined show slightly 

more taxonomic variety, but their combined numbers 

are probably no more than half of the pelecypods. No 

specimens of Monoplacophora, Polyplacophora or 

Hyolitha have been found. All three of these molluscan 

classes are rare fossils in the late Paleozoic.

PELECYPODA

The pelecypods are only slightly less diverse taxonomically than the brachiopods and would probably be 

more evidently diverse if better preserved specimens 

were available. The pelecypods specimens are almost as 

numerous as the brachiopods, although because of their 

smaller average size, they are slightly less conspicuous 

in the total fauna. The pelecypods have been studied in 

detail by Ciriacks (1963), and results of his study have 

been incorporated into this paper.

The distribution of the pelecypods, like that of the 

brachiopods, allows them to be divided into two facies. 

The claystone facies contains PoUdevcia, and Streblochondria and the limestone facies contains the remaining genera. To a large extent, however, brachiopods
586 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

and pelecypods are mutually exclusive in their occurrences. Because there are living representatives of 

many of the fossil pelecypods, their general habitat 

may be discussed with more confidence than that of the 

brachiopods. The pelecypods are discussed from this 

viewpoint rather than from the consideration of facies. 

The pelecypods may be divided into three groups 

for purposes of this discussion: (1) the protobranchs, 

(2) the pectenoids and mytiloids, and (3) the various, 

other groups combined. The protobranchs, including 

Nucula, Nuculana, Nuculopsis, and Polidevcia, are the 

most abundant of the pelecypods. The second group is 

somewhat less abundant; Streblochondria constitutes 

the bulk of this group. Aviculopecten specimens are 

much less common, and the remainder of the pectenoid 

and mytiloid specimens combined aggregate somewhat less than the Aviculopecten specimens. The third 

group is possibly as abundant as the second, but specimens are scattered through many collections and it is 

difficult to make an accurate estimate. Schizodus and 

Permophorus are the two most abundant genera.

PKOTOBRANCHS

In an important work, Yonge (1939) has presented 

a functional interpretation of the morphology of Recent protobranch pelecypods. Yonge indicates that the 

protobranchs are the most primitive living pelecypods. 

The primitive features include, among others, more 

than two adductor muscles to close the shell, relatively 

small and simple gills limited to the posterior mantle 

cavity, and large palp lamellae beside the mouth. There 

is so little difference in the shell features of living and 

fossil forms that essential identity of soft parts and 

living habit is implied.

Although most other pelecypods feed by filtering 

water through their gills, thereby collecting small organisms and possibly organic detritus in the nuculoids, 

the protobranchs collect food from the sediment by 

proboscislike extensions of the labial palps. The larger 

sedimentary particles are sorted out on the labial palps, 

and the smaller are passed through the alimentary 

tract.

As a consequence of this mode of feeding, protobranch pelecypods are members of the infauna and 

spend most of their life at or slightly below the sediment-water interface. The living Nucula moves horizontally through the sediment. Its mode of life and 

dietary habits are thus 'similar to those of earthworms. 

The living Nuculana is apparently less active. It lives 

almost completely buried, and just the posterior of the 

shell extends up into the water.

In the three living species of Nucula studied by 

Yonge, there is a direct correlation between increasing

size of the animal and increasing particle size of the 

sediment. Although little information exists on this 

particular point, it seems logical that smaller animals 

would be restricted or at least inhibited in extensive 

burrowing by the presence of coarse sedimentary 

particles; larger animals probably would be able to 

deal with both fine and coarse particles. Particle size is 

relative and must be considered in terms of the burrowing ability of the pelecypod foot, not in purely objective 

terms of sedimentary size classes.

No detailed studies seem to have been made on relationship of population density to amount of organic 

matter in the sediment. Nevertheless, sediments containing numerous protobranchs probably would have 

a higher proportion of organic matter than those containing few specimens, provided other factors such as 

grain size and interstitial water are the same. Protobranchs have been found at all depths, but they are 

most abundant in extremely shallow water, possibly 

because of the more abundant organic debris generally 

available.

Within the Phosphoria rock complex, protobranchs 

are common in two different geologic settings. In one 

of these settings, Nuculopsis is extremely abundant in 

the Franson of the Uinta Mountains and locally in the 

Ervay on the east slope of the Wind River Mountains. 

In both areas all physical evidence points to extremely 

shallow water. The sediments are fine grained and more 

deserving of the term "claystone" than shale. The light 

color of the sediments suggests that they are now low 

in organic matter. Though many of the Nuculopsis are 

steinkerns and conceivably might have accumulated as 

a lag gravel over many thousand years, they are scattered through the rocks and do not appear to be a sedimentological accumulation. Accordingly, it is suggested 

that the abundance of Nuculopsis might indicate a 

somewhat higher initial organic content in the sediment 

before diagenesis. There seem to be some differences 

between these specimens and those from the thin beds 

of the Retort Member in the Wind River Mountain 

area of Wyoming, which is about the same general 

facies, but the differences are probably only of a specific 

level, if that significant. Steinkerns are characteristically preserved in both members, but detailed comparisons are not possible.

In the other setting, Polidevcia is abundant locally 

in the Meade Peak Member. Like Nuculopsis, where 

Polidevcia occurs, it is abundant; because of its larger 

size, however, there are fewer specimens per volume of 

rock. Specimens in the collections appear to be confined 

to bedding planes. The fact that most retain both valves 

is suggestive of little or no transportation after death. 

At a few localities in southwestern Montana where the
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 587

Retort member is thickest, Polidevcia is abundant. It 

has not been collected from the thinner sections.

PECTENOIDS AND MYTILOIDS

In the second group of pelecypods, there are no 

closely related living representatives of the Permian 

genera. Living representatives of the superfamilies are 

common, however, and provide some ecological information. The two superfamilies in question are distinguished from the protobranchs and most other pelecypods by being members of the epifauna throughout 

their life and by being attached during at least part 

of their phylogeny or ontogeny. This attachment results 

in the loss of one adductor muscle and various modifications of shell shape (Yonge, 1953).

The living mytiloids or mussels, attached by a 

byssus throughout their life, are frequently gregarious 

and can live under conditions of reduced salinity. In 

the Permian collections, Myalina has a shell form that 

suggests an attached mode of life. It is rare, though it 

is most common in association with abundant ramose 

bryozoans and some Derbyia or Spiriferina. Other 

myalinids also are found rarely in this association. 

Mytiloids also occur rarely in collections with 

Plagioglypta or Aviculopecten as a predominate form. 

All occurrences are in fine-grained limestone, but the 

sediment may have been silty in texture rather than 

muddy.

The pectenoids differ from the mytiloids in living 

unattached on the sea bottom; only a few secondarily 

fix their shell in place. They are active forms, and the 

swimming habit of some of the Recent pectenoids is 

well known; however, not all of the Recent forms are 

capable of such prodigious activity. The swimming 

movement is interpreted as a byproduct of the formation within the mantle cavity of strong currents that 

allow the animal to cleanse sediment from its gills 

(Yonge, 1936). The pectenoids are thus adapted to live 

in environments where there is some sediment in the 

water. The maximum rate of sedimentation with which 

these forms can deal apparently has not been studied. 

According to Yonge, pectenoids are characteristic 

fauna of sandy bottoms in shoal waters, areas that 

might have an intermittent heavy load of sediment.

The commercial scallop in Maine (Smith, 1891) commonly occurs in marine waters 24 240 feet deep, but 

there seems to be no relation between the type of bottom 

and the occurrence of this scallop. Another species, the 

bay scallop of North Carolina (Outsell, 1931) is most 

abundant in water less than 6 feet deep, although it has 

been taken in water as much as 60 feet deep. It occurs 

on bottoms that support a growth of eelgrass and may 

occur in water having salinity as low as 20 parts per 

thousand.

There is always some question as to whether information about Recent species is directly applicable to 

distantly related fossil forms. However, there appears 

to be an excellent correlation between the occurrences 

of Aviculopecten and its close allies and the information on Recent scallops noted in the preceding paragraph. At a few localities, Aviculopecten is abundant. 

Most of these localities are in areas which on paleogeographic grounds appear to be of near-shore facies. 

These occurrences are in fine-grained sandstone or 

what may have been a lime sand; none are in rocks 

thought to have had an originally minute grain size. A 

few Aviculopecten occur occasionally with abundant 

Plagioglypta and Schizodus. A few others are found 

occasionally with ramose bryozoans and Derbyia.

Pseudomonotis, a pectenoid which secondarily cements its shell, is also rarely present in this latter assemblage. In a few localities Pseudomon&tis shells form 

beds as much as 1 foot thick.

The life habit of Streblochondria is somewhat difficult to interpret. It is confined to the phosphatic shale 

members, whereas Aviculopecten is limited to the limestones and sandstones. Within the phosphatic shale 

members Streblochondria occurs both in shales and in 

extremely fine-grained limestones or calcareous claystone, although it is more common in shales. Where the 

genus occurs, it is usually abundant.

Some occurrences of Streblochondria could be death 

assemblages. None of the collections give any evidence 

of current orientation of the shells. Some slabs show 

that fossils extend through at least 2 inches of shale. 

In the absence of conclusive evidence of sorting, it seems 

better to consider Streblochondria as gregarious in life.

Unlike Aviculopecten and many of the other pectenoids, Stre~bloclwndria does not have a ribbed shell. In 

addition to being smooth, the shell is thin compared to 

Aviculopecten of the same size. These two features suggest a weak shell that would have been incapable of 

withstanding the extremely rapid and violent contraction of the adductor muscle necessary for swimming; 

there are reports of Recent scallops breaking their 

shells during an abrupt muscle contraction. This surmise might be checked by examining' the depth of the 

muscle scar, but no specimens showing the interior are 

available.

If Streblochondria was exclusively a bottom-dwell' 

ing form, several inferences regarding the sedimentation of the Meade Peak and Retort Members can be 

drawn. The bottom must have been firm enough to support the animal. Because of the small size of the shell 

and the proximity of the soft parts to the sedimentwater interface, the water must have been clear for 

long periods, and thus sedimentation was probably
588 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

slow. Finally, the abundance of specimens implies an 

abundant food supply. The environment of this genus 

might be interpreted as a shallow-water mud area.

OTHEK PELECYPODS

The pelecypods comprising the third group are 

thought to have been filter feeders, those which burrow 

into the sediment and draw water into their bodies by 

means of siphons. Recent pelecypods composing the 

infauna are so diverse and the phylogenetic relations 

are so obscure that it is not possible to draw any firm 

homologies to the Permian.

Analogy with living genera of the same general shell 

form suggests that Wilkingia may have been a fairly 

deep burrower (Elias, 1937, p. 409). Some shells show a 

posterior gape suggestive of long nonretractible siphons. This genus characteristically occurs with brachiopods which seem to have lived on a firm to moderately 

soft bottom.

Pertnoplioms has a shell shape similar to that of 

Wilkingia but is much smaller and occurs in other 

associations. Characteristically this genus occurs with 

ScMzodm, Plagioglypta, and bellerophontacean gastropods in fine-grained calcareous sandstones or limestones. 

Both of these other genera are interpreted as shallow 

burrowers. ScJiizodus is more widespread than Pennopho,ms and occurs rarely with productoid brachiopods, 

particularly in the Ervay Member in the Wind River 

Mountains area.

The few occurrences of Astartella are in sandstones 

suggestive of a near-shore environment. The remaining 

pelecypods are too scattered and too rare for any meaningfully inferences to be drawn.

SCAPHOPODA

The scaphopods form a negligible part of the mollusk 

fauna. Almost all specimens are either Plagiogly pta or 

are generically indeterminate. Although locally common, the scaphopods are the least abundant of the mollusk groups. With the exception of several rare occurrences in the Grandeur Member, the scaphopods are 

limited to localities in the Franson Member and Shedborn Sandstone, both peripheral to the central area of 

phosphate deposition.

Living scaphopods occur through a wide depth range. 

The foot is modified for digging and resembles the 

pelecypod foot in that respect. Most are thought to be 

microcarnivores and detritus feeders and are considered 

to be part of the infauna. Because the scaphopod shell 

is open at both ends, the animal does not burrow completely into sediment but keeps the posterior above the 

sediment-water interface. Commonly within the Phosphoria rock complex, scaphopods are limited to finegrained sandstone or limestone, both of which were

thought to have been sediments through which the animal could have moved.

All the occurrences of scaphopods in the Phosphoria 

rock complex are in areas which on paleogeographic 

grounds are thought to be shallow water and near-shore. 

They are characteristic of south-central Montana and 

the Uinta Mountains area in Utah. Scattered occurrences in the eastern outcrops of the Ervay Member 

along the east flank of the Wind River Mountains, Wyo. 

strengthen the inference of a shallow-water habitat. 

Nicol (1944, p. 556) has suggested that occurrences of 

abundant Plagioglyptn in the Kaibab Limestone 

might be suggestive of hypersaline water.

GASTROPODA

Although the gastropods taxonomically are almost 

as diversified as the pelecypods, they are represented by 

far fewer specimens. If the unusual locality for silicifled 

fossils in the Grandeur Member at Cephalopod Gulch, 

Utah (18890) were disregarded, the abundance of specimens and the taxonomic diversity would drop sharply, 

and the gastropods would then be about as abundant as 

the cephalopods, both in numbers and in diversity. At 

this atypical locality, the tremendous number of 

Orthonema packed into the rock indicates some kind 

of physical sedimentary accumulation. Other genera are 

present in negligible numbers.

If, in addition, one ignores exceedingly rare occurrences of other genera, totaling about two dozen specimens, all gastropods in the Phosphoria rock complex 

are identified as either bellerophontaceans, Babylonites, 

or pleurotomariaceans. Bellerophontaceans and Babylonites are present in about equal numbers; pleurotomariaceans are about half as abundant as either group.

It is possible to divide the gastropods into a limestone facies, containing the bellerophontaceans and 

some of the pleurotomariaceans, and a claystone facies, 

containing Babylonltes and the remainder of the pleurotomariaceans. It may be more meaningfull, however, 

to discuss the inferred physiology of the fossil gastropods. Although there has been some question in the past 

regarding the systematic position of the bellerophontaceans, they are currently regarded as relatively primitive gastropods characterized by aspidobranch gills 

(Knight, Batten, and Yochelson, 1960).

Yonge (1947) has directed attention to the relatively 

delicate nature of the aspidobranch type of gill and its 

susceptibility to fouling by sedimentary particles. 

Yonge (in Yochelson, 1960, p. 215) not only indicates 

that the living aspidobranch-gilled gastropods are restricted to firm bottoms and clear water but also supports the suggestion that the fossil forms believed to 

have this type of gill were equally restricted in their 

habitat.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 589

The bellerophontaceans are the most abundant of the 

three groups of gastropods. Almost all of them occur 

in association with ScMzodus and (or) Plagioglypta. 

Most are found in Shedhorn Sandstone or in limestones 

of the Franson Member, particularly along the Uinta 

Mountains of Utah.

The bellerophontaceans are considered to be members of the epifauna, and their presence implies a firm 

bottom. A few of the specimens are Belleroplwn, but at 

most localities Euphenutes or Euphemitopsis is the only 

bellerophontacean present. These two genera differ 

from Bellerophon in having a large elaborate mantle 

that secreted secondary calcium carbonate on the exterior of the shell (Yochelson, 1960, p. 232-233). 

Whether this is an adaption to allow these genera to 

enlarge the mantle cavity and capacity of the gills, 

and thereby to allow them to live on softer bottoms, 

cannot now be determined. It has been observed that in 

the Pennsylvania!!, Euphemites seems to occur in more 

different rock types than does Bellerophon.

Even though the pleurotomariacean gastropods are 

less abundant than Bdbylonites, they are considered 

next because they have shell features which, like the 

bellerophontaceans, suggest the presence of a pair of 

gills. Two general types of pleurotomariaceans are 

found in the fauna. Glabrocingulum, a relatively small 

gastropod, occurs in the shaly limestones of the Franson Member in the Uinta Mountains where it is associated with abundant small Nucida. Worthenia, a relatively large gastropod, occurs locally in shales of the 

Meade Peak and Retort Members. Although specimens 

are poorly preserved, most of the specimens identified as 

"low-spired gastropods indeterminate" in the Franson, 

Meade Peak, and Retort Members probably are pleurotomariaceans. Almost all of the specimens show features which suggest that they are representatives of 

one or the other of these genera. It is likely that each 

genus is more widespread within its particular facies 

than would be surmised from the identified material.

The presence of G7abrocingulum allows for some interesting speculation. Almost all of the living aspidobranch gastropods are herbivores. Some of the smaller 

ones not only browse algal fronds but spend their life 

on these fronds rather than on the bottom itself. There 

is little direct evidence of gastropods and associated 

algae in the fossil record as yet, but several examples 

have been reported (Yochelson, 1956, p. 191). As was 

suggested in the discussion of OrbwuJoidea from this 

area (p. 583), the Franson sea in the Uinta Mountains 

area may have supported algal growth on which these 

locally abundant small Glcibrocingulum could have 

lived. Alternately, the bottom may have been firm 

enough to allow the small gastropods to crawl about

without being smothered by turbid water. Whatever 

the habitat, the presence of the aspidobranchs suggests 

the need for some vegetation as food supply.

Even if an algal substrate existed for GldbrotinguIwin, this is not postulated for Worthenia because of the 

larger size of that shell. The possible presence of this 

large delicate-gilled gastropod in the epifauna suggests 

that the shales could support the weight of the animal 

as it moved about and that the sediment was not stirred 

up appreciably during this movement.

Bdbylonites differs from the bellerophontaceans and 

the pleurotomariaceans in being exclusively confined 

to the phosphatic shale members where it occurs in 

both shales and dark dense limestones. It further differs 

in having conchological features suggesting a single 

gill, like the Recent Trochus, rather than a pair of gills. 

There is no reason however, to believe that this gill allowed it to adapt to life on a soft muddy bottom as a 

member of the infauna. Many B'abylonites in the Permian of western Texas are from small reefs (Yochelson, 1956, p. 189-190). Others are from thin-bedded 

black limestone of the Bone Spring Limestome, lithologically similar to the "cap lime" of the Meade Peak 

Member. Nowhere in the western Texas occurrences of 

this genus is there conclusive evidence of an infaimal 

habitat for this genus, nor are these occurrences in 

areas suggestive of deep water.

At several localities in southeastern Idaho the "cap 

lime" is crowded with Bdbylonites. This may have been 

the result of transportation by currents. None of the 

specimens seem worn, and it is more likely that these 

occurrences are the result of a lag accumulation, the 

smaller fossils being removed by relatively gentle 

currents.

CEPHALOPODA

The cephalopods are intermediate in abundance between the gastropods and the scaphopods. They are 

little varied taxonomically; all but about 25 specimens 

have been referred to Pseudogastrioceras. These few 

varied genera include both coiled and straight phragmocones. Most of them are from limestones which on 

paleogeographic considerations are thought to have 

been deposited in near-shore shallow water.

In contrast, Pseudogaxtrioceras is characteristic of 

the phosphatic shales. Some specimens have also been 

obtained from the dark fine-grained limestones associated with the phosphatic shales; these limestones are 

uncommon, however except at Wanrhodes Canyon and 

the Right Fork of Hobble Creek in Utah. Characteristically several Pseudogastrioceras specimens occur in 

the same collection, though specimens are significantly 

less common than any of the other fossils common in 

the phosphatic shales. Many specimens, like other fos-
590 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

sils in the shales, are flattened by diagenetic compaction. 

Both shells and aptychi (apertnral covers) have been 

found.

Most ammonoids are thought to have been efficient 

swimmers, possibly carnivorous in habit. The small 

number of specimens of Pseudogastrioceras, compared 

to other genera, fits well with its theoretical position in 

the food chain. Although several genera of the Meade 

Peak and Retort epif auna were within the size which 

would have been prey to a moderate- to large-size 

predator, there is no direct evidence as to what particular animal group or groups served as a source of food. 

Pseudogastrioceras is almost never found in association 

with other invertebrates; the rare occurrences with 

other invertebrates are with a variety of organisms. 

Specimens occasionally are associated with fish scales. 

The virtual lack of associates, except for these fish remains, leads to the speculation that the shells may not 

now be where they lived but may have drifted to 

slightly deeper water before being incorporated into the 

sediment.

Speculations about the life habits of the nautiloids 

(Flower, 1957, p. 831-834), which might also apply to 

the ammonoids, seem to indicate that the animal in life 

had control over its buoyancy by regulating the amount 

of gas within the camera. Soon after death, the aptychus, if one were present, would rot free from the soft 

parts, and its loss would destroy the hydrostatic balance. This would then allow the shell to drift until the 

gas within the shell was dissipated. Drifting of shells 

after death has been demonstrated in the Recent 

Nautilus.

It is not certain how much this possible drifting after 

death might have influenced the present distribution of 

the fossils. Two lines of evidence suggest that Pseudogastrioceras during life may have been poorly adapted 

to swimming and may have spent much of its life at or 

near the site of epif aunal concentrations. First, the shell 

is relatively wide and has a rounded venter. The most 

efficient swimmers among the cephalopods are thought 

to have been narrow with a sharp venter, a streamlined 

shell form that developed little water resistance. Second, Pseudogastrioceras has a calcified aptychus. This 

extra weight must certainly have limited its ability to 

swim.

The finding of aptychi in the Phosphoria Formation 

is most unexpected, as Paleozoic aptychi are exceedingly rare fossils (Gloss, Gordon, and Yochelson, 1964). 

Mesozoic aptychi are uncommon, although locally there 

are extensive beds containing virtually no fossils other 

than aptychi, which generally have been interpreted as 

sedimentary lag deposits. Most of the Phosphoria 

aptychi have been found in dense dark limestones within

the Meade Peak Member at the Right Fork of Hobble 

Creek, Utah; the majority of the remaining occurrences 

are in the nearby Wanrhodes Canyon section in rocks of 

the same lithology. The relatively large amount of finegrained limestone, the abundance of aptychi, and the 

relatively great thickness of the Meade Peak strata in 

both of these Utah sections are atypical of the Meade 

Peak Member in southeastern Idaho. Perhaps, these 

atypical features may 'be correlated. Possibly the central Utah area was further from the shoreline.

The occurrences of aptychi differ from those in the 

Mesozoic in that many Pseudogastrioceras shells occur 

with the aptychi. In most Mesozoic limestones containing abundant aptychi, shells are absent and the relating 

of the proper aptychus to its shell becomes a complex 

problem. The proximity of aptychi and shells suggests 

that little drifting of the animal took place after death.

In addition to Pseudogastrioceras shells and aptychi, 

one other unusual indication of cephalopods has been 

found in the phosphatic shales. These are onychites 

(small chitinous hooks) thought to be modifications of 

the suckers found on the tentacles of squids. Similar 

structures have been described from the Permian of 

Greenland (Fischer, 1947"). Little is known about the 

animal, but it is believed to have been a nectonic form.

ARTHROPODA

Arthropods are poorly represented in the collections. 

Both of the trilobite pygidia reported occur in rocks 

that may be older than the type Grandeur. Because 

trilobites are rare in Permian rocks elsewhere in the 

United States, little significance is attached to their 

absence from the Phosphoria rock complex.

No attempt was made to search the collections carefully for ostracodes by any means other than a hand 

lens. Although it is possible that scattered specimens 

have been overlooked, it is certain that no large concentrations of ostracodes have been ignored. A few occurrences were noted in both fine-grained limestones and 

shales but are more common in the latter. The bulk of 

the ostracodes are from the Meade Peak Member. The 

two ostracode collections from the Franson Member 

contain a few poorly preserved specimens which may 

have been reworked.

A few borings similar to those attributed to parasitic 

barnacles (Saint-Seine, 1954) have been observed in 

some brachiopod shells. Most are found in the localities 

where specimens have been silicified and can be examined readily. Usually, only moderately large to large 

specimens are bored. The borings are distributed without any obvious pattern but are particularly noteworthy 

in the collection from a limestone lens in the Rex Chert 

Member at the South Fork of Sage Creek, Idaho.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 591

FISH

By DIANNE H. VAN SICKLE

Of approximately 1,500 fossil collections, about 400 

collections contain fish remains. About 15 percent of 

the collections are from Montana, 25 percent each from 

Utah and Idaho, and about 35 percent from Wyoming. 

In about 60 percent of the collections fish are found in 

association with invertebrate fossils. Most of the fish 

remains are associated with mollusks, but many are 

associated with orbiculoid brachiopods. In those collections in which fish are the only fossils, most consist 

of scales and small teeth, rather than bone.

With few exceptions, the fish remains are fragmentary and are mostly unarticulated pieces of teeth, scales, 

and bone, of which teeth are predominate. In Idaho most 

of the remains are from the Meade Peak Member, and 

most are scales and small teeth. The distribution of these 

remains and their approximate abundance are shown in 

figure 166. In Wyoming, Utah, and Montana, more are 

found in the Franson Member, Retort Member, and 

Shedhorn Sandstone than in the Meade Peak. These 

collections are commonly teeth and indeterminate bone.

Although fish remains are present in all members of 

the Phosphoria rock complex, different kinds seem to 

be more characteristic of certain members. In the Grandeur Member, particularly in the Utah and Wyoming, 

palaeoniscoid teeth or "fairy collar buttons" (Yochelson 

and others, 1961) and indeterminate bone seem to be the 

predominate material.

The Meade Peak Member is characterized by an 

abundance of scales in Idaho, to a lesser degree in 

Wyoming and Utah, and to an even lesser degree in 

Montana. The scales are predominately those of indeterminate palaeoniscoid and acrolepid fish. The most complete specimen found was the flank region of Acrolepis 

sp., identified by D. H. Dunkle, from the Meade Peak 

Member at Hot Springs, Idaho. In the Retort Member, 

scales, tcieth, and "fairy collar buttons" are about equally 

abundant.

In the Franson Member, Shedhorn Sandstone, and 

Ervay Member, teeth and "fairy collar buttons" are 

most abundant. Most of these are from sandy limestones. 

The teeth are palaeoniscoid in nature. Collections near 

presumed former shorelines usually contain only the 

more resistant kinds of remains.

Preliminary identification of the fish remains in Wyoming was done by D. H. Dunkle, U.S. National Museum, and the writer, but material from the other States 

was not examined in detail. These identifications are 

given in table 5. It is not possible to comment on the 

stratigraphic distribution of fish remains reported by 

E. B. Branson (1916) and C. C. Branson (1933).

ASSOCIATIONS OF THE FAUNA

Although life habits and relative abundance of animal species in the total fauna may provide data applicable to ecologic interpretation, the association of 

various fossils may likewise yield valuable information. 

The data on life habits and abundance are slanted more 

toward biology, and the data on associations apply more 

to sedimentation; each contributes to reconstruction of 

former environments.

Ideally, each collection should be considered simultaneously from the standpoint of fossils and matrix. In 

this work, first consideration was given to the fossils exclusively. In part, this approach was chosen because 

general reconstruction of the former environment based 

entirely on physical features was already available 

(Sheldon, 1963; Cressman and Swanson, 1964). It is desirable to test these conclusions by independent consideration of the fossils. The evidence presented seems 

to support earlier interpretation of the environment.

FOSSIL CATEGORIES

Several characteristic associations of fossils were 

noted in the early part of this study of the fauna, and 

a system was devised to help clarify interpretation, especially of the possible ecological interrelations of 

various kinds of organisms. To avoid misinterpretation, the term "category" was used in place of "association," which may carry a biologic connotation. For 

convenience these categories are indicated by number; 

for example, collections containing only orbiculoid 

brachiopods are always designated by "23" irrespective of their geologic distribution. The category number is given on the charts of faunal distribution just 

above the symbol indicating the stratigraphic position 

of that individual collection.

These categories have certain inherent weaknesses 

which should be discussed before their advantages can 

be mentioned. The groupings are synthetic rather than 

analytic. Because of the large number of theoretically 

possible combinations of fossils which could be devised, 

it was impossible to begin with a rigid framework 

into which the individual collections would then be 

assigned. Rather, the process was to group all collections that contained one particular form and subsequently, by considering one or more of the associated 

fossils in the collection, to separate atypical collections 

from this main group. In effect, this trial and error 

method was an informal chi-square test, but all reference as to whether a collection "fit" or not was based 

on so many variables that no formal mathematical expression of similarity among collections was possible. 

The dividing of groups into subgroups naturally could 

not be continued indefinitely to take into account all
592 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

the many variables in kind and number of associated 

fossils. Eventually a point would be reached where 

there would be so many different categories that, in 

effect, there would be no grouping of the collections.

Most of the categories defined as containing one, two, 

or three faunal elements are distinct. Those that include more than this number are less obvious. A certain 

amount of judgment was obviously used to determine 

the limits of the various groups employed. This, in 

turn, raised the problem of the importance to be assigned to the number of specimens present in individual collections. For most categories the larger number 

of individuals has been the deciding factor, but in a 

few small collections where only one or two of each 

kind are present, emphasis had to be given to one form. 

Thus, a collection with one Bathymyonia, and one 

Derbyia may have been assigned to the category defined by the former rather than the latter. For example, 

the grouping for tentacle hooks of squids or Lingula 

has been designed to call attention to distinctive forms 

even though they may be in the minority.

The quality of preservation has been given little consideration. Thus, indeterminate linoproductoid, CancrmeUal Cancrinetta, Cancrinetfa cf. C. phosphatica, 

and C. phosphatica have all been taken to mean the 

same. While the probability is high that they are all 

the same, in view of the limited nature of the fauna 

found in the better preserved material, there is no assurance that this is necessarily so. One or two wholly 

artificial categories have been designed for indeterminate forms that could not be readily accommodated in 

other groupings.

It is also recognized that in dealing with the preserved 

hard parts of fossils one is dealing with a biased sample. As the remains of soft bodies or even traces of their 

activities are not preserved, one can do not more than 

note that such bias exists.

These categorizations, however, have distinct advantages. It has long been known that there are fundamental differences in sites where animals live. These differences are so obvious that occasionally they tend to be 

overlooked. The very fact that there are only a few 

categories out of many theoretical groupings reinforces 

this obvious difference.

ISTot only does the presence or absence of certain category numbers in various stratigraphic units indicate 

the presence or absence of some fossils, but the number 

of each of these categories gives at least a semiquantitative expression of the relative abundance of the kinds 

of animals in each unit. The number of collections 

within each category clearly expresses the differences 

among the various units.

It is recognized that available computor techniques 

could be used to determine the various combinations 

into which the fossils may be grouped. Use of these machines was rejected, however, because of the large 

amount of work required to program and prepare raw 

data for such an operation. Furthermore, a purely mechanical approach does not allow one to evaluate variation due to collecting and preservation; doubtlessly such 

an approach would have resulted in more groupings 

than are employed here. After this work had been completed a sample of the localities were analyzed by computor methods to test for associations. This test was 

not satisfactory.

The fossil categories used are as follows: 1

2. Assemblages of gastropods and (or) pelecypods, 

frequently pleurotomariacean gastropods, Naticopsis, Cyclites, and (or) OrtJwnema, Astartetta, 

and (or) Wilkingia, rarely with a few associated 

nuculoid pelecypods and (or) fish fragments.

3. Pleurophorid and (or) parallelodontid pelecypods, 

including generically indeterminate specimens, 

associated with a few pectenoids or other mollusks, commonly other pelecypods.

4. Predominantly ScMzodus occasionally associated 

with a few other mollusks, usually pelecypods.

5. Predominantly Avwulopecten, commonly associated 

with smaller numbers of Scltizodus, rarely associated with parallelodontid pelecypods, myalinid 

pelecypods, Streblochondria, and (or) Naticopsis, 

in that order, or rarely predominately Pseudomonotis.

6. Plagioglypta, bellerophontacean gastropods, and 

Scliizodu-s, or rarely Plagioglypta and (or) bellerophontaceans alone, commonly associated with 

pectenoid pelecypods and pleurophorid pelecypods, and rarely associated with orbiculoid 

brachiopods, Composita, nuculoid pelecypods, 

and (or) myalinid pelecypods.

7. Predominantly fenestrate bryozoans, occasionally 

associated with fish remains, mostly bones and 

teeth, and (or) rare diversified mollusks, commonly pelecypods.

8. Sponge spicules exclusively or predominantly, rarely with a few Lingula, orbiculoid brachipods, and 

(or) articulate brachiopods.

9. Abundant crinoid stems commonly associated with 

bryozoans.

10. Predominantly Hystricula or indeterminate small 

productoid brachiopods occasionally associated 

with Composita and (or) Ch-onetes, rarely assoi Category 1 was discarded at a late stage of the study. To avoid 

error the other numbers were not changed.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 593

ciated with a few fish remains, usually bones or 

teeth.

11. Predominantly ramose bryozoans, occasionally associated with a few articulate brachiopods.

12. Predominantly ramose bryozoans, occasionally associated with Amculopecten and bellerophontacean gastropods, rarely with fish remains, Pseudomonotis, WilMngia, and (or) nuculoid pelecypods, in that order.

13. Abundant ramose bryozoans and some brachiopods, 

chiefly Derbyia and Spiriferina, less commonly 

associated with Hitstedia, and occasionally associated with 0 rbiculoidea, rarely associated with 

a few crinoid stems, Amculopecten, Myalina, 

Compvsita, bellerophonacean gastropods, and 

(or) fish remains, in that order.

14. Predominantly Derbyia and (or) Spiriferina, commonly associated with ramose bryozoans, occasionally associated with Sphenosteges or 

Bathymyonia, rarely associated with a few crinoid stems, Schizodus, Amculopecten, WilMngia, 

Myalinella, nautiloid cephalopods, and (or) fish 

remains, in that order.

15. Predominantly Neospirifer and (or) Sphenosteges, 

rarely associated with Horridonia and (or) 

Bathymyonia.

16. Predominantly Echinauris, commonly associated 

with Bathymyonia, Composita, and (or) Spiriferina, occasionally associated with a few ramose 

bryozoans, Wellerella, Chonetes, Phricodothyris, 

Huxtedia, and (or) crinoid stems, in that order.

17. Predominantly Bathymyonia and (or) Muirwoodia, commonly associated with Derbym, 

Spiriferina, Composita, and ramose bryozoans, 

occasionally associated with a few Hustedia, 

Echinauris, Schizodus, Allorisma, and (or) 

Amculopecten, in that order.

18. Squamaria, Rugatta, and (or) Kochiproductus, 

frequently associated with some Anidanthus and 

(or) Linoproductus, and Cornposita, occasionally associated with rare Wellerella, Chonetes, 

Bathymyonia, Amculopecten, Derbyia, and (or) 

Rhynchopora, in that order.

19. Frequently Composita or Wellerella, occasionally 

associated with a few Rhynchopora, rarely associated with a few Streblochondria or indeterminate brachiopods, or bryozoans; rarely indeterminate brachiopods exclusively.

20. Crinoid stems exclusively or predominately.

21. Fish remains exclusively, predominantly bone fragments and (or) small teeth, rarely with associated scales.

22. Fish remains, generally scales and orbiculoid 

brachiopods exclusively.

23. Orbiculoid brachiopods exclusively.

24. Predominantly Orbiculoidea, commonly associated 

with small nuculoid pelecypods, less commonly 

associated with small low-spired gastropods, 

rarely associated with fish remains and (or) 

cephalopods.

25. Lingula exclusively, or Lingula associated with 

Orbiculoidea and (or) fish remains, where it then 

is frequently a minor element of the fauna, occasionally associated with a few small nuculoid 

pelecypods or small gastropods.

26. Abundant nuculoid steinkerns (most are probably 

Nuculopsis], commonly associated with small gastropods and (or) small amounts of fish remains, 

usually scales, and (or) rarely associated with 

orbiculoid brachiopods.

27. Lingula, frequently as a minor element of the collection, associated with Echinauris, Streblochondria, Crurithyris, Babylonites, Gancrinella, Leiorhynchus, Amculopecten and (or) Rhynchopora, in that order.

28. Oancrinetta exclusively.

29. Gancrinella, 8trel)lochondria, and Babylonites, or 

two of these three in about equal numbers, frequently associated with smaller numbers of 

Leiorhynchus and (or) Polidevcia.

30. Predominantly Oancrinetta, associated with fewer 

Leiorhynchus, rarely associated with a few orbiculoid brachiopods, productoid, Babylonites, 

and (or) Streblochondria, in that order.

31. Predominantly Streblochondria associated with 

fewer Polidevcia and rarely, other nuculoid 

pelecypods.

32. Predominantly Streblochondria associated with 

fewer orbiculoid brachiopods.

33. Streblochondria exclusively.

34. Abundant Streblochondria associated with fewer 

Cancrinella, Leiorhynchus, and (or) Babylonites, 

in that order.

35. Abundant Streblochondria, usually with fewer 

Ohonetes, frequently with a few Crurithyris and 

(or) Leiorhynchus, rarely with orbiculoid brachiopods, Babylonites, indeterminate gastropods, 

indeterminate pelecypods, and (or) Rhynchopora, in that order.

36. Babylonites exclusively.

37. Predominantly Babylonites associated with fewer 

Streblochondria, Cancrinella, orbiculoid brachiopods, indeterminate brachiopods, and (or) indeterminate pelecypods, in that order.

38. Worthenia exclusively.
594 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

39. Predominantly Worthenia or Worthenia-like steinkeriis frequently associated with fewer Bdbylonites and (or) indeterminate pleurotomariacean 

gastropods, rarely associated with a few Leiorhynchus, indeterminate brachiopods, indeterminate pelecypods, and (or) cephalopods, in that 

order.

40. Predominantly CruritJiyris associated with fewer 

indeterminate gastropods and (or) pelecypods, 

frequently associated with a few orbiculoid 

brachiopods, less frequently associated with 

Leiorhynchus, Chonetes, Babylonites, fish remains, and (or) Streblochondria, in that order.

41. Chonetes exclusively.

42. Predominantly Chonetes frequently associated with 

fewer Streblochondria, occasionally associated 

with fewer CruritJiyris and (or) Leiorhynchus, 

rarely associated with a few Glabrocingulum, 

Composita, and (or) conularids, in that order.

43. Chonetes, Cancrinella, and Babylonites approximately equally abundant, or rarely, two of these 

three genera approximately equally abundant.

44. Chonetes, Leiorhynchus, and (or) Crurithyris 

nearly in equal abundance, frequently associated 

with a few Streblochondria, indeterminate pleurotomariacean gastropods, pectenoid pelecypods, 

and (or) orbiculoid brachiopods, in that order.

45. Crurithyris and Chonetes approximately equally 

abundant, usually associated with fewer orbiculoid brachiopods, occasionally associated with 

Streblochondria and (or) indeterminate gastropods.

46. Crurithyris exclusively.

47. Predominantly Lei&rhynchus associated with fewer 

orbiculoid brachiopods and (or) nuculoid pelecypods, rarely associated with a few Stre~blochondria or fish remains, usually scales.

48. Predominantly Leiorhynchus associated with fewer 

Chonetes, frequently associated with a few Stre~blochondria and (or) Babylonites, less frequently 

associated with a few orbiculoid brachiopods, 

cephalopods and (or) fish remains, usually scales, 

in that order.

49. Predominantly Leiorhynchus associated with fewer 

Babylonites, frequently associated with a few fish 

remains, less frequently associated with a few 

Streb lochondria.

50. Predominantly Leiorhynchus associated with fewer 

Crurithyris, rarely associated with Streblochondria and (or) Babylonites.

51. Leiorhynchus exclusively.

52. Foraminifers or ostracodes exclusively.

53. Predominantly Polidevcia associated with Streblochondria and (or) Aviculopecten, occasionally 

associated with indeterminate pelecypods, indeterminate gastropods, and (or) fish remains, in 

that order.

54. Polidevcia exclusively.

55. Indeterminate pelecypods exclusively (most are 

possibly Polidevcia}.

56. Predominantly indeterminate pelecypods (most are 

possibly nuculoids), occasionally a few indeterminate gastropods, rarely associated with one or 

two generically identifiable mollusks.

57. Fish scales exclusively.

58. Predominantly cephalopods, frequently associated 

with a few Streblochondria and (or) Polidevcia 

and fish remains, rarely associated with a few 

Crurithyris and (or) Rhynchopora.

59. Cephalopods and fish remains, usually scales 

exclusively.

60. Cephalopods exclusively.

61. Squid tentacle hooks exclusively or predominately, 

occasionally associated with fish remains, usually 

scales, rarely with orbiculoid brachiopods or 

cephalopods.

INTERPRETATION OF CATEGORIES

One of the first questions posed in any examination 

of a collection of fossils is whether it is simply an aggregation of sedimentary particles or whether it is a representative sample of the animals living on a former 

sea bottom. There is, however, a continuous spectrum 

running from the sedimentary aggregation to the life 

association, and no collection is entirely one or the 

other. Johnson (1960) has considered the various 

admixtures of fossils which may occur.

Currently, criteria which may be used to distinguish 

life associations from death assemblages are few. The 

writer considers that the characteristic occurrences of 

fossils of diverse size and shape over a geographically 

widespread area allows one to infer that sorting has 

been a minor feature (Mudge and Yochelson, 1962). 

Conversely, the disarticulation of pelecypod valves and 

the abundance and arrangement of shells in a matrix 

allow one to imply strong sorting. Between these two 

limits there is little but personal opinion to determine 

the nature of the grouping.

The examples of extreme sorting are easiest to deal 

with because they are the most clear cut. These include 

collections in the following categories: 2, 3, 9, 20, 21. 

Not all collections included under each category are 

necessarily sedimentary aggregations, but this explanation probably applies to the majority of them. Some of 

the collections in category 23 are from the "fish-scale
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 595

marker bed" in the Meade Peak Member and are aggregations. Disarticulated sponge spicules, category 8, and 

fragmentary bryozoans associated with fragments of 

fish, category 7, are also indicative to some degree of 

sorting.

The remaining categories are all thought to approximate the natural associations of the animals that developed hard parts. Several categories include a few 

collections which suggest some sorting, but the sorting is 

not pronounced compared to the others noted in the 

preceding paragraph.

One approach which may be taken to the question of 

sorting in the bulk of the collections is through size distribution of fossils. All information on size distribution 

is based solely on inspection, with no measurements 

within individual populations; full use has not been 

made of this tool. For the brachiopods and pelecypods 

in the "claystone f acies," size distribution is moderately 

good to fairly good, in that small specimens are more 

abundant than larger ones. This distribution applies 

particularly to collections in categories 28-54. In some 

of the "limestone facies," size distribution of the various genera is not so pronounced; more specimens are 

closer to adult size, as judged by comparison with fossils from other areas, than in the "claystone facies." 

This distribution applies particularly to collections in 

categories 10 and 14-19. The fact that almost all collections lack fossils under 0.5 millimeters in maximum 

width indicates that some sorting from the early 

growth stages has taken place. There is no evidence that 

the smaller fossils were destroyed by solution.

Another approach to the question of sorting is 

through preservation. The best preserved fossils are 

those in the "claystone facies." Even though more of the 

individual shells have suffered from the effects of compaction and solution than fossils in other facies where 

fresh rock has been sampled, fine morphological details 

still have been preserved. In the "limestone facies" 

brachiopods that bear spines commonly have them 

broken off at the base. The bryozoans associated with 

these brachiopods are commonly in small pieces. This is 

particularly noticeable among collections in categories 

16-18.

Only a few other categories suggest some current or 

wave activity. Neospirifer, category 15, commonly is 

worn. On the other hand, the usually large bryozoan 

colonies in categories 11-14, particularly in 11 and 12, 

suggest little or no breakage. Steinkerns of Nuculopsis, 

category 26, commonly show little variation in size, but 

it cannot be determined if this is because the species involved are inherently of small size.

There is little evidence regarding salinity. Some of 

the mollusk assemblages, categories 4 and 6, and possibly 26, may have been able to live under slightly 

hypersaline conditions. Crinoids and bryozoans, categories 7, 9,11,12,13, and 20, almost certainly lived under conditions of normal salinity, but not all these categories are considered to be life associations. Most of the 

categories containing brachiopods probably indicate 

normal to near-normal salinity.

Direct information as to depth ranges of fossils is 

virtually nonexistent. The only fossil to which much 

significance can be attached is Lingula, characteristic of 

categories 25 and 27. Its occurrence probably indicates 

water much less than 50 fathoms deep and possibly less 

than 10 fathoms deep. By inference from paleogeographic reconstructions for this and other areas, some 

of the mollusks, particularly in categories 2-6, are 

thought to have lived in quite shallow water. The 

amount of wear 011 some of fossils in categories 15 and 

18 is indicative of shallow water.

The categories are numbered in a sequence that appears to be from near shore to offshore, with a few exceptions included arbitrarily for convenience in compiling. Some deviation from an ideal scheme is necessary 

because there probably were several different kinds of 

shore zones; some workers might question the precise 

placement of several of the categories. In the main, 

however, this sequence reflects what is thought to be 

the most logical interpretation.

Categories 2, 7, and 21 seem to be characteristic of 

beach or near-beach environments. They are found commonly in the Shedhom Sandstone and shoreward sandstone facies of the Franson Member. Categories 4-6 are 

most characteristic of argillaceous limestones in shallow-water areas of the Franson Member. It is possible 

that categories 4 and 6 are based only on slight collecting differences. Category 3 is more of a catchall but approaches a beach coquina and is not common in the 

Grandeur Member.

The relative depth of sponge spicules, category 8, is a 

problem. Partly because some cherts grade into the 

Shedhorn Sandstone and partly because a few orbiculoid brachiopods also occur with the spicules, they have 

been placed as remains from an extremely shallowwater fauna. It is recognized, however, that this assemblage could occur in deeper water.

Categories 9 and 10 probably are a little out of sequence and might be better moved in the sequence to 

indicate slightly deeper water. Conversely they, with 

some of the collections in category 18, seem to form a 

bioclastic "limestone facies" sequence in the Grandeur 

Member which, in part, is comparable to the sequence 

in the two younger limestone members. These collections might be taken as approximately equivalent to 

the bryozoan collections in categories 11 and 12. Gate-
596 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

gories 11-17 are the "limestone facies" particularly 

characteristic of the Franson and Ervay Members. They 

are arranged in order from firm to slightly softer bottom, from quiet to slightly more turbulent water, and 

presumably, from shallower to slightly deeper water.

The collections in category 18 include both those from 

the Grandeur Member and those from the Rex Chert 

Member. Collections from each unit are a little different, but there are so few of them that it was not worthwhile to divide the group. Crinoid stems, category 20, 

are partly from limestone lenses in the Rex Chert Member and are partly from collections in the Grandeur 

Member which are probably related to category 7. Category 19, containing miscellaneous small brachiopods, 

does not fit conveniently into the scheme, except that 

occurrences are related to the brachiopod part of the 

"limestone facies."

Generally, the categories listed above go from a beach 

or shallow bottom, possibly of fine lime sand, through 

a region of quiet water and firm bottom, into a slightly 

deeper bottom having slightly more turbulent water. 

The sequence goes from quartz sandstone or limestone, 

through dense limestone, into more shaly limestone or 

bioclastic limestone. This sequence is interrupted by 

the large number of collections from the "fish-scale 

marker bed."

The widespread "fish-scale marker bed" near the base 

of the Meade Peak Member is composed predominantly 

of organic fragments. The unit occupies an area approximately 40 by 80 miles and is underlain by limestone 

and overlain by dark mudstone. Within its area of outcrop, thickness of the bed ranges from about 0.1 to 1.0 

foot. Because it shows no evidence of barrier bars or 

other near-shore features, the bed is thought to have 

been deposited at moderate depths by moderate, rather 

than strong, currents (R. P. Sheldon, written commun., 

1961). Most of the collections in category 22 come from 

this unit; some, but not all, of the collections in category 23 come from this unit. No clear-cut separation of 

the more complete Orbiculoidea from the fragmentary 

specimens was made at the time these categories were 

established because of the difficulty of defining objective criteria; in retrospect this now appears to be significant. A few of the resistant fish fragments, category 

22, come from this unit. Most of these are more characteristic of other units in a beach facies, but they are 

placed next to the other category containing fish remains simply as a convenience.

Another sequence begins with category 23. Some, but 

again not all, collections that contain only Orbiculoidea 

are characteristic of the shallow-water facies of the 

Franson and Ervay Members. While theoretically it 

may have been more meaningful to distinguish the

larger species of Orbiculoidea which are characteristic 

of these members from the smaller species which are 

characteristic of the phosphatic shale members, so many 

of the collections contain indeterminate specimens that 

in practice this distinction is difficult to follow.

Categories 24 and 26 are characteristic of the shallowwater part of the Franson Member and may simply be 

due to slight differences in collecting. A few of the 

indeterminate pelecypods, category 56, may also go here. 

Category 25 containing Lingula is closely related to 24 

and 26 and again may be due only to slight differences 

in collecting. One or two occurrences are in near-beach 

sands.

Category 27, also containing Lingula. is artificial and 

does not fit well into this sequence, It is justified because 

of the emphasis which has been placed on that genus as 

an indicator of shallow water. Lingula does occur in a 

few collections with "limestone" brachiopods; more significantly, it occurs rarely but with a variety of fossils 

in the "claystone facies."

Almost all of the collections in the remaining categories occur in the Meade Peak and Retort Members. 

It is extremely difficult to develop any succession of 

fossil types within these members. This may be due 

to the lack of information on which to base ideas regarding functional morphology, the many combinations of fossils found in the collections, and the intricate 

interbedding of lithologies or some combination of 

these.

The fish scales (category 57) may have settled in the 

quietest and deepest water, but the shell-bearing cephalopods (categories 58, 59, and 60) may have preferred 

more open water. The squids (category 61) may have 

preferred open water, but other evidence suggests shallow depths. For the categories between 28 and 57, no 

special plea can be made for the arrangement adopted.

A claystone sequence begins in shallow water with 

fossils in calcareous claystone or argillaceous limestone, 

perhaps best interpreted as a mud area below the level 

of tidal influence. As stated earlier, it is theoretically 

possible that there may have been growths of algae or 

other marine plants in the area. There is no evidence 

of strong wave or current action. The remainder of 

the sequence contains a limited variety of fossils on a 

relatively soft, extremely quiet bottom of clay or finegrained limestone in deeper water. It goes from beds 

containing Chonetes, Streblochondria, and Cancrinella, 

through those containing Crurithyris and Leiorhynchus, into those containing Polidevcia, the distribution 

of the fossils possibly being controlled by slightly deepening water. It ends with open-water fossils that may 

have lived over the deepest part of the basin.
BIOSTRATIGRAPHY OF PHOSPHORIA. PARK CITY, AND SHEDHORN FORMATIONS 597

PALEOECOLOGICAL INTERPRETATIONS

In this section, the more important details presented 

elsewhere in this paper are summarized and an interpretation of former ecology is drawn from them. Sheldon, Maughan, and Cressman (1967) have constructed 

an environmental map for the Phosphoria rock complex 

at the time of maximum transgression during Meade 

Peak time; Sheldon has also constructed such maps for 

other horizons. Their interpretations were based on 

paleogeography, lithology, and physical stratigraphy; 

the writer's interpretations are drawn almost entirely 

from study of the fossils. These interpretations done 

independently and based on different premises are in 

impressively close agreement.

Because the data on the fossils are necessarily less 

complete than those available from consideration of 

physical stratigraphy, the ecological speculations are 

summarized in terms of stratigraphic units rather than 

time sequences. As a consequence, not all possible lines 

of investigation have been pursued. For example, it is 

possible to demonstrate a salinity gradient in the Franson Member from near-shore hypersalinity to offshore 

normal salinity. Temperature gradients in all likelihood 

also existed. Other speculations based on paleogeography could be listed, but they are far removed from the 

scope of this paper.

Treating the ecological reconstruction by stratigraphic units allows certain generalizations to be made. 

The Shedhorn Sandstone, in effect, is a near-shore quartz 

sand. Such deposits are among the poorest environments for preservation of fossils, and consequently the 

fauna of the Shedhorn is sparse. The Phosphoria Formation is chiefly a silicious ooze and mudflat deposit. 

The ooze contains little except sponge spicules. The 

mudflat environments contain a characteristic "black 

shale" fauna of brachiopods and mollusks. The Park 

City Formation varies from lime sand to lime mud. In 

some areas it bears a restricted molluscan fauna, and 

in other areas, a more varied brachiopod and bryozoan 

fauna.

In detail, the picture naturally is more complex. The 

formations are thick and contain varied lithologies, each 

with its own characteristic fauna. The categorization of 

fossil collections in each member provides a better expression of the f aunal aspect than does a simple listing 

of species. These categories may in time provide a more 

precise method of correlating the variations in faunas 

with the variations in lithologies. In Kansas, where the 

stratigraphic units of Permian age are thinner and of a 

more uniform nature throughout their outcrop, a close 

correlation between lithology and fauna was observed. 

(Mudge and Yochelson, 1962, p. 107-108).

PARK CITY FORMATION 

GRANDEUR MEMBER

Because of the limited number of collections, their 

wide distribution, and the inclusion of rock units of 

several different ages within the Grandeur Member, less 

evidence is available to reconstruct the depositional environment for this member than for either of the 

younger members of the formation. The overall aspect 

of the fauna is tabulated in table 1 by fossil category and 

number of collections.

TABLE 1. Occurrences of fossil categories in the Park City 

Formation

[Grandeur Member includes Wells(?) Formation in Idaho and Ervay Carbonate 

Rock Member includes "Upper Franson" of Utah]

Fossil 

category

2

3...... .........

5..... ..........

6 

7 

8............ ...

9-. . .... .....

10 

11 

12 

13 

14

15 

16 

17 

18 

19 

20 

21 

99

23

24 

25 

26 

27 

29 

41 

48 

49 

52 _

55

57 

Park City Formation

Grandeur Member

o

 a

T3 

W

31 

21 

21

4, 21

22

1

5, 2 2 

2 

»1

1, »2

2

1 

1

Montana

2

i

5 

1 

3

1

5 

1 

1 

1

1

1

fS C3

£

4 

1 

1

2

5

3

5

2

1 

13

2

3

2

1

Wyoming

2

5

3 

1

1

1

1

2 

4

 

1

1

Franson Member

o

3 e

M

1

2

i

i

Montana

5

1

8 

1

1

1

7

4

2 

1

1

1

1

£

i

i

10i

4 

1

1 

1

2 

3 

3 

1 

1 

1

1

1

Wyoming

COM*.

1

3 

6 

3

1

1

8 

5 

7 

4 

4 

6 

5

2

1 

1 

5 

1 

1 

1 

1

1

Ervay 

Carbonate 

Rock 

Member

1 

£

il

U

 i~f

12 

12 

U 11

11

11

Wyoming

1

2 

5 

4 

8 

 .

4

2

2

1 "Upper Franson."

2 Wells(?) Formation.

If the collections that are probably, or possibly, older 

than the type Grandeur are excluded, the remainder, 

although widely scattered, seem to fall into a logical 

pattern. At and near the type section, the fauna consists 

primarily of moderately large to large productoids. 

These are in a coarsely crystalline limestone composed 

primarily of crinoid stems; prior to diagenesis this limestone almost certainly was a lime sand rather than a 

lime mud. The fauna and rock type suggest that this was 

an environment of marine shallow water of normal salinity. The same general fauna and rock type persist
598 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

westward at least to the Utah-Nevada boundary and 

southward into the outcrop area of the Kaibab Limestone. It is not known if this same environment existed 

throughout the southwestern region.

At Hot Spring, Idaho, specimens are less common 

and many are worn. In general, the outcrops in Idaho, 

northward from the type section, have yielded fewer 

fossils and locally have lacked the larger productoids. 

The fact that most of the fossils are moderately to severely worn suggests that the water may gradually have 

shallowed northward, so specimens were subjected to 

more severe currents or wave action.

A few collections to the northeast of the type section, 

for example Brazer Canyon, Utah, and Deadline Ridge, 

Wyo., contain abundant small permophorid pelecypods 

in a fine-grained limestone. This limestone is interpreted 

as an extremely shallow-water deposit possibly accumulating on a near-shore mudflat. At several localities, 

orbiculoid brachiopods occur below these pelecypod 

beds.

Overlying the productoid beds near the type section 

is a thin finer grained limestone crowded with gastropod 

Ortlionema. It clearly is the result of sedimentary sorting and accumulation. The same sort of bed, possibly the 

same unit, has been found to the west in the Oquirrh 

Mountains in Utah. Still further west, in Nevada, the 

uppermost beds of the Grandeur are characterized by 

abundant, severely worn specimens of Composita. These 

occurrences suggest quite shallow water and vigorous 

wave or current action near the end of Grandeur time.

FRANSON AND ERVAY MEMBERS

Collections from the Franson Member to a large extent fall into two general facies as is shown by the distribution of fossil categories in table 1. A molluscan 

f acies containing ScTiizodus, Plagioglypta, and bellerophontacean gastropods is characteristic of southwestern 

Montana and eastern Utah; a bryozoan-brachiopod 

f acies is characteristic of western Wyoming. It is especially from this latter f acies that some varied ecological 

interpretations can be made. Most remarks about the 

Franson fauna apply equally well to the Ervay fauna.

The best preserved and most abundant fossils from 

the Franson Member were obtained in the Wind River 

Mountains. A relatively large number of collections are 

available at several localities. These collections show 

that there is a definite order of change in the fauna 

proceeding upward through the Franson, as has been 

intimated under the discussion of the brachiopods. Less 

complete sequences from outcrops to the north and west, 

in Wyoming, support this sequence of change.

The faunal progression does not start at the base of 

the member but starts at the line of maximum regression of the sea (Sheldon, 1963) within the body of the 

Franson. Few collections were obtained below this line 

of regression. Strong support for the suggested sequence 

of faunal changes described in the following paragraph 

was supplied by identification of this series of fauna 

in reverse order, below the inferred line of maximum 

regression at Fall Creek, Idaho.

The fossils immediately above the line of maximum 

regression, and presumably those in shallowest water, 

are Orbiculoidea (Roemerella). Commonly, specimens 

are abundant; occasionally, a few nuculoid pelecypods 

may be associated. They occur most often in light-gray 

claystones. The next highest beds contain abundant ramose bryozoans, characteristically in dense limestones. 

More commonly, a few specimens of Derbyia and Spiriferina are associated with the bryozoans. At some 

localities, a few pectenoids or myalinoids are associated; 

the mollusks and brachiopods are not mutually exclusive. The overlying beds are lithologically similar but 

are better characterized as Derbyia or Spiriferina assemblages containing some bryozoans.

Collections from the remainder of the member are 

predominated by brachiopods. For the most part, they 

appear to be in more shaly beds but may occur in limestones. Neospirifer, SpJienosteges, Sphenalosia, and 

"Liosotella" each characterize a few collections, but these 

genera so rarely occur in the same collections that they 

are for the most part mutually exclusive. Commonly, 

smaller nonproductoid brachiopods are associated with 

each. A few of the underlying fossils may be in the 

collections, but they are uncommon; mollusks are almost never present. It is difficult to find relationships 

among these collections, but evidence from scattered 

occurrences and from the relative position of underlying and overlying assemblages suggests that they are 

not lateral equivalents but occur upward in the order 

indicated. Beds which are equivalent or higher in the 

sequence contain abundant Echinauris.

The highest beds in the sequence are characterized 

by Batliymyonia and, to a lesser extent, by Muirwoodia. 

As in the underlying beds, some nonproductoid brachiopods may occur; a few pelecypods are also found in 

this faunule. All fossils mentioned earlier may occur 

together, but at least some of this mixing may be the 

result of collections being taken through several feet 

of strata. Some collections containing Bathymyonia as 

part of a mixed fauna show minor differences in the 

matrix adhering to the different fossils. The collections 

containing BatJiymyonia characteristically are in calcareous shales.

Field evidence from Utah and Montana suggests that 

the molluscan f acies may be the approximate equivalent 

of the bryozoan beds. Productoid brachiopods and
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 599

bryozoans rarely occur at the same locality with these 

mollusks. At most localities, collections of orbiculoid 

brachiopods occur near the mollusks, but they may be 

either above or below them. This molluscan facies is 

worthy of further study, for if there is one fossil that 

characterizes the Franson Member, it is Plagioglypta. 

The abundance of scaphopods in this facies is particularly impressive when compared to the rarity of 

scaphopods elsewhere in the Paleozoic.

Plagioglypta and ScJii^odus were members of the 

infauna, but the bellerophontaceans were epifaunal. 

Their common occurrence in this facies suggests a firm 

but relatively fine bottom sediment containing some 

organic matter. A near-beach environment of fine lime 

sand is possible. In a few places, the fossils are abundant and worn, and the shells have formed a fossil 

coquina. Nicol (19M) has suggested that ScTiizodus and 

Plagioglypta may have been able to live in hypersaline 

water. The geographic distribution of this f aunule is 

certainly suggestive of shallow water and possibly 

hypersaline conditions.

The collections from Alpine Creek, Mont., and Forellen Peak, Wyo., are marginal to the brachiopod and 

bryozoan facies of the Franson or Ervay and differ 

from this typical molluscan facies. They are principally 

small pelecypod shells which seem to have been deposited near a beach. In southwestern Wyoming, collections from Deadline Bidge and field observations 

on Commissary Bidge, just to the north, are best interpreted as beach coquinas of mollusk shells, even though 

the fauna is more similar to that of the Franson in the 

Uinta Mountain area. They strongly support Sheldon's 

(1963) interpretation of a shallow barrier or submarine 

ridge within the area of deposition of the Franson sea. 

Except for these few occurrences, there are no indicators 

of depth among the Franson fossils.

The physical stratigraphy of the Franson indicates 

that a widespread regression occurred during the deposition of the unit, and was followed by a widespread 

advance of the sea. Increasing depth would be a correlative of this marine incursion, as would be a gradual 

change in bottom conditions increasing with distance 

from the shore. The changes in the fauna as interpreted 

from functional morphology correlate well with this 

physical picture.

Two extremely shallow-water conditions are suggested. In the first, there is no clearly defined change 

from shallow to deeper water, and a thin sheet of water 

may have extended for many miles eastward in the 

Uinta Mountain area. With such a large shallow-water 

surface, evaporation may have significantly changed the 

salinity from near normal to hypersaline. Where organic matter was present and the sediment size was con269-092 <68 3

ducive to burrowing, a restricted molluscan fauna 

flourished.

In the second suggested shallow-water environment, 

shallowing and the development of mudflats may have 

been more rapid. In such an area, as was found in western Wyoming and in the Uinta Mountains of Utah, 

nuculid pelecypods flourished. These animals may have 

been able to live under conditions varying slightly from 

normal salinity. It is further possible, but not probable, 

that the shallow water supported a growth of marine 

plants to which the Orbiculoidea were attached. Some 

individuals are brokens but there is no evidence of 

strong wave action.

As depth increased, more normal salinity was assured and organisms could lie below the zone of severe 

wave action. Bryozoans flourished on the firm to hard 

bottom that was firm enough to allow for cementation 

of Derbyia. Spiriferina may have attached its pedicle 

to the bottom or to the bryozoan colonies. A few pectenoid pelecypods may have swum into these bryozoan 

meadows. The few crinoids did not form large stands. 

With a slight additional increase in depth, the number 

of bryozoan colonies was reduced, but Derbyia and 

Spiriferina continued to flourish on the firm bottom. 

Other cementing or pedicle-attached brachiopods, such 

as Sphenosteges and Neospirifer, lived on a slightly 

softer bottom.

Although at a slightly greater depth the bottom was 

far from being a soft bottom ooze, it became less firm, 

perhaps because this was the accumulation area bypassed by the finest sediment in the shallower water. 

The productoid brachiopods were able to subsist on this 

bottom because their spines prevented the shell from 

sinking into the sediment. Occasionally a few shallowto deep-burrowing pelecypods invaded this habitat, but 

they were a minor element in the predominately 

brachiopod fauna.

The maximum depth limit is, of course, impossible to 

estimate. Abundance of the fauna implies a prolific 

food supply, which in turn strongly suggests that the 

fauna was living in the photic zone. Depth of the 

Bathyrwjonia beds, presumably the deepest part of this 

sequence, is estimated to be no more than 200 feet and 

possibly less than 100 feet. The bryozoan beds are believed to lie a short distance below the zone of severe 

wave action, but where water circulation would still be 

sufficiently vigorous to bring them food. A depth range 

from 10 to 50 feet seems reasonable. The shoreward 

molluscan fauna may have existed in even shallower 

water.

Marine conditions may have varied from deep water 

and a slightly loose bottom, through an offshore hard 

bottom, to a shore zone of fine quartz sand, or more
600 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

commonly fine lime sand, which has subsequently 

changed diagenetically to a fine-grained limestone. If 

there was any variation in salinity, it may have been 

from slightly less saline in the deepest part, through 

nearly normal salinity in the bryozoans beds, to hypersaline conditions near shore. Current and wave action 

was light to moderate and may have been more vigorous offshore than near shore. The waters were clear 

most of the time. The rarity of bored shells and bryozoans in growth position suggests intermittent 

sedimentation.

The fossil categories recognized within collections 

from the Ervay Member are listed in table 1. The 

Franson collections are not only more diverse but are 

more widespread. Within the Wind River Mountains 

area, a brachiopod-bryozoan facies is found in the 

Ervay that is comparable to that of the Franson.

There are, however, certain differences between the 

fauna of the two units. Fenestrate bryozoans are relatively more abundant in the Ervay; ramose bryozoans 

are more abundant and have an overall larger size in 

most Franson collections. There are a few more mytiloids, and, relative to the number of collections, a few 

more pectenoids in the Ervay. Crinoid stems seem to 

be slightly more common in the Ervay where they occur in association with the bryozoans.

The brachiopod assemblages in the two members also 

show a few dissimilarities. Hustedia is locally abundant 

in the Ervay but not in the Franson. Neospirifer is 

much more common in the Franson than in the Ervay. 

Battiymyonia and Echinauris are a little more common 

in the Franson than in the Ervay. Derbyia, Spiriferina, 

Sphenosteges, and Composita are more characteristic 

of the Ervay than they are of the Franson.

At best, all differences are slight, and the similarities 

between the fauna of the two members are by far in the 

majority. In fact, it is impossible to determine conclusively whether a particular collection is from either the 

Franson or the Ervay. The geographic distribution of 

the Ervay fauna is somewhat different from that of the 

Franson in that the brachiopod facies seems to extend 

further eastward in Wyoming, but again these are 

minor qualitative distinctions.

If the assumptions made earlier about life habits of 

the animals are correct, the slight differences in the 

fauna could well be interpreted as implying that the 

Ervay sea was somewhat quieter and possibly shallower 

than the Franson sea. The greater number of f enestrate 

bryozoans implies the necessity for a larger surface 

area containing more zooids to obtain food for the 

colonies; consequently, quieter waters are suggested. 

The larger number of attached filter feeders, for example, Derbyia and mytiloid pelecypods, suggests both

nonturbid water and a firm bottom. The larger number 

of small pedicle-bearing brachiopods might suggest a 

firm bottom; the lesser number of large productoids 

inferentially supports the presence of a slightly firmer 

bottom.

The Ervay molluscan facies bears the same shoreward relationship to the Ervay brachiopod-bryozoan 

facies as does the molluscan facies in the Franson Member. Within the area studied, the virtual absence of the 

molluscan facies in the Ervay further accentuates the 

slight difference in geographic distribution of faunal 

facies between the two members. The few collections available from this facies suggest that there 

may be relatively more scaphopods and fewer pelecypods in the Ervay molluscan facies than in the Franson 

Member, but additional collections are required before 

a critical study of this facies can be undertaken.

PHOSPHOBIA FOBMATIOH

MEADE PEAK AND RETORT PHOSPHATIC SHALE;

MEMBERS

R. A. Gulbrandsen (written commun., 1961) points 

out that the Retort Member contains a smaller percentage of rare metals, including vanadium, and locally a 

higher percentage of organic matter than does the 

Meade Peak Member. There are some differences in the 

fauna between the two members as shown by the distribution of fossil categories in table 2. The Retort Member contains a larger percentage of Nuculana and 

Pseudogastrioceras than does the Meade Peak. Conversely, the Retort has not been extensively sampled 

and is not as thick as the Meade Peak. In the thickest 

sections of the Retort Member from which collections 

were made, the faunas of the two members are similar. 

These similarities far outweigh the differences, and, 

like the Franson and Ervay Members, the differences 

are of degree rather than kind.

As discussed on page 583, the brachiopods may be 

divided ecologically into those in "limestones" and those 

in "claystones." The mollusks are also readily divided 

into these two groups; pelecypod and gastropod genera 

are limited to the "claystone facies," and the abundance 

of cephalopods and the absence of scaphopods is characteristic of it.

According to W. W. Rubey (oral commun., 1959) fossil occurrences in the phosphatic shales are rare. In the 

vicinity of Afton, Wyo., Rubey estimates that only 

about one in a hundred of the slight lithologic changes 

within a section of the shale bears fossils. Whether this 

observation can be applied to the entire area cannot be 

determined but the vertical distribution of the collections tends to support this observation. This feature 

suggests that the distribution of fossils is more restricted
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS

TABLE 2. Occurrences of fossil categories in the Phosphoria and Shedhorn Formations

601

Fossil category

2

3____ .._.__...__

4__. ____________

5 ___________

6

7___________..__

8 _

9 -

10 ___________

11__ _ _ ____

12___.__________

13. _

14 __________

15-_-_______.___

16 ___________

17 ___________

18 ___________

19 ___________

20 _____ __ _

21 _ __ ______

22 ___________

23 _______

24_____ __ ______

25 ___________

26 __ _ _

27 ___________

28 ___________

29 ___________

30 __________

31 ___________

32 ________

33 -__--__

34______________

35 __________

36 __________

37 ___________

38 __________

39 ___ _________

40- _ _________

41 ___________

42 ___________

43- _ _________

44______ _ _____

45__-__________

46. _ __________

47 __________

48 ____ _______

49 __________

50 __ -__--._ _

51 ___________

52 __ __________

53 __________

54 __________

55 ___________

56 __ ______

57 __________

58 __________

59. __ -___-__-.

60 __________

61- _________

Phosphoria Formation

Meade Peak Phosphatic Shale Member

Idaho

5

5

1

1

2

1

2

14

60 

6 

30 

16 

6 

6 

3 

5 

4 

15 

6 

12 

47 

37 

15 

15 

17 

3 

1 

20 

9 

7 

10 

5 

27 

37 

9 

12 

8 

6 

8 

9 

11 

13 

5 

1 

3 

12 

2 

12 

15

Montana

1

1

1

1

6 

1 

1

2

1

Utah

2

1

1

2 

4 

14 

1 

21 

1 

12 

71

4

1

10

2

3

6 

6 

7 

1 

3 

1 

1

4

2

2

2 

4 

11 

5 

35 

4

Wyoming

3

1

2

1

1

17 

5 

15 

5 

7 

3 

1 

5

2

3

1 

4 

2 

5 

4

2 

6 

2

1 

1

1 

1 

1

4 

1

5 

6

Retort Phosphatic Shale Member

Idaho

1

1

Montana

1

9 

5 

12

4 

4

2 

1

26

2

2 

1

3

Wyoming

1

1 

1

1

2

4

2

7 

7 

7

1 

10

1

1

1

2

1

Lower chert, Rex and Tosi Chert Members

Idaho

11

1 

1

1 

1

7

1

1

1

1

2

1

1

3

Montana

3, M

3 1 

3 1

3 2

2, * 1

1

1, 3 2

1

3 2

3 3

2

3 1

Utah

2

1

1

Wyoming

»1,5

2 

1

2

1

4

4 

1 

3

3 1

2 1,1

3 1

1

Shedhorn Formation

Lower and upper

Members

Montana

4

1 

4

1

1

1

1 1

1

Wyoming

il,2

1

12,1

U,3 i 1

i 2 

i 1

i 2

1

16,1 

i 7 

1 

i 2 

i 1 

1

i 1

1 Lower Member. * Lower Chert Member. Tosl Chert Member.
602 GEOLOGY OF PERMIAN KOCKS IN THE WESTERN PHOSPHATE FIELD

in the shales than in the limestones. Where the fauna 

does occur, however, specimens are commonly abundant.

Even though the fauna is restricted in kind and in 

vertical distribution, this fact is by no means easy to 

interpret. The geographic distribution is of limited use 

because so many of the faunal elements occur at each 

section. There is some indication that Nuculana is limited to sections relatively far from presumed shorelines, 

but even this is tentative.

In the following figures, the approximate stratigraphic position of individual collections and the fossil 

category of each are plotted to uniform vertical scale. 

The purpose is to aid in determination of systematic 

faunal changes analogous to those in the Franson and 

Ervay and to provide another method for summarizing 

fossil distribution data.

The collections from the Meade Peak Member in 

Idaho are shown in figures 158-161. Those from the 

Meade Peak Member in Utah are shown in figures 162 

and 163. Those from Wyoming are shown in figures 

164-166. Finally, the collections and categories in the 

Eetort Member in Montana are shown in figures 167 

and 168.

Like the collections from sections of the Meade Peak 

Member in Montana, collections from measured sections 

of the Ketort Member in Wyoming and Idaho are few 

and scattered and have not been shown in these figures.

It would be helpful if the lithology of the matrix 

were plotted together with the fossil category; however, 

it is considered advisable to await more definitive studies 

of the physical stratigraphy. This is particularly true of 

the southeastern Idaho and southwestern Wyoming 

areas which have yielded most of the Meade Peak collections. The Meade Peak Member is informally divided 

into three units poor in phosphate and two economically 

productive phosphate beds. The lower productive bed 

is commonly underlain by the "fish-scale marker bed" 

and overlain by the "cap lime." As noted on page 582, 

this lower lime bed is composed mostly of orbiculoid 

brachiopod fragments from some sort of physical sedimentary accumulation.

There are a few differences between the dark finegrained "cap lime" and the more characteristic massive 

to shaly argillites of the phosphatic shales. The fact that 

a few pieces of matrix are more crowded with fossils 

than are the bedding planes elsewhere in the members 

suggests that some transportation or lag effect has concentrated them. Several of the very rare members of the 

fauna, for example Anidanthus, are confined to these 

limestones. Teeth whorls of the shell-crushing shark 

Helicoprion are not uncommon in the "cap lime"; a few 

occur elsewhere in the Meade Peak Member.

Bdbylonites and Leiorhynchus are the most characteristic fossils, but other members of the fauna also 

occur in the "cap lime." The local abundance of the 

benthonic pleurotomarian gastropod might indicate 

that this sediment was not stirred up appreciably when 

the animal moved about. These observations suggest 

that the environment of the limestones may not have 

been markedly different from that of the claystones. 

Sheldon (1963, p. 81) notes that interbedded carbonates 

and phosphate-poor claystones are more common 

than the interbedded carbonates and phosphate-rich 

clay-stones.

In spite of the lack of information on the precise 

lithologic composition of the matrix, some generalizations can be drawn from the vertical distribution of 

fossils. Those that appear most obvious are the following:

1. Lingula is rare but is widespread in the Meade Peak 

Member. Where it does occur, it is most commonly 

either fairly low or fairly high in the section.

2. Crurithyris is widespread throughout most of the 

sections in Idaho in a zone a little below the middle 

of most sections.

3. Leiorhynchus is not as common as Crurithyris. Although it occurs throughout the section, characteristically it is found above or below the zone of 

Crurithyris.

4. Ohonetes most commonly occurs near Crurithyris^ 

just below the middle of most sections.

5. Cancrinella commonly occurs relatively high in the 

sections but seldom is the highest fossil found. 

It most commonly occurs with or near Streblochondria.

6. Most assemblages of Nuculana and Orbiculoidea occur in Utah, but a few extend into the southeastern 

Idaho basin.

7. Nuculana are most common in the Ketort Member in 

Montana. In the Meade Peak Member it seems to 

be more common in the sections north of Montpelier and more common in the upper third of the 

member above the Crurithyris but below the Cancrinella zone.

8. Pseudogastrioceras is widespread in the middle third 

of some sections but is most commonly associated 

with Nuculana or near it.

9. Squid tentacle hooks are erratic in distribution, but 

their common occurrence near the base of the section or in thinner sections suggests that the animals may have preferred shallow water. 

There are exceptions to every one of these generalizations. Attempts to make other generalizations about 

the distribution of the various faunal elements have
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 603

Henry 

1309

Rocky

Canyon

1304

Mud 

Spring 

1351

46-12641-37 

45-12639-34 

45-12640-32

48-12638-4 

48-12637-3

30-11712-86 

37-11711-84 

21-11710-83 

43-11709-82 

43-11708-80

- - 36-11706-71

- 46-11705-66

25'

-20'

- 15'

-10'

- 5'

L 0 

VERTICAL SCALE

Gravel Creek 

Divide 

1308

T" 25-11618-74

- 21-11617-71

 24-11616-63

 23-11614-46

Wolverine

Canyon

1322

Bear Creek 

37 (1353)

- 46-11704-49

46-11703-47 

46-11702-43 

60-11701-41 

60-11638-41

- 60-11637-27

- - 43-11700-5

- 15-11699-2

- -15-11698-1

Fall Creek

+ 5-12114-42 39(1338)

- 21-12112-34

 - 60-12111-30

- - 43-12110-27

 - 33-12109-5

 21-12534-57 

53

- - 61-12292-11

61-12291-7 

21-12290-5

 - 36-11612-27

 32-11611-19

- 23-11610-15

 21-11609-10

 - 21-11608-2

- - 21-11607-1

och

lley

314

- 33-11602-104

 23-11505-97

- 34-11604-94

 24-11603-90

 27-11601-83

 26-11600-76

 51-11599-74

 36-11598-73

 23-11597-55

 35-11596-54

 21-11606-52

 47-11595-51

 59-11594-42

 21-11593-33

 34-11592-30

 21-11591-29

 61-11590-3 

 21-11589-1

34-11634-R-l

23-11633-101 North

34-ii632-ioo Wooiey

33-11631-99 Range

12

53-11630-89

 21-11629-83

 53-11628-81

 46-11627-64

 45-11626-48

- 46-11625-47

- 23-11624-46

- 50-11623-42

 33-11622-21

61-11621-3 

: 61-11620-2 

r 21-11619-1

30

 27-10440-88

 23-10439-87

 32-10438-86

 32-10437-85

 32-10436-84

 37-10435-79

 21-10434-76

 54-10433-75

. 24-10432-73

 33-10431-72

 25-10430-70

 55-10429-69

- 42-10428-65

 45-10427-63

- 34-10426-61

 33-10425-59

 35-10424-57

 46-10423-50

 45-10422-47

- 45-10421-36

 41-10420-35

 23-10419-34

 34-10418-32

 34-10417-31

- 33-10416-22

 21-10415-12

 45-10414-10

- 21-10413-4 

- 21-10412-2

FIGURE 158. Stratigraphic position of collections in the Meade Peak Phosphatic Shale Member of the Phosphoria Formation in Idaho from 

Mud Spring to North Wooley Range. Numbers in stratigraphic columns consist of first, the fossil category number of each collection, second, 

the collection number, and third, the bed number of each collection. Vertical scale: 1 inch equals 20 feet. Wolverine Canyon section 

complicated by faulting; upper part missing (B. R. Cressman, written common., May 8,1961).
604 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

Conda mine 

1200

" ^0-9711-142 

51-9710-140

33-9709-138 

. 28-9708-137

Blackfoot A?!

Narr 

12

North

Kendall Canyon y^y !

32-10481-98 ~: 

6J-10479-96 :

North

Rasmussen

Valley

1233

-25'

-20'

-15' 

-10' 

-5'

-0 

VERTICAL SCALE

Ballard

Trench

1316

 - 36-11696-9

 10-11695-1

- 24-10447-79

 32-10446-77

South 

Rasmussen 

Valley 

J232

 50-10444-55

 23-10443-40

 36-10442-22

48-10441-5

46-10472-61 :

38-10486-20

53-10459-12 :

43-10457-9 :

 49-10485-5

-30-10482-99 JL 

; 33-10480-97

-

 55-10478-79

54-10477-78

 45-10476-73 

 54-10475-71 

33-10474-69

 35-10473-62 

: 46-10471-58

 35-10470-48

61-10469-43

 48-10468-41

 45-10467-40

 47-10466-39

 58-10465-37

 58-10464-35

48-10463-34 

 60-10462-31

 21-10461-17

; 19-10460-13

- 53-10458-10

 49-10456-8

3S

37-10503-99 -

33-10524-101

50-10523-100

54-10502-94 

55-10521-89

45-10501-89 

21-10520-84 21-10499-86 -

53-10519-83

54-10518-82 caldwell

Can 

12

 41-10517-74 

19-10516-71

- 34-10515-69

 19-10514-65 ;

46-10513-61

 46-10512-48

61-10511-37

45-10510-31

26-10509-25

21-10508-23

21-10507-21

7-10527-3 :

/on

30

30-10548-81 

30-10547-79

- 35-10546-78

- 33-10545-74 

- 33-10544-73

53-10543-71

58-10542-68

- 58-10541-67

- 41-10540-64 

- 49-10539-63

- 36-10538-61

- 34-10537-59

> 35-10536-57

 19-10535-47

 60-10534-30

 61-10533-20

 57-10532-17

 52-10531-16

- 21-10530-12

 21-10529-7

 22-10528-4

 43-10526-2

/ey 

OWS fej

51 !gj

///

30-10506-111 ;g4

32-10505-109 /S'j 

31-10504-108 //

\ %

y\ /S

% W

\ XXr

/A /A

A <yy

'/A //*

/ //I 21-10500-87 "Xy

52-10498-85 Woodall///

Creek //7

1262//J'

2-10564-91 - 

37-10563-89 

34-10562-88 - 

34-10561-87 -

46-10497-74

33- 10558-69 :

33- 10556-67 :

. 40-10496\ 38

: 44-10495-^" 

 42-10494-37

 35-10493-35

- 23-10492-33 

 50-10491-31

 19-10490-30

 61-10489-25

__ :

- 61-10488-8

Illl

1A

 37-10560-73

 21-10559-71

; 33- 10557-68

 22-10555-55

21-10554-53

 23-10553-51

33-10552-43

46-10551-36

 21-10550-24

Furnace Shale

 "^ap lime"

Lower phosphate bed) MINI! jjjjjjjj-i-*-'-^^ IJjLLJLij-'-

'/ 

41- 9705-77

46-9704-S3

FIGURE 159. Stratigraphic position of collections In the Meade Peak Phosphatic Shale Member of the Phosphoria Formation In Idaho from 

Ballard Trench to Conda mine. Numbers In Stratigraphic columns consist of first, the fossil category number of each collection, second, 

the collection number, and third, the bed number of each collection. Vertical scale : 1 inch equals 20 feet. Correlation by K. T. Montgomery. 

Kendall Canyon section complicated by faulting (B. R. Cressman, written commun., May 8, 1961).
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 605

South

Stewart

Canyon

1306

33-11546-162

-25'

2-9954-186 - 

29-9955-184 

54-9974-183 

34-9958-167 : 

4-9960-165 : 

31-9962-165 : 

31-9963-165 : 

52-9966-159-2 

52-9967-1587 

55-9969-156V 

60-9971-154^ 

52-9972-1547 

19-9787-154'

34-9784-129

36-10121-11

- 0 

VERTICAL SCALE ersistent highgrade bed

49-9922-194 

47-9973-193 

34-9923-189 

30-9924-188

Spring 33-10087-168 

 ^ e "an tnnoeiccj

- 34-11562-108

34-11561-105 

8-11560-104 

-11559-103

32-10054-149 

32-10053-148 33-11516-11 

30-11515-109 - 

33-11514-108 -

34-9785-140Johnson/

Creek/ 

1209/ 58-10080-123 

54-10079-121

33-10078-119

33-10077-115 

2-10076-113

30-11583-84 

1-11582-82 

-11581-81 

580-79

33-9783-122 

34-10028-111 10074-107 

37-10073-105 

28-10049-107 51-10072-104 37-10044-106 23-11511-74 

±v 21-11579-72 34-11510-73

>H-11578-70

46-11509-61 

23-11508-60

40-10070-78 45-11531-60 46-10069-76

35-11530-59 

45-11528-57

48-10042-61 

42-10041-60 

42-10040-59

,42-1 

z/45-1

J-44-10037-56 

46-10036-55

1^60-10097-56 

M6-100S6-55 40-10068-51 

40-10067-50

 6Q-10999-37

 4-10998-35

44-10065-44 

46-10095-44 42-10064-42

+ 46-10094-43 - 21-11573-36

 21-11572-34

1-10997-31 

 4- 52-10996-29

 4- 40-10092-35 

36-100S1-33

+ 40-10108-23/ 

 51-10107-2

21-1154813 j : 21-11549-4 21-11565-1 

1-11547-1

57-9931-1

FIQOEB 160. Stratigraphic position of collections in the Meade Peak Phosphatic Shale Member of the Phosphorla Formation In Idaho from Trail Canyon to West Dairy. Numbers In stratigraphic columns consist of first, the fossil category 

number of each collection, second, the collection number, and third, the bed number of each collection. Vertical 

scale: 1 Inch equals 20 feet. Correlation by K. T. Montgomery. South Stewart Canyon section complicated by faulting 

with possibly some repetition (E. R. Cressman, written commun., May 8, 1961).
606 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

21-10581-9 

46-10580-8 

40-10579-7

Parrs

Canyon

1266

31-10922-101 

35-10921-99 

43-10929-98 

35-10920-97 

30-10919-96 

30-10729

FIGURE 161. StratigrapMc position of collections in the Meade Peak Phosphatic Shale Member of the Phosphoria Formation in Idaho from 

Swan Lake Gulch to Hot Spring. Numbers in stratigraphic columns consist of first, the fossil category number of each collection, second, 

the collection number, and third, the bed number of each collection. Vertical scale: 1 inch equals 20 feet. Correlation by K. T. Montgomery. 

Swan Lake Gulch section complicated by faulting (E. E. Cressman, written commun., May 8,1961).
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 607

Strawberry 

Valley 

1371

-25'

-20'

-15'

-10'

-5'

VERTICAL SCALE

Franson

Canyon

1347

~ ~24-I249Z-l>C 49-47 

- - 22-12491-PC 45

Lake Fork 

1235

- - 26-10800-42

- 25-10799-40

- 26-10798-39

- - 26-10797-38

Little

Brush

Creek 12"

20-10016-19 -

24-10014-16 - 

23-10013-14 '

Zl

r 26-10018-22 

- 24-10017-20

- 26-10015-18 L 

 26-10012-8

 . -

Horseshoe

Canyon

1339

- 24-12282-28

Brush ' 

Creek 24-12276-22 = Gorge Rock

1219 Canyon

 26-10011-25 1220

 26-10010-22

 26-10009-21 

 26-10008-20 : 

 26-10007-19 fc 

V23- 10006- 18 

\24-10005-17

 26-10002-13

 26-10001-10

5

~ 26-9999-26

- 26-9998-25 

- 26-9997-24

\29-9996-23~~~ .-_ 

 26-9995-18

 26-9994-15

 26-9991-1

26-12281-27

26-12280-26

26-12279-2S 

26-12278-24 

26-12277-23

20-12275-21

. 26-12274-20

 26-12273-15

21-10796-27 Diy

Canyon 

1229

"24-10794-28 

- - 26-10793-25

23-10802-H 

57-10801-6

Wolf 

Creek 

1231

T26-10788-3S

26-10787-30 

25-10786-2S

61-10792-9 

21-10791-7

- 61-10784-11

21-12672 

23-12673

26-12677 

21-1267* 

57-12689

FIGURE 162. Stratigraphic position of collections in the Meade Peak Phosphatic Shale Member of the Phosphoria Formation in Utah from 

Little Brush Creek to Strawberry Valley. Numbers in stratigraphic columns consist of first, the fossil category number of each collection, 

second, the collection number, and third, the bed number of each collection. Vertical scale : 1 inch equals 20 feet. Correlation by 

K. T. Montgomery.

269-095
608 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

Rght

Fork of -,e,

Hobble nBrazer

Creek Wanrhodes -0, Canyon 

1271 Canyon '^OS

60-10697-105

60-10693-101

60-10670-44 -

26-10667-37 ;

.

I

\

I270 Li 5'

 26-10704-144

 60-10703-125 

. 26-10702-124

. 58-10701-123

 26-10700-120

 60-10699-107

; 60-10698-106 

: 28-10696-104

 60-10695-103

: 60-10694-102

 60-10692-100

- 58- 1069 I -S9

- 26-10690-98

 28-10689-95

- 20-10688-92

. 2-10687-91 

 20-10686-90

 26-10685-83 

 60-10684-82

 60-10683-81

 60-10682-78 

 60-10681-77

 60-10680-76

60-1067?-71 

60-10678-70 

60-10677-69

60-10676-67

60-10675-66

59-10630-83 - 

58-10628-79 : 

26-10674-60 '. 

58-10625-75 ;

0-10673-55

9-10672-47

8-10671-45 ..

60-12624<JJ 

6-10669-41

9-10668-38

6-10666-36 

6-10665-30

6-10665-30

5-10663-14 

5-10662-13

6-10661-12 

58-10612-12 

1-10660-9 

-10659-8 

6-10658-5 : 

6-10657-4 : 

-10656-3 \ 

26-10655-2 '

'

- 10'

-5'

 26-10652-208

- 24-10651-205 _ Q

VERTICAL SCALE

 26-10650-199 Fort

- 23-10649-198 DoilglaS

1350

- 48-10648-192

 48-10647-187

 48-10646-183 

 48-10645-182

 25-10644-175

- 20-10643-172

 25-10642-151

 60-10641-123

 60-10640-104

 60-10639-102

33-10638-97 

 59-10637-95 

- 60-10636-93 

60-10635-91

58-10634-88

60-10633-87

60-10632-86 

59-10631-85

61-10629-82 

58-10627-77 

58-10626-76 

58-10624-74

60-10623-73

57-10621-66

26-10620-65

25-10619-64

60-10618-58

60-10617-32

21-10616-20 

25-10615-17

55-10614-15

58-10613-14

26-10611-11 

26-10610-10 

26-10609-8 

26-10608-7 

25-10607-6 

26-10606-5 

lx 26-10605-4 

>26- 10604-3

 21-12527P-186

 39-12526P-1S3

- 20-12525-179

Devils

Slide Upper 

1345 Brazer

 24-12524-168

 56-12523-161

 23-12522-158

 21-12521-145

- 56-12520-139

 39-12519-123 

 36-12518-122

 21-12514-112

Canyon

1228

21-10772-58 -

 42-12484^!

 2-12483-10

 39-12482<6 ! 

41-10755-4 

- 5-10780-81

- 23-10779-70

r 23-10778-66

- 23-10777-65

- 23-10776-64

- 45-10773-61 

V41-10774. 

*> 44-10775 ^57 

 45-1077K

 60-10770-53 

 60-10769-50

 41-10768-46

 51-10767-40

 51-10766-39

 33-10765-26

 33-10764-24 

43-10731-19 " 

26-10116-19^

45-10112-16 -

 32-10763-18

 47-10762-15

- 51-10761-13 

- 33-10760-10 

 25-10759-9 

 26-10758-7 

 43-10757-6 

; 42-10756-5

19-10742-139

28-10741-138

North

Crawford

Mountain 

1292

 42-10740-91

 2-10739-83

 60-10738-70

 43-10737-64

- 51-10736-58

 33-10735-42

 42-10734-37

 33-10733-36

- 19-10732<jJ

I 43-10115\,» ' 43-10114' 

^41-10730 \,, 

^41-10113'"

 41-10111-13

 23-10110-1 :

- 23-10985-101

 60-10984-90

- 23-10983-87

- 23-10982-85

 55-10981-84

Laketown 

 33-10979-76 Canyon

 42-10978-71 129°

 52-10977-60

 21-10976-53

 61-10975-51

46-10974-25

52-10973-23

33-10972-22

33-10971-13

33-10970-10

26-10969-1 

43-10968W-1 ~ 

s-43-10967W-2

 23-10960-28

._

 24-10959<||

 23-10963-1$

 36-10962-7 

57-10961-a

FIGURE 163. Stratigraphic position of collections in the Meade Peak Phosphatic Shale Member of the Phosphoria Formation In Utah from Right Fork of Hobble Creek to Laketown Canyon. Numbers In Stratigraphic columns consist of 

first, the fossil category number of each collection, second, the collection number, and third, the bed number of each 

collection. Vertical scale: 1 inch equals 20 feet
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 609

Cokeville

12*

Cumberland 

1346 (147)

24-12562W2

21-12573-52

36-10923-145 

- 21-12572-43

42-10928-135 

46-10930-133 :

 61-12571-32

- 26-12570-28

 21-12569-25

 21-12568-18

 22-12567-16

- 28-12566-15

 57-12565-13

- 47-12564-5

- 21-12563-1

: 39-18889

19

45-10936-193

42-10937-191

5-10938-190

41-10939-188

North Fork

of Pine

Cre 

12

25-10949-178

41-10948-176

41-10947-174

27-10946-171

i-'lolilliie Middle Fork

25-10951-164 of Pine

25-10950-162 rroai, 

10-10954-160 U66K

,12

^5-12470-148 ^5-10942-148

- 41-10941-146

 24-10940-145

- 23-10924-144

. 24-10925-^ 

24- 10926^ "d

- 44-10927-136 

- 42-10929-134

 40-10931-129

 45-10932-127

 40-10933-117

 45-10934-116

- 60-10943-112

 60-10944-111

 46-10945-31

05

- 14-9719-72 :

- 19-9721-59

- 39-9713-15

- 36-9712-1

ek

34

28-9753-81

28-9752-80

28-9751-79

30-9750-78

23-9749-77

28-9720-73

30-97 19A

 23-9718-65

 45-9717-55

- 26-9716-50

- 60-9740-43

 58-9715-42

- 39-9714-35

Coal

Canyon

1201

- - 41-18896

- 23-9745-104

- 25-9743-98

- 3-9742-81

45-9741-75 

60-9733-67 

45-9734-68

 52-13302

 21-13301

 23-13304

FIGURE 164.. Stratigraphic position of collections in the Meade Peak Phosphatic Shale Member of the Phosphoria Formation in Wyoming 

from Cumberland to Basin Creek. Numbers in stratigraphic columns consist of first, the fossil category number of each collection, second, 

the collection number, and third, the bed number of each collection. Vertical scale: 1 inch equals 20 feet.

Lay I and

Canyon

1202

- 24-9754-86

£ 48-9755. 

- 53-9757-75

 44-9758-66

 60-9759-64

-25'

- 20'

- 15'

10'

u 0 

VERTICAL SCALE

Basin 

Creek 

1381
Fall Creek 

39(1338),

Bear Creek 

 37(1353)

Rex Chert 

32 miles

Buck Creek 

60 (1332)

Member of the Phosphoria Formation

64 miles

Fontenel

Deadline Ridge Creek 

107 (1380) 108 (137

9 miles

FIOTJEE 165. Stratigraphic position of collections in the Meade Peak Phosphatic Shale Member of the Phosphoria Formation in Wyoming and eastern Idaho from Fall Cree

Numbers in Stratigraphic columns consist of first, the fossil category number of each collection, and second, the collection number. Vertical scale: 1 inch equals 20 feet. Prepared by E

correlation see Sheldon (1963, pi. 7).
Fall Creek 

39(1338)

6

miles

Fiat Ventre 

Teton Pass Creek Slide 

23 miles 49 (1370) 20 miles 50 (1335) 42 (1326) 32 miles

Tos! 

Creek 

56 (1333) 35 miles

Din w

Lak

Lower chert member, of the

FIGUEE 166. Stratigraphic position of collections in the Meade Peak Phosphatic Shale Member of the Phosphoria Formation in eastern Idaho and Wyoming from Fall Creek

bers in stratigraphic columns consist of first, the fossil category number of each collection, and second, the collection number. Vertical scale: 1 inch equals 30 feet. Prepared by 

ical correlations see Sheldon (1963, pis. 5 and 6).
612 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 613
614 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

been completely unsuccessful. The seemingly random 

distribution of the several kinds of fossils is in marked 

contrast to the situation in the Franson and Ervay 

Members where the regular sequence of fossils can be 

logically interpreted from both functional morphology 

and nature of the sediment.

There are several possible explanations for this pronounced difference in the distribution of fossils between 

the shales and the limestones. The one that seems most 

reasonable is that the shales represent a stable environment that varied only within narrow limits whereas the 

limestones represent an unstable environment that 

changed its character through time. In the stable environment relatively minor changes, especially slight 

changes in the physical character of the bottom sediments, governed the distribution of the few animals that 

were able to live in this generally unfavorable habitat.

To summarize, the Meade Peak and Eetort Members 

are interpreted as quiet-water deposits. Sediments were 

fine grained with much interstitial water. The bottom 

may have been too soft much of the tune for an epifauna 

to exist. Where bottom conditions were better, a restricted fauna flourished. Orbiculoidea^StreblocJiondria^ 

Babylonites, and Ohonetes were limited to the firmest 

bottoms. Cruritlvyris and Cancrinella may have been 

able to live on slightly softer bottoms. LewrJiyncJius 

and the burrowing Nuculana might have been able to 

exist on even softer bottoms. Distribution of the various 

groups of fossils might be governed by local changes in 

bottom conditions, but the overall vertical distribution 

suggests that there might have been a correlation between a slightly firmer bottom and slightly shallower 

water. The fauna was prey to cephalopods and sharks 

but is seldom found with the predators. Other fish lived 

in the waters, above the epifauna and possibly in the 

deeper water of the basin.

Little can be surmised about the chemistry of the 

water. Echinoderms and bryozoans, both excellent indicators of normal marine salinity, are conspicuous by 

their absence, but this absence can be explained by unsuitable bottom conditions. The presence of abundant 

brachiopods is suggestive of normal or near-normal 

salinity. In spite of the fact that a reducing environment existed within the shale members, the water near 

the sediment-water interface was rich in oxygen and 

thus in contrast to the oxidizing environment in the 

shallower water sediments of the limestone members 

(Sheldon, 1963, p. 146). The abundance of fossils provides the evidence for this assumption. R. P. Sheldon 

(written commun., 1961) rightly points out that this 

assumption applies only to those beds that contain fossils; the absence of fossils on most bedding planes is 

evidence that suggests a reducing environment.

As the fauna shows little diversity, less than optimal 

conditions for a benthonic fauna are implied. Part of 

the restriction of the fauna could be due to water cooler 

than that in the seas of calcium carbonate deposition. 

Abundance of Nuculana is slight support for the cooler 

water, but, nevertheless, cool water is a logical corollary 

of deep water.

Considerable attention has been devoted to the possible depth of the phosphate-depositing waters. Phosphates have been reported at depths from beach zone 

to thousands of fathoms. McKelvey, Swanson, and 

Sheldon (1953, p. 59) suggest that the Phosphoria sea 

was 200-1,000 meters deep. To the writer, however, even 

the lesser of these two figures seems extremely large.

The abundance of organisms within shale members 

implies an abundant food supply. In turn, this suggests 

that the animals lived within the zone of abundant light, 

the zone of plant production in the sea. This zone is 

commonly taken to be from the surface to about 200 

feet, most production being within the first 100 feet. 

The writer considers that 200-300 feet is a maximum 

depth for this fauna, but because no precise depth indicators are known among the fossils, other workers 

may prefer hypotheses favoring greater depths.

E. R. Cressman (written commun., 1961), while 

agreeing that the seas during Meade Peak and Retort 

times were moderately shallow, suggests that the sea 

floor was generally deficient in oxygen as indicated both 

by the reduced state of uranium in apatite and the lack 

of disturbance of the sediments by infaunal activity. He 

suggests that the occurrence of fossils could represent 

infrequent freshening of a generally foul benthonic environment. The writer concurs with Cressman in this 

opinion, as the two different lines of evidence are by no 

means mutually exclusive.

Cressman also points out that the downward rain of 

organic debris could support a large population well below the photic zone and that the abundance of fossils 

does not necessarily indicate a high rate of organic 

production. E. P. Sheldon (written commun., 1961) 

notes that sediments rich in organic matter are not 

limited to shallow water and cites Walvis Bay, SouthWest Africa, as an example. While the writer agrees 

with these points as theoretical considerations, he does 

not feel that they apply to the deposits in question.

LOWER CHERT, REX, AND TOSI CHERT MEMBERS

It is advisable to treat the lower chert, Eex, and Tosi 

Chert Members together not only because they are of 

similar lithology, but also because collectively, they contain few fossils. Many of the collections, which years ago 

had been identified in the field as coming from these 

chert units, do not have a chert matrix and contain fos-
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 615

sils characteristic of other stratigraphic units. The fossil 

categories, tabulated in table 2, include these atypical 

collections. Most of these atypical collections reflect 

changes in rock nomenclature.

If the collections that are not from a siliceous matrix 

are laid aside, all collections from the lower chert and 

Tosi Chert Members and many from the Kex Chert 

Member are excluded. The chert matrix collections contain abundant sponge spicules, occasional fish scales, 

and occasional orbiculoid brachiopods. Some of the 

closely associated collections in a limestone matrix contain Lingula and scattered pelecypods and gastropods.

It is generally agreed that spicules form an appreciable bulk of the cherts. It is further argued that solution and redeposition of spicules is the source of most 

of the rest of the chert. The possibility of inorganic deposition of more than half of the chert is discounted 

(Cressman and Swanson, 1964, p. 369). However, the 

organisms, especially sponges, did extract SiO2 from the 

water, and the sponges probably were present in profusion because silica and other nutrients were abundant.

Cressman and Swanson (1964, p. 371), quoting de 

Laubenfels, suggest that the sponge fauna lived in 

water of normal salinity and low current velocity. The 

sponges are believed to have been able to thrive on an 

ooze bottom. Finally, it is suggested that the sponge 

fauna lived at a maximum depth of 50 meters.

The presence of rare linguloid and orbiculoid brachiopods in the spicular cherts tends to reinforce the suggestion of no more than moderate depths for the site of 

chert deposition. Further, the discovery by E. L. Yochelson and T. M. Cheney of mud cracks 2 feet below a 

chert bed in Dinosaur National Monument, Utah, during the 1959 field season, shows that some of the Permian cherts were deposited in shallow water.

Several collections from limestone deserve special 

consideration. The limestones within the Rex Chert 

Member are all most impressive. The few that were examined during 1959 show a remarkable facies change 

from cryptocrystalline chert to coarsely crystalline 

limestone within a few hundred feet. None of the lenses 

were examined in detail, but all appear to be relatively 

small bodies completely enclosed within chert. They 

seem to be less than 100 feet thick.

One lens examined in southwestern Montana and several examined in southeastern Idaho contained only crinoid columnals. The matrix appears to be composed 

primarily of crinoid debris. Other lenses have yielded 

a brachiopod fauna. The collections from Deer Creek, 

Idaho, contain only abundant Anidanthus; those from 

Brazer Canyon, Utah, contain only Antiquatonia; those 

from the South Fork of Sage Creek, Idaho, contain 

both these and other genera of brachiopods.

The fauna from the South Fork of Sage Creek is 

better known because several blocks of silicified fossils 

were obtained. The overall aspect is more similar to the 

dictyoclostid beds of the type area of the Grandeur 

member than to the Bathymyonia beds of the Franson 

and Ervay Members. The similarity, of course, is taxonomically superficial and does not relate to species and 

genera.

Possibly the single most impressive feature of this 

fauna is the poor state of preservation of some of the 

fossils. Many are bored, having both spindle-shaped 

holes in the shells and, more rarely, holes penetrating 

the entire shell thickness. Almost all of the productoids 

lack spines. Some even have worn ornamental ridges. 

Many specimens are broken, but it is not possible to determine what percentage were broken while in the matrix and what percentage were cracked during preparation for examination.

The limestone lenses are interpreted as banks that coexisted during times of chert deposition. Although they 

could have had a variety of origins, a firm part of the 

bottom, possibly associated with a slightly shallower 

depth, would provide satisfactory conditions for settling of pelagic larvae. Because of soft bottoms surrounding these areas, other larvae could survive only 

where the first specimens had already formed a firm 

bottom. This severely limited area would tend to perpetuate itself by further settling of larvae until it was 

finally overwhelmed by ooze.

These features are not considered to be reefs, because 

there is no indication of a firm organic framework 

which would haiv© acted to bind sediment. How much 

debris was shed into adjacent chert is not known. These 

accumulations did persist throughout part of Kex time. 

If colonization of these small favorable areas depended 

on the settling of pelagic larvae, we can expect the variety in fauna which is found among these lenses.

The suggestion that the fauna of these lenses lived in 

shallow water is supported by several facts. First, the 

fossils, even where only crinoid stems occur, are abundant. Second, where other animals occur, the fauna is 

as diverse as in most of the brachiopod-bearing collections elsewhere in the Phosphoria rock complex. Third, 

the worn nature of specimens suggests some wave or 

current action, again an indication of only moderate 

depths at most. A depth of significantly less than 50 

meters is plausible, if not probable.

The large number of crinoid stems, the diverse productoid brachiopod fauna, and the presence of rare 

rugose corals all tend to support the idea that these 

faunas lived in water of normal marine salinity. Perhaps the deeper water surrounding these presumed
616 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

banks was of a slightly different chemical composition 

or salinity.

The limestone lenses appear to be 30-50 feet stratigraphically above the main beds of commercially mined 

phosphate (E. P. Sheldon, written commun., 1961). It 

is difficult to see what part they may have played in 

phosphate deposition, though they may have been incipient during deposition of the lower part of the Meade 

Peak Member. If these banks rose a distance above the 

sea floor, they would have formed a band of slightly 

shallower water extending, with intermittent breaks, 

approximately parallel to the Idaho-Wyoming boundary for some dozens of miles. On the shoreward side 

such a feature might have allowed for some slight differences in water chemistry which triggered the deposition of phosphate.

Alternatively, and more logically, lenses may not 

have become important until the latter part of Meade 

Peak time when they formed a more impressive geographic and hydrographic element in the pattern of 

the Permian sea. The formation of commercial deposits 

having a high total percentage of phosphate seems to be 

the result of the combination of two factors: The deposition of phosphate itself and the paucity of other sediments. The banks could have been instrumental in 

changing the current pattern by inhibiting upwelling 

currents which are postulated as the primary source of 

phosphate; also they could have affected shore currents 

and allowed more sediment to be carried to the Meade 

Peak basin. Moreover, they could have partly affected 

both of these elements.

E. E. Cressman (written commun., 1961) doubts the 

importance of these lenses. He cites the uniform nature 

of the member as evidence that there were no incipient 

banks during Meade Peak time. The distribution of the 

known lenses suggests that they are virtually parallel 

to the strike of shoreward facies. Most damaging to 

the hypothesis, however, is that two of the lenses studied 

in detail show no thickening but rather a replacement 

of an equal thickness of chert.

It is difficult, therefore, to maintain the hypothesis 

presented. By way of a partial defense, it should be 

emphasized that, although the Meade Peak does maintain a uniform character laterally, it does show vertical 

change of a cyclical nature. Furthermore, the relationship of the lenses to shoreward facies is as one would 

anticipate. If the lack of compaction of siliceous ooze 

around these limestone masses is shown to be consistent 

in other areas, it will naturally force the abandonment 

of the hypothesis that these were "banks" of organisms. An alternative explanation that these might be 

the fillings of submarine channels raises more problems 

than it solves. Nevertheless, the limestone lenses within

the Eex Chert Member remain one of the most difficult 

features to place in the overall regional pattern, and 

further study should be devoted to them.

SHEDHOBN SANDSTONE

The few collections from the Shedhorn Sandstone are 

summarized by fossil category in table 2. Because of 

the small number of collections, those from atypical 

lithologies are given undue emphasis, and the fauna 

appears to be more diversified than it actually is.

Cressman and Swanson (1964, p. 364^367) have discussed the environment of deposition and paleogeography of the Shedhorn Sandstone. Because of the degree of particle sorting, the stratigraphic thinning, and 

the shoreward position of the sand with reference to 

the Eex and Tosi Chert Members, the seaward edge 

of the sand sheet was apparently deposited in water 

that was less than 50 meters deep. Moreover, following 

the equations developed by G. H. Keulegan and W. C. 

Krumbein, the water may have been no more than 9 

meters deep at 100 miles from shore.

The limited faunal evidence fully agrees with the assumptions of an extreme shallow depth and a nearshore environment of the formation. Most of the fossils, particularly from the northern exposures of the 

upper member of the Shedhorn Sandstone in Montana 

and some of the northern exposures of the lower member of the Shedhorn Sandstone in Wyoming, are Plagioglypta and Schizodus or Permophorus. Elsewhere, in 

Montana bellerophontaceans are abundant. The assemblage is similar to that in the Franson Member of the 

Park City Formation in Utah, where there is equally 

good paleogeographic and stratigraphic evidence for 

postulating extremely shallow water. On the whole, the 

fossils of the Shedhorn Sandstone commonly are less 

well preserved than those from the shoreward facies of 

the Franson Member.

Although not all mollusks are indicative of shallow 

water, wherever these forms have been reported from 

the upper Paleozoic of North America, there has been 

no evidence of anything other than shallow-water conditions. At Alpine Creek in southwestern Montana, the 

abundance of pelecypods and the worn and bored condition of many of them are suggestive of a beach deposit like the modern-day coquina rock of Florida. At 

Forellen Peak, in northwestern Wyoming, similar 

pelecypods occur, although they are much less abundant 

and the rock is not a true coquina. Local abundance of 

resistant fish remains is evidence of strong wave or current action.

During part, if not most, of Shedhorn time, the bottom may have been reasonably firm and the sediment-
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 617

water interface may have been clear. Support for this 

line of reasoning is given by the presence of large bellerophontacean gastropods. These are interpreted as bottom-dwelling forms requiring clear water to prevent 

fouling of the delicate gills by sediments (Yochelson, 

1960). The occasional presence of Derbyia in Wyoming 

further supports this line of reasoning. Like most larger 

articulate brachiopods, Derbyia was a bottom-dwelling 

form. During its development, the pedicle was lost and 

the animal lived with its interarea cemented to the bottom or to other hard objects. The dense growth of unbroken bryozoan colonies in their living position at 

Tosi Creek, Wyo., is still further evidence of a stable 

bottom and clear water.

Cressman and Swanson (1964, p. 351) note the presence of many columnar bodies within sandstones and 

cherts of this formation and suggest that these may be 

the remains of burrows. Although this is a logical assumption, particularly in view of the shallow-water 

nature of this deposit, exception must be taken here. 

These columnar bodies were observed at several localities during the 1959 field season and exhibit few characteristics that the writer would interpret as indicative 

of burrows. Furthermore, they are strikingly different, 

both in their large size and in their regularity, from 

more typical burrows observed at the West Fork of 

Blacktail Creek in southwestern Montana.

AGE OF THE PHOSPHORIA AND CORRELATIVE 

FORMATIONS

Williams (1959) has discussed the overall correlations of the various rock units within the Phosphoria 

rock complex. For each stratigraphic unit he included 

the fossils that were known to occur in it and based his 

compilation both on published literature and on extensive collections. However, he made no attempt to indicate the relative abundance or distribution of the various species throughout the outcrop area. Table 3 summarizes the distribution data presented in the f aunal 

distribution charts. The reported occurrences of species 

and genera are, in the main, similar to those given by 

Williams, but, as would be expected, a few additional 

taxa have been identified in the collections examined 

and, conversely, several of the taxa previously reported 

were not found.

Table 3 shows what appear to be anomalies. Certain 

fossils are occasionally found throughout the outcrop 

area in stratigraphic units where they are not normally 

characteristic. Other rare fossils seem to show Late 

Pennsylvanian or Early Permian affinities. These exceptional occurrences must be considered before a more 

meaningful discussion of the ages of the various rock 

units can be given.

The apparent anomaly is usually based on the fossils 

from a single collection, and the nature of the collection 

suggests an alternative explanation for its stratigraphic 

position. Some of these collections are mentioned later 

under "Geographic distribution of collections." The 

numbers given in table 3 refer to the anomalous occurrences, which are as follows:

1. From collection 12638, Mud Spring, Idaho; lithology is not typical of Meade Peak Member.

2. From collection 12637, Mud Spring Idaho, and 

11698 and 11699, Eocky Canyon, Idaho; in the 

first locality the lithology is not typical of the 

Meade Peak Member; in the second locality the 

fossils are worn and appear to be reworked.

3. From collections 11698 and 11699, Eocky Canyon, 

Idaho; fossils are worn and appear to be 

reworked.

4. From collection 12631, Montpelier phosphate pit, 

Idaho; collection contains two different lithologies and is thought to be from both Meade Peak 

and Franson Members.

5. From collection 10483, Kendall Canyon, Idaho; 

from a phosphatic shale, Meade Peak Member, 

rather than from the Eex Chert Member as listed 

in the preliminary section.

6. From collection 10484, Kendall Canyon, Idaho; 

considered to be Meade Peak Member rather than 

Eex Chert Member as indicated on field label.

7. From collection 10061, Mabie Canyon, Idaho; considered to be Meade Peak Member rather than 

Eex Chert Member as indicated on field label.

8. From collection 9904, Big Sheep Canyon, Mont.; 

from beds thought to be older than type Grandeur 

Member.

9. From collection 11673, Hogback Mountain, Mont.; 

from beds thought to be older than type Grandeur 

Member.

10. From collection 11644, Little Sheep Creek, Mont.; 

from beds thought to be older than type Grandeur 

Member.

11. From collection 11675, Hogback Mountain, Mont.; 

and collections 9905 and 9906, Big Sheep Canyon, Mont.; from beds thought to be older than 

type Grandeur Member.

12. From collection 9906, Big Sheep Canyon, Mont.; 

from beds thought to be older than type Grandeur 

Member.

13. From collection 11674, Hogback Mountain, Mont.; 

from beds thought to be older than type Grandeur 

Member.

14. From collection 10852, Sawtooth Mountain, Mont.; 

the collection is from a chert, possibily Franson
sp. indet- - .. ..

Antiguatonia cf. A.

sulcatus Cooper _ ...

Squamaria ives

(Newberry) so. indet. _

XX

X

X

X

S

X

X

X

X

Juresania sp. indet- .... Bathymyonia nevadensis (Meek) _____ cf. B. nevadensis 

(Meek).. .....

X

S

x

X

<

<

X

<

X

X

S1 °

^2 p

o> S.S 

gg

XX

"Echinauris" sp.... ... "Liosotella" sp. indet.. Hystriculina cf. H.

wabashensis (Nor- wood andPratten) 

XX

X

X

X

X

X

X

iX

X

Echinauris subhorrida (Meek) _______ sp. indet _ .....

X

X

sp. indet.. _ ...Sphenalosia smedleyi (Muirwood and

X

sp. indet ........... Sphenosteges hispidus (Girty)..-......-. 

X

X

f

<

>

cf. C. arcuatus 

(Girty)..... 

X

(X

<

r!

1

X

X

X

a?

 al'S'S'SP

* ** 2! " ^ f* 

p,$?3 p, 5

"ql^ |

X

X X to to

c£ to

X

X X

X

X

X X

X

X

X

X

XX X

X X do o

X

X X

X X eo to

X

J

cf. C. subtttita 

(Hall)... ........ mira (Girty) __ . 

X

r

\

<

<

X

X

Composita subtttita 

main

X

.18.

...s aU 3 » I? S3

1.5' 0 OA

».^r*cp. 

te1 ^

3

X

X X

X

X

<

><

3

X

X

X

>

>

>

!

f

a'

Ob^ 

"1

V

^g-p.!

X

X

y

y

X

X X

X

X

X

X

X

X

X

X

X

X

X

X

X

cf. 0. (R.)

utahensis (Meek). 

cf. 0(0.)missou- riensis CHlinmQrrn

X

X

X

X

X X XX

X ! X

: x:

<

sp. indet ____ 

Orbiculoidea (Roemerella) utahensis HUnnVI

X X

X X

x

< X X

X

X X

X X

X X

X X

X

X

X X

X

>

li § fflS.

o- o"! *< O

| q; | |

I

XXX

x x

x x

x x

x x

x x

x x

x x

x

x

X

X

!

X

X

X

X X

X X

X X

X

XXX

! x

x x :

Haplistion sp.. __ ...Sponge spicules undet..

>

X

X

X

X

<x

< X 3 CO

<x

Tosi Chert Memb

phoria)

Ervay Carbonate B

ber (Park City)

Eetort Phosphatic S

ber (Phosphoria)

Upper member (She

Lower member (She

Eex Chert Memb

phoria)

Franson Member (P

Meade Peak Phosph

Member (Phospho

Lower chert memb

phoria)

Grandeur Member (

" Upper Franson" 

(Park City)

Eex Chert Memb

phoria)

Franson Member (P

Meade Peak Phosph

Member (Phospho

Grandeur Member (

Tosi Chert Memb

phoria)

Cherty shale mem

phoria)

Eetort Phosphatic S

ber (Phosphoria)

Upper member (Sh

Lower member (Sh

Eex Chert Memb

phoria)

Franson Member (

Meade Peak Phosp

Member (Phospho

Grandeur Member (

Eetort Phosphatic S

ber (Phosphoria)

Upper member (Sh

Lower member (Sh

Eex Chert Memb

phoria)

Franson Member (

Y Meade Peak Phosp

 * Member (Phospho

X

Grandeur Member 

Wells Formation
JiakeveUia'! sp ____ Castianetta sexradiata (C. Branson)- __ 

X

XX X

X

X

>

(Myalinella) meekiDunbar _ 

X

<

Myalina (Myalina) sinunta G.Branson . 

(Myalina) wyo- mingensis thomasi Mmvoll

<

<

a

3, 

3'

*

X

X

X

X

X

X

X

ii

X

X

X

i

X

X X

X

X

x x

X

X

X

j

Xo

X

x x

Polidevcia bellistriata (Stevens) ___ --.-

X

pulchra (Beede 

and Rogers). . 

sp. indet ____ 

X

X

X

X

X

X

X

X

X

<J1

<x

X

i

X

poposiensis (C.

<

<

X

sp. C ofCiriacks montpelierensis cair+irl

X

X

X X

X

I

Nuculopsis sp. A ofCiriacks.- _____

X

X

parvaradiatus

X

Paleoneilo mcchesi a ' 

=>_

1'

5 |

X

X

X

X

X

Hustedia phosphorien- »f«n TirQnsnn

><

A

a,

_.!

3 

D.

5-,

!

X

X

»

X

X

X

X

cf. Skentuckensis

X

X

Spiriferina pulchra

X

X

X

)/

3' 

|

X

X

X X

Rhynchopora cf. R.

B 

o. 

a>

X

X

XX

X

X

X

X

X

X

XX XX

XX X

x: ; x

cf. C. ostiolatus Girty 

X

X

X

X

X

Chonetes ostiolatus

airt.v

X

X

X

X

^

bSB

3§

X

X

X

x

X

XX

X

X

X

Derbyia magna C . Branson. _____

X

X

sp. indet .- Muirwoodia multi~

X

X

X X

X

X

X

>

 o^ 

5

cf. C. ph-osphatka rairt^rt

X

X

X

X

ex

X

i

X

X

Cancrinetta phosphatifa. rairtvl

X

X

J3

=>,

3" 

3.;

X

3.V

1

X

XX

X X

X 

-i 8- 

3-3 

if

X

X

X

Linoproductus cf. L.prattenianus (Nor- Rugatia occidentalis

Tosi Chert Mem

phoria)

Ervay Carbonate 

ber (Park City)

Retort Phosphatic 

ber (Phosphoria)

Upper member (S

Lower member (S

Rex Chert Mem

phoria)

Franson Member (

I Meade Peak Phos

[ Member (Phosph

Lower chert mem

phoria)

Grandeur Member 

X

X

" Upper Franson

(Park City)

Rex Chert Mem

phoria)

Franson Member (

Meade Peak Phos

Member (Phosph

Grandeur Member 

Tosi Chert Mem

phoria)

Cherty shale mem

phoria)

Retort Phosphatic 

ber (Phosphoria)

Upper member (S

Lower member (S

Rex Chert Mem

phoria)

Franson Member 

Meade Peak Phos

Member (Phosph

Grandeur Member 

Retort Phosphatic 

ber (Phosphoria

Upper member (S

Lower member (S

Rex Chert Mem

phoria)

Franson Member 

Meade Peak Phos

Member (Phosph

Grandeur Member 

Wells Formation
cf. E. phosphori- ensis Girty __ .. 

WUkinaia sp. indet 

X

X

X

X

X

X

ueitowes sp.. ____ _. Edmondia stuchburia ... cf. E. gibbosa

X

X

X

X

X

X

Pseudopermophorus jinnettae (Ciriacks) 

X

X

$

,

^

Permophorus albequus

fBp.Aflp.1

X

X*_*

Ol

X

Eoastarte subcircuiaris Ciriaclrs

X

? 

12»

X

Astartelia subquadrata 

G1rtv

X

X

3" 

a. 

\

X

X

-1M, S

^

 fss, ? s'

3 o

is ^gS'

1

X

3>

J?'

! «

-a 

^i 

43 I.

3h§

5 & 

Is.

X

X

X

Q 

3l

?s. » a 

s§

Ho"

A

3

I

5-

X

X

X

X

X

X

X

X X

X

X

X

canalis U. -branson. subovatus C iriacks 

cf. S. wheeleri Swallnw

X

X

X

X

2.

*»

perf

uonocardium sp. indet. 

Schizodus bifidut fMria.p.lrs

X

X

X

 '

X

X ><

OC

V

X

X

X

Pseudomonotis sp. indet. ________

X

X

X

[

X*-

Cyrtorostra varicostata

X

X

sp. indet _.

Camptonectest sp.

in HP*

<

X

X

X

>

X

? cf.'s.'tubicoitaia Ciriacks- ____

X

X

f

i

f

<Q

al

 a.

^a-

 1 8 

 g

X

X

X

Streblochondria montpelierensis (Girty) .... cf. Smontpelieren- xix (fiirt.v)

Xo>

X

Annuliconcha sp ___ Girtypecten sp. indet- ? sn inrlpt

X

X

X X

^

X

X

-J

X

X

X

Xh- 1

to

X

cf. -4delawarensis 

(Girty)... ....... sp. indet .. _ .__

sp. indet _________ Acanthopecten alatus

X

X

X

X

X

vx

X

X

X

X

X

X

X

\s

X

X

X

[

cf. A. vanvleeti 

Beede ___.

X

v

X

X

<

X

O O«5

fC°£f

lirfe

5-B 2J 3

Ifil 

1 «

X

X

X

X

X

X

X

X

X

cf. A. phosphaticus 

(Girty)... .......

Aviculopecten phos- *nhfjfirt/.» fliri-v

X

X

X

Tosi Chert Mem

phoria)

Ervay Carbonate 

ber (Park City)

Retort Phosphatic 

ber (Phosphoria

Upper member (S

Lower member (S

Rex Chert Mem

phoria)

Franson Member 

Meade Peak Phos

Member (Phosp

I Lower chert me

| phoria)

Grandeur Membe

" Upper Franso

(Park City)

Rex Chert Mem

phoria)

Franson Member 

Meade Peak Phos

Member (Phosp

Grandeur Membe

Tosi Chert Mem

phoria)

Cherty shale me

phoria)

Retort Phosphati

ber (Phosphoria

Upper member (S

Lower member (S

Rex Chert Mem

phoria)

Franson Member 

Meade Peak Pho

Member (Phosp

Grandeur Membe

Retort Phosphati

ber (Phosphoria

| Upper member (S

Lower member (S

[ Rex Chert Me

phoria)

Franson Member 

1 Meade Peak Pho

| Member (Phosp

Grandeur Membe

Wells Formation
Ostracodes undet-- 

Fish remains __ 

X!

Xj

Xi

Xi

X|

Xi

XI

-x !

Xi

Xi

XI

x:

XX

XX

X

X

i

X

X

I

X

1

X

X

X

X

X

X

x

X

^

1

f

!

x

D

X a

»

5*

I

?

3

x

X

o

o

4

1

X

X

X

X

X

X

X

3

 + 

?

^

T>« 

X

^

f<?3

X

5

01 §

^11D 2.

SJ>

>§

X

X

X

X

X

X

13

1

3

X

»"§'

"'E

1"p

x

S S& o

 SrfW O

5|g|

f^o 3

5-g « 0 

*S ^

« §*

*/

X

X

X

i

3 01

llJ 

*p

X X

CJ a.'

ES

1 

O

3

x

% 

1

^

X

?

1

0,

3

X

Orthonema vt.0socorX

" Trachydomia" n. sp_ Naticiform gastropod indet.--- _-

X

X

Cy elites? sp. indet ___ Naticopsis (Jedia) sp. indet _____

X

X

bt

i 

?3

x

3C*

ED-f

X

X

Plathywortheniat indet- Glabrocingulum coro- natum H. Chronic _ ?n. SD ___ 

X

X X

1

 >

3

5" 

a<-D 

 *

X

X

X

w n 

3 §

II

otf

X

X

X

*

X

XX

X

i

~,ta Isj

^PI-S 3-S^KjS

f5-|i

X

X

X

X

X

X

71

X

3

1T>

X

X

X

cf. B. deflectus IB..

X

Bellerophon deflectus 

H. Chronic. ___

X

31

X

3^

X

X

3

X

Warthia fissusYochel- son ___

X

subpapillosus ( White)-. 

X

X

X

X

Eupfomites crenu- latus Yochelson __ sp. indet ___ ....Euphemitopsis cf. E.paucinodosus Yochel- son._ ____ .

X

X

X

X

X

X

X

X ^

X

X

n

3

D

X

)/

Plagioglypta canna (White). 

X

X

X

X

en

XX

x

s/

X

3

19 

-f

X

X

cf. S. carbonaria fGirty). -- 

X

Sanguinolttes elongatus Ciriacks. __

Tosi Chert M

phoria)

Ervay Carbon

ber (Park Ci

Retort Phosph

ber (Phospho

Upper member 

Lower member 

Rex Chert M

phoria)

Franson Memb

Meade Peak Ph

Member (Pho

Lower chert m

phoria)

X

Grandeur Mem

" Upper Fran

(Park City)

Rex Chert M

phoria)

Franson Memb

I Meade Peak Ph

Member (Pho

X Grandeur Mem

Tosi Chert M

phoria)

Cherty shale m

phoria)

Retort Phospha

ber (Phospho

Upper member 

Lower member 

Rex Chert M

phoria)

Franson Memb

Meade Peak Ph

Member (Pho

Grandeur Mem

Retort Phospha

ber (Phospho

Upper member 

Lower member 

Rex Chert M

phoria)

Franson Memb

Meade Peak Ph

Member (Pho

Grandeur Mem

Wells Formatio
622 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

Member or Rex Member equivalents, not from a 

phosphatic shale.

15. From collection 10829, Cedar Creek, Mont.; in a 

sandstone matrix, and thought to be from lower 

part of Shedhorn Sandstone rather than from 

Retort Member.

16. From collection 12248, Bull Lake, Wyo.; from beds 

thought to be older than type Grandeur Member.

17. From collection 12249 Bull Lake, Wyo.; from beds 

thought to be older than type Grandeur Member.

18. From collection 15153, Dinwoody Lakes, Wyo.; 

from beds thought to be older than type Grandeur 

Member.

19. From collection 12152, Dinwoody Lakes, Wyo.; 

from beds thought to be older than type Grandeur 

Member.

20. From collection 12201, Tosi Creek, Wyo.; from beds 

possibly older than lower part of Shedhorn Sandstone.

21. From collection 18897, Middle Fork of Pine Creek, 

Wyo.; in a limestone matrix and thought to be 

from Ervay Member rather than from Retort 

Member.

22. From collection 9729A, Middle Fork of Pine Creek, 

Wyo.; thought to be from Ervay rather than 

from Retort.

23. From collection 13310, Basin Creek, Wyo.; the 

specimen is worn and possibly reworked.

24. From collection 122264, Bull Lake, Wyo.; the 

lithology of this collection is identical with an 

Ervay collection immediately overlying.

25. From collection 12166, Dinwoody Lakes, Wyo., and 

collection 12262, Bull Lake, Wyo.; the Bull Lake 

specimens found in a phosphatic matrix, are worn 

and appear to be reworked.

26. From collection 13347, Deadline Ridge, Wyo.; the 

specimens, found in a phosphatic matrix, are 

worn and appear to be reworked.

PHOSPHOEIA FORMATION

MEAIM3 PEAK ANI> RETORT PHOSPHATIC SHAMS 

MEMBERS

The Meade Peak Member is the approximate equivalent of the Franson Member. More detailed stratigraphic studies (Sheldon 1963, p. 84; McKelvey and 

others, 1959, p. 3) suggest that the basal part of the 

Meade Peake may be equivalent to the uppermost part 

of the Grandeur Member of the Park City and that 

the bulk of the Meade Peak may be equivalent to the 

lower part of the Franson Member. Although many 

local lithologic correlations remain to be worked out, 

it is possible that the line of maximum regression within

the Franson (Sheldon, 1963, p. 124-125) may nearly 

coincide with the upper boundary of the Meade Peak 

Member throughout most of the Meade Peak outcrop.

The Retort Member is approximately equivalent to 

the uppermost part of the Franson Member, throughout most of the outcrop area. This is not to be confused 

with the "upper Franson" of Utah as used in this 

report. Some of the Retort Member may be as young 

as equivalents of the Ervay Member, but this relationship is less obvious and more difficult to prove.

The physical stratigraphic data implies that most, if 

not all, of both the Meade Peak and Retort Members 

are equivalent to the Franson Member. Some minor 

differences between the faunas from the two shales are 

analogous to the differences between the Franson and 

Ervay faunas. However, the differences between the 

faunas of the two shales are fewer than the differences 

between the faunas from the two limestones, and much 

of the difference may be due to the thinner section and 

less extensive collecting from the Retort. This faunal 

similarity between the two members may be a further 

reflection of the relatively short time interval represented by both members and the intervening strata.

Most of the information on the age and correlation of 

the Meade Peak is derived from study of the cephalopods. These were first considered to be of mid-Permian 

age (Miller and Cline, 1934) and more likely equivalents of the Leonard Formation than of the Word. 

Later studies of the cephalopods from southwestern 

Wyoming (Miller, Furnish, and Clark, 1957) were 

more indicative of a Leonard equivalent. These same 

authors also noted the occurrence of Pseudogastrioceras 

simulator (Girty), the most common Phosphoria 

species in the Kaibab Limestone.

The suggested Leonard correlation based on cephalopods is at variance with that indicated by the brachiopods. G. A. Cooper (in Dunbar 1960, p. 1769), in discussing Cancrinella phosphatica (Girty), remarks that 

this species ". . . is confined to the higher Word and its 

equivalents." The Permian faunas described by Cloud 

(1944) and Cooper (1953) from Mexico have some 

species either closely related to or conspecific with those 

in the phosphatic shales of the Phosphoria Formation. 

These and associated Mexican brachiopods appear to be 

closely related to those in the type Word. The brachiopods are also dated as no younger than Word equivalent 

by their association with Waagenoceras.

The remaining faunal elements contribute virtually 

no information about the age of the phosphatic shales. 

The Babylonites species are not conspecific with those 

from western Texas and seem to be less like species 

from high in the Word Formation than like those from 

low in the Word and high in the upper part of the
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 623

Leonard Formations. The pelecypods and fish fragments have not been studied in detail.

Part of the question of correlation certainly is due 

to semantic difficulties. For many years there has been 

some confusion in use of the terms "upper Leonard" 

and "lower Word." Some of the paleontologists engaged 

in study of the western Texas fossils now recognize that 

one characteristic fauna occurs in the upper part of the 

Leonard and lower part of the Word, and there is no 

"faunal break" at the formational boundary. Some 

authors refer to this fauna as Leonard, and others refer 

to it as Word. There has been a certain amount of misinterpretation, but the Leonard age used by A. K. Miller 

and associates probably refers to the Leonard (upper 

part) and Word (lower part) equivalents. Nevertheless, 

the problem of age is still unresolved because the molluscan evidence suggests a late Leonard-early Word 

age, and the brachiopod evidence suggests a late Word 

age.

LOWER CHERT, REX, ANI> TOSI CHERT MEMBERS

Field studies have demonstrated that (1) the lower 

chert member is in large measure the lateral equivalent 

of the Grandeur Member in one direction and part of 

the Meade Peak Member in another, (2) the Eex is 

the equivalent of the Franson Member in one direction 

and the lower part of the Shedhorn Sandstone in 

another, and (3) the Tosi is the lateral equivalent of the 

Ervay Member in one direction and the upper part of 

the Shedhorn Sandstone in another. The chert members themselves contain practically no fossils that can 

be used to determine age.

Fossils found in the chert matrix are sponge spicules, 

inarticulate brachiopods, and fish remains, but none 

of the fauna is indicative of any particular subdivision within the Permian or even of Permian age. The 

isolated spicules probably will never contribute significant information on the age of the cherts (E. M. Finks 

oral commun., 1960), nor will detailed study of the few 

inarticulate brachiopods probably ever contribute much 

additional stratigraphic information. The fish remains 

are virtually unknown and thus theoretically hold some 

promise for future investigation. Their fragmentary 

nature, however, suggests that their study will not provide significant contributions to biological or stratigraphic knowledge.

The stratigraphic position of the few mollusks found 

in the collections from these members is uncertain. As 

noted earlier, the field assignment of mollusk collections from a limestone matrix to the chert members may 

be erroneous. Even if these mollusks do belong to the 

members as assigned, the fossils are almost without 

exception poorly preserved, and reliance can only be

placed on the overall appearance of the collection rattier 

than the specific or generic identity. Within this broad 

framework, the few fossils in limestone doubtfully from 

the lower chert member in Wyoming are suggestive of 

the Grandeur member, and those doubtfully from the 

Tosi Chert Member in Wyoming are suggestive of the 

Eetort Phosphatic Shale Member. The mollusks in finegrained limestone from the Eex Chert Member in 

Idaho are somewhat better preserved and are more indicative of the Meade Peak member. It is recognized that 

these same pelecypods occur in the Eetort, but stratigraphic considerations seem to rule out correlation of 

of the Eex with that member.

In contrast to these few molluscan collections, the 

fauna of the limestone lenses within the Eex Chert 

Member contain stratigraphically useful brachiopods. 

These lenses have not been adequately sampled, however, and further collecting may prove rewarding. The 

fauna at the South Fork of Sage Creek is best known 

because silicified fossils were obtained there.

The three largest brachiopods at this locality are 

BatJiymyonw nevadensis (Meek), Kochiproductus cf. 

K. longus (Meek), and Antiquatonia cf. A. sulcatus 

Cooper. KocTiiproduotus has not been observed in collections from the Franson and Ervay Members, and 

Antiquatonia sulcatus, in association with a varied 

brachiopod fauna, has been described from beds in central Oregon thought to be equivalent to the lower part 

of the Word formation (Cooper, 1957b, p. 18). The 

ranges of the various Permian species of KocJiiproductus are, as yet, not well known.

It is unlikely that all the limestone lenses within the 

Eex Member occur at the same stratigraphic level. 

However, it is equally unlikely that there is enough 

variation in stratigraphic position of these lenses to 

materially modify the general tentative age determination, based on one brachiopod, of equivalence to the 

lower part of the Word Formation.

Several of the most fossiliferous collections from the 

Tosi Chert Member in Montana, particularly from the 

West Fork of Blacktail Creek (1302), are from calcareous mudstone rather than the bedded chert which is 

characteristic of the member. The assemblage is unique 

to the southwestern Montana area, but, with the exception of Leptodus, no genera are present which are not 

found in either the Franson Member, the Ervay Member, or both. The Leptodus (Dutro and Yochelson, 

1961) is a long-ranging form that occurs in western 

Texas from fairly low in the Leonard Formation to 

relatively high in the Word Formation. The preservation of Leptodus and other specimens from this locality 

is by no means good, and consequently, further collecting will probably not result in the finding of specifically
624 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

identifiable material that can be correlated with the 

standard North American section. The fauna as a 

whole, because of the relatively large variety of mollusks and the rarity of larger productoids, is more suggestive of the Ervay Member than any of the other 

stratigraphic units examined.

PARK CITY FORMATION 

GRANDEUR MEMBER

Williams (1959, p. 36) indicated a Leonard age for 

the Grandeur Member and based this age on collections 

from Hobble Creek, Utah, which contained, in particular, Squamaria ivesi (Newberry). A similar fauna has 

been found at the type locality and elsewhere in the 

vicinity of Salt Lake City, Utah. Additional evidence 

for the age of the Grandeur is provided by the collections from Cephalopod Gulch. The molluscan fauna 

identified is strikingly similar to that of the Kaibab 

Limestone in northern Arizona (Chronic, 1952), the 

lower part of the Bone Spring Limestone, and the 

Leonard Formation in western Texas.

The possibility that the Grandeur Member, referred 

to in earlier literature as the lower part of the Park City 

Formation, could be of Pennsylvanian age has been 

ruled out (Williams, 1959, p. 36, footnote 12). It is 

hoped that this erroneous age determination will be 

dropped from the literature. Nevertheless, this does not 

imply that all the rocks identified as Grandeur during 

the field investigations are of Leonard age, because only 

in southeastern Idaho and the Wasatch Mountain area 

of Utah is the faunal evidence for this age unequivocable. To the east of the Wasatch front, scattered occurrences of poorly preserved Squamaria, which may be 

S. ivesi, suggest that rocks extending as far east as 

Horseshoe Canyon (1359) on the north side of the 

Uinta Mountains are of the same age.

In marked contrast at Big Sheep Canyon (1224) in 

southwestern Montana, there is nothing in the fauna to 

indicate a Leonard age. Poorly preserved Linoproductus and Hystriculina show features of L. prattenwnus (Norwood and Pratten) and H. wabasliensis 

(Norwood and Pratten), respectively. The presence of 

Platycrinites columnals, the pelecypod Annuliconcha, 

and a complete sponge is unique to this locality; the 

presence of a trilobite pygidium is virtually unique.

The sponge has been identified by E. M. Finks (personal commun., 1960) as Haplistion sp. (Demospongea, 

Lithistida, Ehizomorina). According to Finks, this 

genus is a synonym of Pemmalites Dunikowski. He 

states that the sponge is related to a group of species 

of Haplistion that range from Mississippian through 

middle Permian rocks in various parts of the world. In 

North America, related species are known from the

Magdalena Group (Des Moines equivalent) of New 

Mexico and from the type Wolfcamp Formation of 

Texas (Finks, 1960). The Montana specimen is probably a different species, and its age could be as young 

as Leonard equivalents. The rest of the fauna suggests 

an age older than Leonard.

The remaining collections from Montana that were 

identified in the field as Grandeur do not suggest a 

Leonard age; one or two, in fact, indicate an older age. 

These are discussed on p. 631. The majority contain 

no diagnostic fossils, and determination of age must 

await the collection of additional material. At this time, 

there are no collections available to suggest that rocks of 

true Grandeur age exist at any of the Montana sections 

measured.

In Idaho, collections from the divide between Trail 

and Wood Canyon (K) possibly may be older than 

Grandeur. Most of the remaining brachiopod collections 

may be indicative of Grandeur age, but it is to be emphasized that correlations are tenuous and based on little 

faunal evidence.

Eastward from the articulate brachiopod localities, 

two sections in Idaho have yielded Orbiculoidea,' northeastward one section contains permophorid pelecypods. 

Still further northeastward only a few fish fragments 

were found. Present knowledge indicates that none of 

these fossils is confined to a particular part of the late 

Paleozoic. Their inclusion within the Grandeur makes 

a logical facies pattern, and purely on this basis they 

are considered to be Grandeur and thus of Leonard age.

In Wyoming it is more difficult to determine the age 

of the pre-Meade Peak rocks. In western Wyoming, 

particularly in the southwestern part of the State, pelecypods and orbiculoid brachiopods occur to the east of 

Idaho collections that contain typical Leonard age fossils. Although the fossil assemblages cannot be dated 

intrinsically, a logical regional interpretation of facies 

changes suggests that they are of Grandeur age and 

comparable to the few Idaho localities just mentioned.

The collections from Bull Lake (82) and Din woody 

Lakes (75) are in marked contrast to those mentioned 

in the preceding paragraph. They resemble nothing 

else from the Grandeur Member, either in Wyoming 

or the other three States. Some parallel can be drawn 

between the Dinwoody Lakes collections and those from 

Big Sheep Canyon (1224) in Montana, on the presence 

of fenestrate bryozoans, Hystriculma, and a trilobite 

pygidium, but other specimens are not common to the 

two areas. The peculiar fauna suggests that these rocks 

may be older than the type Grandeur Member, but 

neither the Bull Lake nor the Dinwoody Lakes collections can be conclusively dated as either Pennsylvanian 

or Permian.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 625

In summary, the type Grandeur and the Grandeur 

in north-central Utah and southeastern Idaho contain 

a brachiopod fauna of Leonard age. To the east, in the 

Uinta Mountains area of Utah, beds contain inarticulate brachiopods and pelecypods and may be of the 

same age. To the northeast, in the Wind River Mountains of Wyoming, beds called Grandeur may be older. 

To the north and northwest at scattered outcrops in 

Idaho, beds older than type Grandeur also may be 

present. In southwestern Montana, the Grandeur beds 

are almost certainly older than those to the south.

FRANSON AND EBYAY MEMBERS

Williams (1959, p. 37) listed the fossils from the 

Franson and Ervay Members primarily on the basis 

of earlier work by Girty (1910,1920, 1927) and Branson (1930). These lists do not distinguish "upper Franson" or Ervay equivalents in Utah from the true 

Franson of Wyoming and thus mask possible faunal 

differences between the two members. In the identifications reported in the faunal distribution charts and 

summarized in table 3, it can be seen that the differences 

between the Ervay and Franson in terms of the species 

and genera confined to each member are negligible. Most 

of the apparent differences between these faunas are 

due to the identification of more mollusks, especially 

pelecypods in the Ervay. Most of the species that are 

unique to the Ervay occur at one or two localities where 

they are uncommon to exceedingly rare; in terms of 

the total fauna these differences are inconsequential.

Williams (1959, p. 40) wrote "The faunas of the parts 

of the Park City above the Meade Peak are not definitely known to be younger than the Word, but some 

may be younger. * * * The widespread appearance 

above the Word of reef facies and of other beds not of 

normal marine facies could account for the absence in 

Texas of faunas that may have continued into postWord time in the Rocky Mountains and Great Basin 

regions." The recent Permian correlation chart (Dunbar, 1960) shows the Ervay to be near or at the top of 

the Capitan limestone because of a reported occurrence 

of Gerster brachiopods and Capitan cephalopods. The 

Gerster Formation of western Utah and Nevada is commonly considered to be the equivalent of the Ervay 

Member.

If it is granted that the underlying Grandeur is 

correlative with the upper part of the Leonard Formation and the lower part of the Word Formation, at least 

four correlations are possible: (1) The Franson Member could be equivalent to the lower and middle parts 

of the Word, and the Ervay Member could be equivalent 

to higher parts of the Word; (2) the Franson could be 

equivalent to the lower and middle parts of the Word,

there could be a diastem, and the Ervay could be equivalent to the Capitan; (3) there could be a diastem above 

the Grandeur, the Franson could be equivalent to higher 

parts of the Word, and the Ervay could be equivalent 

to Capitan; and (4) there could be a diastem above the 

Grandeur and both the Franson and the Ervay could 

be Capitan equivalents.

To the best of the writer's knowledge no correlations 

with post-Capitan rocks are currently employed, and 

there seems to be no evidence for seriously considering 

this possibility. Of the four possibilities listed, the 

writer prefers the first but cannot rule out the third. 

The second and fourth theoretical correlations find little 

support either in the physical stratigraphy and regional 

relations of the rocks or in their faunas.

If a later Word age is indicated for the upper part of 

the Franson, the line of maximum regression within the 

Franson Member may then mark the approximate position of the Leonard-Word boundary (Sheldon and 

others, 1967). However, if the entire Franson is correlated with the lower part of the Word, the FransonMeade Peak boundary in southeastern Idaho may correlate with the Leonard-Word boundary. Unfortunately 

in no part of the area studied is there a fossiliferous 

sequence suitable for unequivocable establishment of 

this boundary. Moreover, the precise position of this 

boundary does not appear to be important.

As noted earlier, in a broad sense both members are 

characterized by two facies. The molluscan facies is 

best developed in the Franson Member in the Uinta 

Mountains area but occurs in the Ervay at Bull Lake 

and eastward into Wyoming. The brachiopod-bryozoan 

facies of both members is best developed in the Wind 

Eiver Mountains of Wyoming. Present knowledge 

shows that the two faunas provide slightly conflicting 

stratigraphic information.

Bellerophon deflectus H. Chronic has been recorded 

from the Franson Member at several localities in Wyoming. This species is characteristic of the Bone Spring 

Limestone, the Kaibab Limestone, and the upper 

Leonard-lower Word sequence. EupTiemitopsis subpapillosus is common in the Franson and occurs in the 

Glorieta Sandstone in New Mexico. These few fossils 

suggest a late Leonard to early Word age for the Franson Member.

Additional support for this correlation is given by the 

occurrence of the sponge Actinocoelia maeandrina Finks 

in the upper part of the Franson Member near Dubois, 

Wyo. (Finks and others, 1961, p. 554). The species is 

characteristic of the Kaibab Limestone, the upper part 

of the Bone Spring Limestone, and lower "transition 

facies" of the San Andres Limestone. A similar species
626 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

occurs in the lower part of the Word Formation in the 

Glass Mountains of western Texas.

Conversely, Dr. G. A. Cooper (oral commun., 1960) 

has suggested that a collection from near the top of the 

Franson Member along the north canyon wall of the 

Washakie Reservoir not far from Fort Washakie in the 

Wind River Mountains is, like the fauna of Word 

"limestone four," from high in the Word Formation. 

Comparison of the two brachiopod assemblages is difficult because that of the Franson is much less varied 

than that of the Word, and few species are common 

to both limestones.

Earlier, Cooper (1957b, p. 18) provisionally correlated a Permian fauna from east-central Oregon with 

the lower part of the Word and, by implication, with 

the Phosphoria. He also suggested that the fauna of the 

Monos Formation in Mexico (Cooper, 1953, p. 21-80) 

was correlative with the middle and upper parts of the 

Word and was younger than the Phosphoria. There is 

some similarity between these Oregon collections and 

those from the Franson, but a closer correlation appears 

to be with the Rex fauna.

Faunas from the Monos Formation of Mexico are divided into eight zones, and the sequence consists primarily of a limestone, a shale, and a limestone. The 

shale contains a fauna similar to that in the Meade Peak 

and Retort Members. The faunas within the limestones 

suggest that there is more similarity to a FransonRetort-Ervay sequence than there is to a Grandeur 

(Kaibab)-Meade Peak-Franson sequence. If Cooper's 

(1957b, p. 18) correlation of the lower part of the Word 

and Phosphoria applied only to the Franson, the Mexican correlation would suggest that the entire postGrandeur part of the Park City Formation was of 

Word age. This suggested interpretation is put forth 

most tentatively because it is based on the overall aspect 

rather than the identity of species within the 'various 

faunas.

If the entire Franson Member is correlated with the 

upper part of the Word Formation, more important 

than the position of the Leonard-Word boundary is the 

age of the Ervay Member. In the past, considerable emphasis has been placed on the occurrence of Spiriferina 

pulchra (Meek) in the Ervay Member. The Spiriferina 

fauna is characteristic of the Ervay Member and the 

upper part of the Gerster Formation in western Utah 

and Nevada and also occurs in the Franson Member. 

Spiriferina pulchra and its associates may not occur below the line of maximum regression within the Franson 

Member, but too few collections are available from below this line to be significant.

It is possible that the Ervay and it equivalents may 

be correlative with the lower part of the Capitan Limestone, but several lines of argument are opposed to a 

correlation with the uppermost Capitan (Dunbar, 

1960): (1) As noted elsewhere within this paper, slight 

differences between the Franson and Ervay faunas are 

in degree, not kind, (2) if the presence of Cancrinella 

phosphatica (Girty) and Leiorhynchus in the Retort 

Member is used as evidence for "higher Word" age 

(Cooper in Dunbar, 1960, p. 1769), its occurrence stratigraphically just below the Ervay suggests that the 

Ervay does not necessarily include much of Capitan 

time, (3) "Echinoconchus" ( Bathymyonia) nevadensis, a fossil which does occur in the Ervay, is shown by 

Dunbar (1960) as ranging from just below the middle 

of the Word to just above the middle of the Capitan, 

and in the rocks studied, this species and Spiriferina 

pulchra ha've coextensive ranges, and (4) in the Wind 

River Mountain area there is no suggestion of a major 

stratigraphic break above the Franson Member, and 

there is a relatively thin sequence approximately 150 

feet between the Franson fauna, dated by Cooper as 

"high" Word, and the top of the Ervay.

A detailed biometric study of the Franson and Ervay 

fossils may eventually indicate slight but persistent differences in what have here been identified as the same 

species. This sort of study, combined with more detailed 

information on the distribution of brachiopod fauna in 

western Texas would allow one to make more precise 

correlations than those which have been indicated. 

Pending such studies, however, the available evidence 

indicates a Word age for the Franson Member and a 

late Word to early Capitan age for the Ervay.

SHEDHORN SANDSTONE

It is recognized that the Shedhorn Sandstone is the 

lateral equivalent of other members of the Phosphoria 

rock complex. Cressman and Swanson (1964, p. 286) 

have documented this interfingering in detail. They indicate that the lower part of the formation is the lateral 

equivalent of the Rex Chert Member of the Phosphoria 

Formation and the Franson Member of the Park City 

Formation and that the upper member is the lateral 

equivalent of the Tosi Chert Member of the Phosphoria 

Formation. The age of the Shedhorn can be interpreted 

from the age assigned to the fauna in the more f ossilif erous intertonguing members. For this reason and because 

the faunas had not been studied at that time, Williams 

(1959, p. 36) wrote no preliminary statement on the age 

of this formation.

The known Shedhorn fauna is disappointingly small. 

The Wyoming collections from the lower part of the 

Shedhorn, for the most part, contain either a few brachiopods which occur in rocks similar to those of the
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 627

Franson Member or poorly preserved mollusks suggestive of the molluscan fauna from the Franson.

The faunal evidence for the age of the upper part of 

the Shedhorn is somewhat better but allows several 

other interpretations to be made. The northernmost 

and northeasternmost collections in Montana contain 

a limited molluscan fauna, closely related to a particular rock facies and possibly transgressing the limited 

time span between the Rex and Tosi Members. Nevertheless, supplementary evidence of an older age for 

at least some of the upper Shedhorn is shown by the 

presence of abundant BelleropJion deftectus H. Chronic 

and some Euphemitopsis subpapillosus (White) at Cinnabar Mountain (1363) and a single specimen, possibly E. paucinodosus Yochelson, at Big Timber (M). A 

collection of silicified fossils from Cedar Creek (1256), 

although nominally from the Retort Phosphatic Shale 

Member, is almost certainly from the Shedhorn Sandstone because it is in the sandstone matrix typical of 

that unit. This collection contains BelleropJwn deftectus H. Chronic, Euphemites crenulatus Yochelson, and 

KnigJitites (Retispira) eximia Yochelson, characteristic of the upper part of the Leonard and lower part 

of the Word Formations in western Texas. Permophorus and Plagioglypta from this locality are conspecific 

with specimens from the Franson at Big Sheep Canyon 

(1224).

Locally, there are mollusks from the upper part of 

the Shedhorn Sandstone which are found in the upper 

Leonard-lower Word sequence. It follows that there 

are at least four possible factors which may influence 

interpretation of the age of the Shedhorn Sandstone: 

(1) There has been confusion in identifying the upper 

and lower units in the field; (2) the upper part of the 

Shedhorn Sandstone may be older in sections peripheral to the type section than it is in the type section, 

(3) the Rex and Tosi Chert Members, the presumed 

temporal equivalents of the Shedhorn, are of nearly 

the same age, and (4) these mollusks have a longer 

range in Montana than in the area from which they 

were first described.

Considering the detailed field studies made, it is illogical that confusion in identifying field units existed. It 

is also illogical that the fourth factor would influence 

age interpretation from what little is known of the 

mollusks elsewhere in the Permian of the United States. 

Both the other factors may have influence. Certainly 

this faunal evidence seems to support the contention 

based on examination of the brachiopods that the Franson and Ervay Members of the Park City are little different in age. Further study of the pelecypods in the 

Shedhorn Sandstone may eventually provide more information bearing on its age and correlation.

Cressman and Swanson (1964, p. 382-383) suggest 

that to the east of the Madison River in Montana there 

may be an unconformity at the top of the Permian. The 

Shedhorn Sandstone at Cinnabar Mountain could then 

be older than the upper part of the Shedhorn to the 

west, a theory being in complete agreement with the 

limited faunal evidence.

SUMMARY OF AGE RELATIONSHIPS

The material presented in this paper can better be 

considered a survey of the fauna rather than a study 

of the fauna. Careful redescriptions of the species and 

comparison with related species remain to be made. 

Table 4 is an attempt to indicate, after the minor stratigraphic inaccuracies indicated in table 3 have been corrected, the occurrence of the identified or identifiable 

species within the rocks studied to which further study 

should be directed.

TABLE 4. StratigrapMc occurrence of brachiopods and mollusks 

in the Phosphoria rock complex

Taxon

Orbictdoidea (Roemerella) 

utahensis (Meek).. 

cf. 0. (0.) missouriensis

Wellerella cf. W. osagensis

Neospirifer pseudocameratus 

(Girty). -.

Sphenalosia smedleyi Muirwood

Kochiproductus cf. K. longus 

(Meek)

Bathymyonia nevadensis (Meek). 

Antiquatonia cf. A. sulcatus

Rugatia, occidentalis (Newberry).

Muirwoodia multistriatus 

£Meek)

Phynchopora cf. /?. taylori Girty _ 

Spiriferina pulchra Meek 

cf. S. kentuckensis

Hustedia phosphoriensis C. 

Branson _ _ 

StratigrapMc unit

Grandeur Membe

X 

X

X

 -

X

X 

X

Lower chertMember

....

 -

Meade Pekhosphatic Shale y 

A Member

X

X 

X

X

 -

X

X

X

Franson Member

X 

X

X

X

X

X

X

X

X 

X

X 

X

X

Rex ChertMember X 

 -

X

X

X

1 Lower ofShedhorn member

1 Formation

X

X

X

 -

1 Upper Shedhorn ofmember 

1 Formation

 -

X

X

 -

X

Phosphatic Shale Retort

Member

X 

X

 

 

"Upper Franson" Member

 -

X

 

X

I Ervay Cabonate Rock

Member I 

 -

X

X

X

X

X

X 

X

X

Tosi Chert Member

X

X

X

X

 

X 

X
628 GEOLOGY OF PERMIAN BOCKS IN THE WESTERN PHOSPHATE FIELD

TABLE 4. Stratigraphic occurrence of brachiopods and mollusks 

in the Phosphoria rock complex Continued

Taxon

Nuculopsis poposiensis C.

obesa (White)-.. 

Acanthopecten alatus C.

Aviculopecten cf. A. kaibabensis 

I^ewell

cf. A. phosphaticus Girty.---

cf. A. alternatus C. Branson,

Streblochondria? guadalupensis 

Girty--.--- 

cf. S. montpelierensis 

(Girty) 

Myalina (Myalindla) meeki

Pseudopermophorus annettae

Eoastarte subcircularis Ciriacks. _

Sanguinolites elongatus Ciriacks . 

cf. S. carbonaria (Girty) ..... 

Schizodus subovatus Ciriacks. __

Costatoria sexradiata (C.

Castianella sexradiata (C.

Edmondia cf. E. gibbosa Swallow.

Astartetta subquadrata Girty- ....

Plagioglypta canna (White) .... 

Euphemites crenulatus

Euphemttopsis cf. E, paucinoBetterophon deflecttis H. Chronic.

Knightltes (Retispira) eximia

Olabrocingulum coronatum H.

Orthonema cf. 0. socorrcense 

Qlrty. ........................

Stratigraphic unit

Member Grandeur 

X

X

y

X

X 

X

X

X

X

X 

X 

X

X

X 

X

X

X

X

X

Lower Member chert 

X

Meade Pekhosphatic Shalo 

Member

X

X

X 

X

X

X

X

X

X

X

X

X

X

X

V

X

X

X

X

Franson Member

X 

X

X

X

X

X

X

X

X

X

X

X

X

Rex Chert Member

....

X

X

X

X

1 LowerShedhorn memberof 

1 Formation

X

X

X

X 

X

X

X

Shedhorn Upper member ofv 

A Formation

X

X

X

X

X

X

X

X

X

X

Phosphatic Shale Retortv 

A Member

v

X

X

X

$-4

1 

i

~a

1 

! 

&

X

X

Carbonate RockErvay 

Member

X

X 

X

X

X

X

X

X

Tosi Chert Member

X 

X 

X

X

X

The fossil group most urgently in need of re-collection 

is the pelecypods. They constitute almost half of the 

species which may eventually be useful for correlation

of the members. Unfortunately more than one-fourth 

of these species are known from only a few specimens. 

Most of the rest come from widely scattered localities. 

Many of the other mollusks also are not well represented. About half of the few gastropods and cephalopods identified are represented by rare specimens from 

only one locality. The specific identity of some of the 

brachiopods may eventually need to be reexamined. 

Studies in progress on the better preserved and more 

abundant faunas of western Texas will, when completed, aid in identification and interpretation of the 

forms listed.

The vertebrate fragments also remain to be evaluated. Some work has been done on fish material, but 

only preliminary identifications of the Wyoming collections are available. These are given in table 5. These 

studies and reinterpretation of earlier investigations in 

the light of new Stratigraphic data may eventually 

make the fish fragments more useful as Stratigraphic 

indicators.

Detailed field studies have clearly demonstrated the 

intertonguing of the various rock units within the 

Phosphoria rock complex. Such a Stratigraphic relationship implies that at least part of every lithologic 

unit must transgress time. Considering that the area 

of outcrop is measured in thousands of square miles, 

the age of a member at one particular place may have 

little bearing on its age in another place. Keliable guide 

fossils seem to be absent from some of the lithic units 

and rare in the others. As a result of this combination 

of factors, there has been a tendency, best exemplified 

in the Permian correlation chart (Dunbar, 1960), to 

equate the Phosphoria rock complex with most of midPermian time.

The writer feels that the Phosphoria rock complex 

may not occupy as long a time span as has been suggested. The available evidence suggests that all the rocks 

may have been deposited during the time represented 

by the Leonard and Word Formations in western Texas. 

The Grandeur Member seems to be equivalent to the 

Leonard Formation. The Meade Peak and Ketort Members may be as old as latest Leonard or earliest Word 

and may be as young as latest Word. The Franson Member may occupy this same time span. The Ervay Member may be either of late Word or post-Word equivalence ; if the latter correlation is preferred, there is still 

no paleontologic evidence that an extensive interval of 

post-Word time is represented by that member. The 

Shedhorn Sandstone seems to be of late Leonard-Word 

equivalence, but this may be because the known fauna 

consists mostly of mollusks. In overall aspect the mollusks seem to indicate a slightly older correlation than 

do the brachiopods. Pending further evidence, this ap-
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 629

TABLE 5 Distribution and preliminary identification of fish remains in Wyoming 

[Symbols for stratigraphic units defined on p. 576. Compiled by D. H. Dunkle and D. H. Van Sickle]

Collection

1ORA1

12563 

12567 

12568 

12569 

12572 

12573 ___ 

13314 __

13315 _ ... 

13321 

13322 

10934 

10933-. ___ . _ . 

10932- _ ... 

10925 

10970 

12436 -

12471 

19735 

19747 

13301 

13331 

13334 

13342. ___ _ ..

13344 

12310. __ 

12311 _ 

12147- ___

12148 

12138 

12660 

12665 ___ . __ 

12686 _____ .

12667 __

12575 

12581 __

18598 

12554 

18597 

12555 

12557 ___ 

12559 

12548. ______ - _

12549 __

18593. ___ 

18C99- _ 

12126 . _ . _ ...

12128 __ .

12129- _

12131 ___

12222 __ ... __ . ....

12224 ___ _ ...

12226 __ ....

12117 

12544 

12545 .

12118 

12537 _

12121 

12123 .........

12214 

12215 

12216 

12217 

12218 

12220 

12202 ........

18591..... ...........

12205 .......... 

12206 

12207 

12208 

12209 ........

12211 .

12212 . 

12238 .

12243 

12245... .............

12246 .........

Section

Name

- do..... ... .... .... 

. do ... ....... 

 .do . .......

 ..do ... .... .... -

 do 

 do. ... ..... ......

--...do-.------. 

"Wlioat ProoV

... -do..-. 

 do ... 

 do. .... ... 

do . . .

 do .. 

 do _ 

do . . _ ___

 do ... ... ... .... . 

do

 do .

..... do ..... ... ... ... 

-.-do . _ .

 do ...

 do __ ... ... __ 

 do 

do

 do 

 do 

 do..___ 

 do _. 

Eed Creek... _

.....do- ... 

 do - 

 do 

 do 

 do ... 

Flat Creek _ __ _ 

 do. ..... ... 

 do . __ ... __ ....

 do 

 -do..... ... 

 do 

 do 

.... -do...... . . ...

 do....... ...

.... .do .......... .... ... ... ...

 do 

 do ........ ...... .......... .... ....

.. do .... .......

 do .. ..... .... ...... ........

 do .. . .. ..... ... ...

.... .do ......... .... ............

 .do - . . .

 do . ... ...... .. .....

 do ....... ........ 

 do- ...... .

 ..do .... ......... ........ ......

.... .do ...... ......... ......... ...... .... ..

 do ....... .......... 

No.

1346

1346 

1346 

1346 

1346 

1346 

1346 

1378 

1878 

1378 

1378 

1289 -

1289 

1289 

1289 

1289 _ 

1205 

1201.. 

1379 

1379. 

1380 

1380 

1331 _ 

133U1332 

1332. 

1324. 

1325. 

1325 

1325 

1325 

1370 

1370 

1360

1360 

1360 

1360. 

1360. _

1360 __ 

1368 

1368 

1327 

1326 _ ....

1326 

1326... _ .

1326 .......

13335- _ .

13335 

13335 

1323 

1323 

1323 

1323 

1323 ..

1323 

1323 

1334 

1334 ...

1334 

1334. 

1334 

1334 

1333 

1333 

1333 .

1333 

1333 

1333 

1333 

1333. 

1333 

1336. 

1336 

1336 

1336 

Strattgraphicunit

Q

M 

M 

M 

M 

M 

M 

M 

LC 

Q 

M 

M 

M 

M 

M 

M 

M 

M 

M 

F 

E 

M 

M 

M 

M 

LS 

M 

M 

M 

M 

M 

LS 

LS 

Et 

US 

M 

Et 

G 

LS 

LS 

LS 

Et 

LS 

LS 

LS 

LS 

LS 

M 

M 

F 

F 

M 

Et 

US 

Et 

Et 

LS 

LS 

Rt 

Rt 

Rt 

Rt 

Et 

Et 

Rt 

Et 

US 

LS 

M 

F 

F 

F 

Rt 

Rt 

US 

E 

F 

Rt 

Et 

E

Placodermi

Placoid scales

 .

X

----- 

Chondrichthyes

Cladodus sp.

X

X

X

Ctenocanthus sp.

v

X

X

Dkrenodis (Pristicladodus) sp.

--

X

Dolophonodus sp.

X

Helicoprion sp.

X

--

d 

1

X

--

V

V

X 

X

X

Dettodus sp.

X

X

Crassidonta sp.

X

--

Janassa sp.

--

-

Bradyodont teeth undet.

X

X

--

Cochliodont teeth undet.

X

-

--

Hamatus sp.

X

--

X

Ancistriodus sp.

X

v

--

Osteichthyes

Rhadinichthid scales

--

X

v

Elonichthid scales

X

--

--

Acrolepid scales

X

X

X

X

--

Platysomid scales

--

--

Palaeoniscoid fragments

X

X

X

X

X

X

X

X

--

"Fairy collar buttons"

X

X

X

X

X

X

X

X

X

X

X

v

X

X

X

X 

X 

X

X

X

X

Miscellaneous

Scales undet.

X

X

X

X

X

X

X

X

X

X

X

-

Bone undet.

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X 

X

Fin-ray undet.

X

--

Spines undet.

X

X

--

Calcined cartilage indet. 

Teeth undet.

X

- X

X

- X

X-

- X
630 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

TABLE 5 Distribution and preliminary identification of fish remains in Wyoming Continued

Collection

12179-..-.-..-.....

12180... ............ .

12181- .

12193-... - 

191 Qf\

12200 ............

191 KA

12156 

12157-- . -.

12169 ..........

12163 

12J fifi 

12170. .

12171 .............

12251 

12252 

12253 

12254....-- . .

12229 

12230-.- -.--.

12235 . -.

Section

Name

.....do- .............. ......................

-...do 

.....do-.-....... .. ...............

.do 

 ..do . . . ..........

 . do... ............... - .. .- 

 do - .- - --.. .

.....do 

. do-. . 

 .do... 

..... do ._ 

.... .do.. .. ...

... -do-..... 

.... .do 

.... .do... ................. ..................

No.

1329 

1329 -..

1329. 

1 39Q

1 39Q

1329 , 

1 V>f\

1325- 

1325 

1325 

1325.... 

1325......

1325 

1328.......

J328 ....

1328 .

1328 

1330 

1330. 

1330 

Stratlgraphic unit

LS 

LS 

LS 

Rt 

TO 

E 

E 

M 

M 

LS 

F 

Rt 

Rt 

Rt 

E 

Q 

LO 

M 

M 

Rt 

Rt 

E

Placodermi

1 

5

£

Chondrichthyes

c

-§ 

1

5

c

V.

Z 

|

G

Dicrenodis (Pristicladodus) sp.

Dolophonodus sp.

X

Helicoprion sp.

e

^

§

v

X

Dettodus sp.

Crassidonta sp.

Janassa sp.

X

Bradyodont teeth undet. Cochliodont teethundet.

Hamatus sp.

Osteichthyes

c

^

£

.1 

s

^

Rhadinichthid scales

Elonichthid scales

X

Acrolepid scales

X

X

Platysomid scales

-

-

Palaeoniscoid fragments

X

X

X

"Fairy collar buttons"

X

X

X

X

X

X

X

X

X

X

X 

X

xxxxx

Miscellaneous

4J

<u 'C

IOD

~

-

-

Bone undet.

X

X

X

X

X

X 

X

-

X

Fin-ray undet.

"-

-

-

Spines undet.

X

--

-

\ Calcified cartilage indet. 

\ Teeth undet.

parent anomaly cannot be resolved and the reader is 

offered two slightly divergent age determinations.

GEOGRAPHIC DISTRIBUTION OF COLLECTIONS

In most of the sections, a substantial number of the 

collections warrant brief comment. By and large, these 

comments are designed to compare or contrast collections from each stratigraphic unit within the four state 

area, even though there is reason to question or even 

to change some preliminary age identifications at some 

localities. Nevertheless, the information has some utility 

and is of most interest to those actively working in the 

areas discussed.

The fossil collecting at most localities was adequate, 

at least for obtaining the commoner fossils, and the fact 

that so many collections having the same matrix contain similar faunas is proof of this. Geographic sampling is far from adequate to uncover any but the most 

obvious regional variations. More than 1,500 collections 

distributed among 122 localities are available, but it 

should be borne in mind that the area sampled is larger 

than England and southern Scotland combined. However, the sampling pattern is exceedingly uneven; more 

than one-fourth of the localities and more than onethird of all the collections are from a comparatively 

small part of southeastern Idaho where, when detailed 

stratigraphic work is completed, it may be possible to 

recognize the more subtle geographic variations of the

fauna. For the rest of the area, the paucity of collections nullified all attempts at analysis of stratigraphic 

units smaller than members.

The stratigraphic distribution of the collections is 

also extremely uneven. More than one-half of all the 

collections are from the Meade Peak Member. The remaining five members of the Phosphoria Formation 

are represented by less than 15 percent of the collections almost two-thirds of these collections are from 

the Eetort Member. The collections from the Park City 

Formation and the supposed Park City Formation 

form about 20 percent of the total, of which nearly 

half are from the Franson Member. Almost as many 

are from the Grandeur Member and beds thought to 

be older than the Grandeur. Only about 10 percent of 

the Park City collections are from the Ervay Member 

and its equivalents. The Shedhorn Sandstone is inadequately represented because less than 3 percent of the 

collections are from that formation.

GRANDEUR MEMBEB OF PARK CITY FORMATION

The available evidence indicates that the rocks below 

the phosphatic shale and above recognized Pennsylvanian age beds are not all of the same age. Nevertheless, except for one collection from the Tensleep 

Sandstone, which contained undoubted Pennsylvania!! 

fossils, all pre-Meade Peak collections are considered
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 631

here. Collections from this interval are designated on the 

faunal lists as G, G? or W?.

IDAHO

The pre-Meade Peak rocks in Idaho are represented 

by 33 collections from 22 sections. Two of the collections contained no fossils and two others could not be 

located for study. As detailed columnar sections are not 

available for most of the localities, it is difficult to know 

quite how to designate these collections. Grandeur has 

been applied in a few localities where the faunal evidence clearly suggests it. Grandeur (?) has been used 

both for those that may be Grandeur, but for which 

the faunal evidence is inconclusive, and for those that 

may be from younger beds but were identified in the 

field as being from the Wells Formation. Many of these 

collections were obtained before differentiation of the 

Grandeur Member was considered. Wells(?) has been 

used for the remaining collections which show no clearcut faunal evidence for their age.

The westernmost collections at Mud Spring (1351) 

(12635, 12636) are the most perplexing. Both contain 

leiorhynchoid brachiopods and a few mollusks, particularly nuculoid pelecypods. The lowest also contains 

Babylonites, which in other outcrops characteristically 

occurs above the Grandeur. Although the collections remotely resemble the mollusk bed at Cephalopod Gulch 

(C) (18890) in Utah, they lack the abundant Orthonema. The collection is from the upper part of a carbonate sequence which, in the stratigraphic nomenclature 

scheme employed, is assigned to the Grandeur Member 

(E. R. Cressman, written commun., 1961). In northeastern Nevada, Bdbylonites does occur in the upper 

part of the Grandeur Member.

Other collections are clearly anomalous, though they 

are still carried here as Wells (?) Formation. At Lone 

Pine Spring (1298) (11518) the collection is from a 

chert containing only sponge spicules. Although this is 

the only occurrence of a spiculite in pre-Meade Peak 

rocks, there is no evidence of structural complications. 

T. M. Cheney has observed spiculites in the Grandeur 

Member in northeastern Nevada (E. R. Cressman, written commun., 1961).

The collection from the divide between Trail and 

Wood Canyons (K) (12260) contains poorly preserved 

ramose bryozoans and a coquina of phricodothyridlike 

brachiopod shells. The collection is not characteristic 

of any member of the Phosphoria Formation or its 

equivalents.

Some of the remaining collections fall into a more 

meaningful pattern. At Hot Spring (1317) (19531) 

and in the lowest part of West Dairy (1208) (9930), 

poorly preserved fossils are suggestive of the "dictyo269-09 2 68 5

clostid beds" in Utah. A small fauna particularly characterized by a linoproductid is found above these fossils 

at West Dairy and at other scattered localities nearby. 

This linoproductid occurs at Grizzly Creek (N) (19533) 

and Rocky Canyon (1304) (11697) to the northwest. At 

none of these localities are the collections large or particularly well preserved. In the same general area a few 

collections contain crinoid remains either exclusively 

or predominately.

At Pole Canyon (1303) (11564) and Snowdrift 

Mountain (1372) (12582) only orbiculoid brachiopods 

are found. These are among the easternmost of the sections; they have approximately the same geographic 

relationship to sections yielding only crinoid stems as 

was observed to the southeast in central southwestern 

Wyoming.

At Bear Creek (39) (12531) a poorly preserved 

pleurophorid pelecypod fauna is like that in southwestern Wyoming, whereas to the north at Fall Creek 

(37) (12289) only a few fish scales have been obtained.

MONTANA

Of 24 collections from the pre-Meade Peak rocks of 

Montana, one was unfossiliferous and discarded. These 

samples are distributed among eight sections, of which 

almost one-third come from Big Sheep Canyon (1224). 

The distribution of the collections is not satisfactory for 

indicating any possible regional variations.

The lowest collection at Hogback Mountain (1299)

(11673) contains, among other noncharacteristic fossils, 

one of the two trilobites found in all the collections 

studied. This collection is immediately overlain by several small collections containing dictyoclostid brachiopods; one collection also contains a solitary coral

(11674). The dictyoclostid brachiopods are not particularly like those from Utah and southern Idaho, although 

their poor preservation prevents close comparison.

Similar faunas showing a little more variety occur at 

Big Sheep Canyon. Relatively high in this section oval 

crinoid columnals, probably Platycrinites^ and a sponge 

are also found. These two fossils are unique in the Grandeur collections. A linoproductid, also unique to the 

Grandeur, has been identified at this locality.

The remaining collections provide few interesting 

fossils. At Wadhams Spring (1246) (10837) mostly 

crinoid stems occur. At Sheep Creek (1234) (10807- 

10809) ramose bryozoans occur and are quite different 

from the fenestrate bryozoans in the Grandeur to the 

south in the North Wooley Range of Idaho. The single 

collection from Warm Springs Creek (11681) (1300) 

contains only Derbyia. At Sliderock Mountain (1301) 

(11671) there are a few poorly preserved phricodothyrid brachiopods like those from the divide between
632 GEOLOGY OF PERMIAN BOCKS IN THE WESTERN PHOSPHATE FIELD

Trail and Wood Canyons (K) in Idaho, and at Little 

Water Canyon (1341) (12297) there is one indeterminate spiriferoid brachiopod and a few fish scales. 

Poorly preserved pelecypods occur at Sawtooth Mountain (1241) and at Crooked Creek (1296), and a few 

Plagioglypta also occur at the latter section.

UTAH

In Utah, 46 collections are available from 13 measured 

sections of the Grandeur. Two of these collections were 

made to obtain additional material from previously 

known localities. Except for the Strawberry Valley 

(13Y1) and Fort Douglas (1350) localities, there are 

few collections from any one section.

Along the north flank of the Uinta Mountains at 

Horseshoe Canyon (1339) (19403) and Bennett Eanch 

(G) (19402), large mollusks, particularly pectenoid 

pelecypods and SeTiizodus are predominate. Scliizodus 

is abundant at Franson Canyon (134Y) (12489,12490). 

A few pelecypods also occur in the small collection from 

Brazer Canyon (1203) (19414).

In marked contrast, the fauna from Mill Creek (D) 

(1Y657) is a brachiopod fauna, large dictyoclostid productoids being predominate. This same fauna occurs low 

in the section at Fort Douglas (1350) (12515, 12516) 

and at Cephalopod Gulch (C) (180Y6). Large indeterminate productoids were obtained low in the section at 

Devils Slide (1345) (19411) and Dry Canyon (1229) 

(10790). A few characteristic dictyoclostids were collected in Horseshoe Canyon from the beds yielding 

abundant pelecypods (19403).

Above these "dictyoclostid beds" at Fort Douglas, a 

series of small collections contain orbiculoids, poorly 

preserved pelecypods and gastropods, and a few Lingula. OrMculoidea is found as the only fossil in four collections from Devils Slide and in one collection from 

Horseshoe Canyon at the top of the Grandeur. At 

Strawberry Valley, a series of small collections are 

characterized by Orbicvloidea, except for one collection 

(12684) which contains abundant euphemitid gastropods and Plagioglypta.

The remaining collections contribute little. A single 

collection from Warnhodes Canyon (12YO) (10603) 

contains only crinoid stems. One from the Eight Fork 

of Hobble Creek (12Y1) (16054) contains a few small 

brachiopods which perhaps could be related to "dictyoclostid beds" to the north. A small collection from North 

Crawford (1292) (10966) is anomalous because of its 

small Clionetes content.

In Cephalopod Gulch immediately above the "dictyoclostid beds," a thin bed (18890) has yielded exceedingly 

abundant Orthonema and some other mollusks. Because

the fossils are silicified, it is possible to dissolve the 

matrix so that well-preserved fossils can be obtained. 

This particular locality accounts for about half of the 

total variety of forms reported from the Grandeur.

WYOMING

The Grandeur Member is poorly represented by only 

21 collections from 8 localities. The Grandeur collections 

fall reasonably well into two groups, those on the east 

side of the Wind Eiver Mountains and those in western 

Wyoming. The single collection from Basin Creek 

(1381) (13303) is atypical of both Grandeur and lower 

chert members because it contains only crinoid stems.

The Grandeur collections from Bull Lake (1328) contain abundant simple neritaceanlike gastropods, some 

large pelecypods, and a few fenestrate bryozoans. Those 

from Dinwoody Lakes (1325) contain Hystrlculina, 

varied small brachiopods, and f enestrate bryozoans; 

they also contain one of the two trilobites found. Taken 

together, these six collections differ significantly from 

other Grandeur collections.

The western collections may be considered as a pelecypod fauna having subordinate inarticulate brachiopods and occasional small fish teeth. These fish teeth 

characterize the basal and shoreward beds. The mollusk 

fauna contains many Schizodus, but is best characterized by pleurophorid pelecypods. The orbiculoids show 

no clear pattern of distribution, except that in sections 

where they occur, mollusk-bearing beds overlie them.

Far to the north at Forellen Peak (4), the fish remains are resistant small teeth and bone fragments. 

They are in a sandstone and strongly suggest a nearbeach deposit. Further south, the pelecypods and inarticulate brachiopods lie to the east of a collection of 

crinoid stems at Basin Creek (1381) and Clionetes in 

northeastern Utah.

LOWER CHERT MEMBER OF PHOSPHORIA 

FORMATION

The lower chert member of the Phosphoria Formation is presently recognized only in the central part of 

western Wyoming. Although it is theoretically possible 

that a few collections from southwestern Wyoming and 

southwestern Idaho may be referred to this unit when 

a definitive stratigraphic study is completed, nothing in 

the lithology or f aunal content of collections from that 

area suggests this possibility. The limited fauna observed is similar to that in the Grandeur Member of the 

Park City Formation in this part of Wyoming.

One collection was made from each of five sections 

of the member. These collections are indicated on the 

f aunal distribution charts by the symbol LC; one collection was discarded because it was unfossiliferous.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 633

The easternmost lower chert collection at Bull Lake 

(82) (12252) contains small fish teeth. Collections from 

Hoback (57) (12137) and Fontenelle Creek (108) 

(13328) contain only orbiculoid brachiopods. The Fontenelle Creek section is overlain by mollusk-bearing 

beds. The southwesternmost collection at Wheat Creek 

(110) (13314) contains Schizodus and a few scaphopods; it is similar in facies to the Grandeur Member 

along the north side of the Uinta Mountains.

MEADE PEAK PHOSPHATIC SHALE MEMBER OF 

PHOSPHORIA FORMATION

As noted, collections from the Meade Peak Phosphatic 

Shale Member are more abundant than those from any 

other unit. The collections are indicated on the f aunal 

distribution charts by the symbol M.

IDAHO

Most of the commercial deposits of phosphate are located in southeastern Idaho, and, accordingly, the most 

detailed work on the Phosphoria project was done in 

this region. A total of 584 fossil collections more than 

one-third of the number available were made from 36 

sections. Eighteen additional collections were found to 

be unf ossilif erous and were discarded.

Collections from four sections that are outside of the 

area bounded on the west by long 112° W. and on the 

north by lat. 43° N. For convenience these can be discussed first. The collections at Mud Spring (1351) further to the west show a diversity of articulate brachiopods similar to that found near the Idaho-Wyoming 

boundary. Oancrinella and Polidevcia are absent. The 

Bear Creek (37) collections to the north and the Fall 

Creek (39) collections to the northwest are most like 

those from nearby Teton Pass (49), Wyo., in containing fish remains and orbiculoid brachiopods. They, however, are augmented by squid tentacle hooks (onychites), which are also seen in western Wyoming at Flat 

Creek (50) and Buck Creek (60).

The Wolverine Canyon section (1322) to the west 

differs from the others mentioned in that it has yielded 

fish remains, Pseudogastrioceras, Orurithyris, Chonetes, 

and Oancrinella as the major f aunal elements.

The majority of the sections in Idaho resemble the 

Wolverine Canyon section. Most contain the five f aunal 

elements mentioned above and Orbiculoidea,^ Leiorhynchus, Bdbylonites, and Polidevcia, Nine sections contain 

Lingula; eleven sections contain tentacle hooks of 

squids. Both these fossils are scattered throughout the 

outcrop area but seem to be almost mutually exclusive 

at individual sections.

The other characteristic fossils show almost no geographic pattern. Although relative proportions of the

alous collections, the faunal distribution is comparable to that in the Wyoming Meade Peak collections 

cal absences of one or another of these forms can be 

readily interpreted in terms of local variation in preservation and collection. If there is any geographic arrangement of the fossils within this area, it is by no 

means obvious.

MONTANA

There are few collections from the Meade Peak in 

Montana as might be anticipated from the pronounced 

northward thinning of the member. Only 14 collections 

distributed among 10 sections in southwestern Montana 

are available.

For the most part the collections require little comment as they contain only fish remains. At Dalys Spur 

(1222) orbiculoids occur with fish; at Crooked Creek 

(1296) (11692) they occur below the fish remains. The 

one collection from Alpine Creek (1307) (11685) contains only a few fragments of orbiculoids.

The higher collection (10839) from Wadhams Spring 

(1246) differs markedly from all the other Meade Peak 

collections in Montana in containing abundant squid 

tentacle hooks. The lower collection at this section 

(10838) and the lower collection at Sawtooth Mountain 

(1241) (10852) both contain indeterminate mollusks 

in a cherty limestone matrix. Except for these two anomalous collections, the faunal distribution is comparable to that in the Wyoming Meade Peak collections 

from north of the 43d parallel.

UTAH

In Utah, there are 2,y2 times as many fossil collections 

available from the Meade Peak Member as from all other stratigraphic units of the Phosphoria rock complex 

combined. The 257 collections, 8 which have been discarded, were taken from 18 localities. Because the fossils available seem to indicate the presence of several 

calcareous layers within the shale, it is impossible to 

consider the fossils in terms of a simple transgressionregression cycle. The collections can be divided into three 

geographic assemblages.

First, from the Uinta Mountains area, 56 collections 

are available from 8 localities. The collections are characterized by the abundant steinkerns of a small nuculoid 

pelecypod. A smaller number of collections contain 

orbiculoid brachiopods, or nuculoids and orbiculoids. 

There are also a few scattered fish remains. Only two 

collections contain other faunal elements: One of these 

from Blind Stream (F) (10804) contains an indeterminate dictyoclostid brachiopod fauna which might actually represent a feather edge of the Grandeur Member; the other collection (10803), underlying the
634 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

dictyoclostid collection at Blind Stream, contains 

Lingula.

Second, in the northern Utah area, 72 collections from 

5 sections are available. There is considerably more 

f aunal diversity here than elsewhere in the State; nuculoid pelecypods are virtually lacking and few orbiculoid brachiopods have been collected. Most of the 

orbiculoids are in the upper half of the section rather 

than distributed throughout.

Probably the most abundant single form in the area 

is Chonetes, followed by Leiorhynchus, Streblochondria, and Crurittiyris, in order of diminishing abundance. Bdbylonites, Pseudogastrioceras, and sporadic 

specimens of a few other genera are also present.

Third, in the Wasatch front area near Salt Lake 

City, 121 collections are available from 5 localities. In 

Wanrhodes Canyon (1270) and the Eight Fork of Hobble Creek (1271), it is possible to discern a pattern of 

vertical distribution. At the base of the section, beds 

contain nuculoid pelecypods and a few orbiculoid 

brachiopods not unlike those from the Uinta Mountains 

area. Above these beds are a group of collections containing Bdbylonites and Pseudogastrioceras. Still 

higher are a few more nuculoid pelecypods, and next is 

a large group of collections containing virtually nothing but Pseudogastrioceras. Immediately above, at Hobble Creek, a zone (10686-10688) contains scattered crinoid debris; more cephalopods are found somewhat 

higher in the section. A few crinoid stems also occur in 

the Wanrhodes Canyon section, but they are relatively 

higher in the section than those at the Hobble Creek. 

The collections above the crinoid stems in this section 

contain predominantly nuculoid pelecypods.

The Strawberry Valley (1371) and Fort Douglas 

(1350) sections contain fewer collections. In each there 

are a few collections in the approximate position of the 

lower cephalopod bed of the other two sections. The beds 

in these two sections, however, primarily contain 

Bdbylonites and few other fossils. Higher beds contain 

too few collections to form a clear pattern. The fifth 

section at the Geneva Steel Company Pit (E) contains 

only fish remains.

WYOMING

Not only are there less than half the number of collections from the Meade Peak Member in Wyoming 

that there are in Utah 111 in all but they are somewhat more widely distributed. Collections have been 

obtained from 19 sections, and almost half of them are 

from 3 sections. Ten other collections, including the only 

Meade Peak collection from Steer Creek, were unfossiliferous and have been discarded.

The collections may arbitrarily be broken into two 

groups, those north and those south of the 43d parallel.

North of this line seven of eight localities contain fish 

remains, and six of eight contain orbiculoid brachiopods. Of considerable interest is the occurrence of squid 

tentacle hooks at Flat Creek (50) and Buck Creek (60). 

The only other f aunal elements are a few indeterminate 

productoid brachiopods at Din woody Lakes (75) and 

Polidevcia at Buck Creek (60). These collections north 

of the 43d parallel most closely resemble those from the 

Meade Peak Member in southwestern Montana.

Collections from four sections south of the 43d 

parallel are similar to most of those north of this line. 

Deadline Eidge (107) contains fish remains and a few 

Lingula. Fontenelle Creek (108) and Basin Creek 

(1381) have fish and orbiculoid brachiopods. At Poison 

Creek (1331) the fish remains and orbiculoids together 

with small nuculoid pelecypods resemble an assemblage 

common in the Uinta Mountains more closely than the 

Meade Peak assemblage from nearby localities. Wheat 

Creek (110) also contains fish and orbiculoids but in 

addition has yielded a few Worthenial Its overall aspect is most similar to the Meade Peak from Laketown 

Canyon in northeastern Utah. Worthenia? also occurs 

at the North Fork of Pine Creek (1204) and Cumberland (147).

Fossils from the remaining six sections in Wyoming 

are strikingly different from those just discussed. Although most sections contain both fish remains and orbiculoid brachiopods, other members of certain fauna 

are common. At Layland Canyon (1202) and Coal Canyon (1201) Chonetes, Grwrithyris^ LeiorhyncJws, Stre- 

~blochondria, Pseudogastrioceras, and Bdbylonites are 

common to abundant. At the North Fork of Pine Creek 

(1204), Oancrinella also occurs. Curiously enough, this 

genus is missing at Cokeville (1289) to the south, although other genera are there in profusion. It is present 

at Cumberland (147), though the fauna is less abundant. In general, these varied faunas lie to the west of 

collections containing orbiculoid brachiopods and fish 

remains and show close similarity to the Meade Peak 

collections from southeastern Idaho.

FKAisrsoisr MEMBEK OF PAKK CITY FORMATION

The Franson Member ranks second to the Meade Peak 

Member in number of collections; however, the number 

of sections used and their distribution is comparable 

with that from the Meade Peak Member in Montana, 

Utah, and Wyoming. Few collections are available from 

the southeastern Idaho region where the Franson interfingers with and is replaced by the Eex Chert Member 

of the Phosphoria Formation. Franson collections are 

designated by the symbol F on the faunal distribution 

charts.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 635

IDAHO

Throughout many of the sections in Idaho, the Franson is not recognized because it is replaced laterally in 

part by the Eex Chert Member. The Franson has only 

been collected at the Fall Creek (39) section, where five 

collections were obtained, one of which is a re-collection. 

In the lowest part of the section (12294, 18594) are 

abundant Neospimfer, some SpJienosteges, and common 

stenoporoid bryozoans. The succeeding collection contains Neospirifer but also has many orbiculoid 

brachiopods and a few nuculoid pelecypods and 

bellerophontaceans.

All these collections lie below but near the line of 

maximum regression of the Franson (Sheldon, 1963 

p. 124). Above the line of maximum regression, one 

collection fairly high in the section contains abundant 

large pelecypods (18595). Another collection, stratigrahically higher, contains only a single Composita 

(12296).

MONTANA

The Franson Member is represented in the collections from Montana by only 34 collections from nine 

sections; two collections are re-collections. Three sections in extreme southwestern Montana have yielded 

more than half of the collections. North Big Hole 

Canyon (1358) (18584) and Hogback Mountain (1299) 

(11677), among the less fossiliferous sections, contain 

only scattered bryozoans.

At Sawtooth Mountain (1241), a collection (10854) 

is noteworthy in containing one of the few horn corals 

found, but the fauna basically consists of bryozoans 

and a few mollusks. Sheep Creek (1234) contains orbiculoid brachiopods, bryozoans, and a few mollusks. The 

Little Water Canyon (1341) collections are similar but 

contain only inarticulate brachiopods, including Lingula (12304), and bryozoans. Mollusks are abundant in 

the collections from Wadhams Spring (1246) but for 

the most part are poorly preserved. They are abundant 

and better preserved in the collections from Big Sheep 

Canyon (1224) and Sheep Creek (1234).

There is a strong similarity between the collections 

from these last two sections which invites comparisons 

with other areas. For example, the Schizodiis-bellerophont&CQ&n-Plagiogfypta faunule found in both is similar to that in the Uinta Mountains of northern. Utah. 

The predominate Neospirifer, found higher in these 

sections, is similar to that in collections from Fall 

Creek (39), Idaho and the Wind River Mountains in 

Wyoming. Finally, the large pelecypods found at Big 

Sheep Canyon (18582) are similar to those from Fall 

Creek in Idaho, Poison Creek (1331) and Middle Fork 

of Pine Creek (1205) in Wyoming, and the Crawford 

Mountains (A) in northeastern Utah.

The single collection from Crooked Creek (1296) 

(11694) contains a few poorly preserved productoid 

brachiopods and some bryozoans. From sections in this 

general area near Lima, Mont., the late J. Steele 

Williams collected abundant Antiqtiatonia; except for 

a few Neospirifer, these earlier collections contain 

little else. These collections are more similar to those 

from limestone lenses within the Rex Chert Member 

in Idaho, particularly those from Montpelier Canyon 

(1207) (9884, 9894), than to any from the Franson 

Member in other States.

UTAH

Because the Retort Shale Member of the Phosphoria 

Formation is absent except in Rich County in northeastern Utah (Cheney, 1957, p. 17), the carbonate sequence above the Meade Peak Member is considered to 

be a single unit. Although it may be possible to distinguish the Ervay Member of the Park City on a 

purely physical stratigraphic basis, the name has been 

employed only in the vicinity of Laketown Canyon. 

The greater thickness of the Franson Member in some 

sections and the more conspicuous development of the 

Gerster Formation in western Utah suggest most 

strongly that in much of the area the upper part of the 

Franson includes beds equivalent to younger members 

elsewhere in the report area. A few of the collections 

occur relatively high in the Franson and their faunal 

content is markedly different from that of the underlying collections. These collections have been differentiated informally as "upper Franson" and are discussed 

on p. 642.

Disregarding these collections, the Franson is represented by 34 collections, one which is a re-collection, 

from 14 localities. Almost two-thirds of these collections are from three of the localities. Two other collections were discarded because they contained no fossils.

Westward from the Uinta Mountains area, at Split 

Mountain (J) (19407), Coulter Ranger Station (H) 

(10019, 19406), and Blind Stream (F) (19408), the 

fauna of the Franson is characterized by Plagioglypta, 

bellerophontacean gastropods, and pelecypods, commonly Scfiizodus or Permophorus. There is some local 

variation in kinds and numbers, but the fauna is clearly 

recognizable. This fauna is also present, though poorly 

preserved, at Brush Creek Gorge (1219) (19405); it is 

well represented at Horseshoe Canyon (1339) (12228, 

19404) and is predominate at Dry Bread Hollow (B) 

(19415).

Devils Slide (1345) yielded a small collection of 

scaphopods and scraps of other fossils (12285). A few 

scaphopods and pelecypods at Franson Canyon (1347) 

(12499) might be representatives of the fauna. At both 

these sections, however, the lithology of the rock and the
636 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

sparseness and the limited variety of the fauna are 

atypical compared with these characteristics of this 

molluscan f acies to the east.

Underlying the Plagiogl/ypta faunule at Horseshoe 

Canyon is a bed containing only orbiculoid brachiopods. 

Overlying the Plagioglypta beds is a collection (12285) 

containing a few bryozoans, one pelecypod, and a fish 

fragment. Above that, a collection (12286) contains 

bryozoan fragments, crinoid stems, an orbiculoid, and 

a fish fragment. The next collection (12287), the highest in the sequence, contains only ScJiizodus. To the 

north at Middle Piney Lake in Wyoming the writer 

observed two zones of Plagioglypta but could not collect from them. Possibly the stratigraphically high 

Schizodus at Horseshole Canyon is indicative of a second molluscan horizon within the Franson Member.

The beds underlying the Plagioglypta fauna at Franson Canyon contain mostly orbiculoids, molluscan steinkerns, and a few fish fragments. The collection immediately below the Plagioglypta beds contains Lingula 

(12497). At Devils Slide (1345) (12486), orbiculoids occur above the Plagioglypta beds.

Wolf Creek (1231) contains orbiculoids, fish remains, 

and nuculoid pelecypods. At Strawberry Valley (1371), 

nuculoids and orbiculoids occur; at Fort Douglas 

(1350), orbiculoids and fish remains again occur. No 

scaphopods or other mollusks characteristic of the 

faunule are known to have been taken from any of 

these three sections. These collections are similar to collections from the Meade Peak Member, and, when a 

definitive stratigraphic study is completed, some or all 

may be transferred to that unit.

In marked contrast to these molluscan beds, the 

Brazer Canyon (1203) beds contain abundant bryozoans. These byrozoans are not so abundant as the similar bryozoans from the Ervay Member at the top of the 

section in this area and seemingly do not form biostromal masses as they do in the Ervay. The presence of 

Antiquatonia (10749) is unusual, but because this genus 

is confined to limestone lenses within the Rex Chert 

Member in Idaho, it is possible that these fossils here 

represent a similar lens, rather than a tongue of the 

Franson Member. In the same general area, at Crawf ord 

Mountains (A) (16710), large Pseudomonotis occur and 

are similar to those found in southwestern Wyoming 

at the Middle Fork of Pine Creek and Poison Creek and 

in Montana at Big Sheep Canyon.

WYOMING

In Wyoming 63 collections, one of which is a re-collection, are available from 17 sections discussed by 

Sheldon (1963). Two other collections were found to be 

unfossiliferous and were discarded. Sheldon indicates

on his columnar sections the presumed point of maximum regression of the sea. Most of the collections are 

from above this line of maximum regression, and consequently only collections from below this line are so 

noted. In contrast to some of the lithologic units in 

Wyoming, there are enough collections from many of 

the sections for one to observe a systematic change in 

the faunas. These changes are not all necessarily related to the one major regressive-transgressive cycle 

but may be caused in part by minor fluctuations of sea 

level during Franson time. This pattern can be interpreted from the geographic distribution if allowance is 

made for the occurrence of several kinds of fauna in 

different strata at one locality.

In addition to these 17 sections, there are 4 sections 

in the southwestern quadrant of Wyoming to consider. 

These are represented by 23 collections, 3 of which are 

re-collections. At Basin Creek (1381) and the Middle 

Fork of Pine Creek (1205), collections listed in the 

U.S. Geological Survey circulars as being from the 

Eex Chert Member would be classed as Franson under 

the revised nomenclature. Collections from Cokeville 

(1289) and Poison Creek (1331) were not listed in early 

publications. The field labels indicate that they were 

obtained from the Rex Chert Member, which is now 

classed as Franson. Those sections have not been analyzed to determine the line of maximum regression. 

Accordingly, it seems best to discuss them first to avoid 

possible confusion about this particular point.

At Poison Creek, two collections contain bryozoans 

and a few pelecypods (12315) and Composita and 

crinoid stems (12316). Of considerable interest were 

beds crowded with the large irregular pectenoid 

Pseudomonotis (18816). Some of the limestones are almost shell coquinas with just enough matrix to hold 

them together. A few bellerophontacean and neritacean 

gastropods occur with the pelecypods. Field observations indicate that there are two molluscan beds stratigraphically about 20 feet apart.

Large Pseudomonotis also occur at the Middle Fork 

of Pine Creek in Wyoming, in the Crawford Mountains 

of Utah, at Fall Creek in Idaho, and at Big Sheep 

Canyon in Montana. They were not discovered until 

about the middle of the 1959 field season, and it was 

not possible to revisit localities in Utah to search for 

them. Nevertheless, they probably will be found in 

other sections.

Basin Creek is an atypical locality in that it has 

yielded abundant well-preserved silicified brachiopods. 

For this reason, several collections have been made. The 

fauna, while large, is little varied and consists principally of Neospirifer and Sphenalosia and most closely 

resembles collections from Fall Creek, Idaho, and
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 637

places on the east flank of the Wind Kiver Mountains. 

A few other brachiopods occur, including one dictyoclostid.

Two small collections from Cokeville contribute little. 

One contains poorly preserved productoids; the other 

contains poorly preserved rhynchonelloid brachiopods. 

The Middle Fork of Pine Creek section (1205), in addition to containing large Pseudomonotis, has many fossils in other collections. In the lower part of the section 

are a few poorly preserved mollusks, above which are 

beds containing abundant "Liosotella" (9723). Still 

higher is a collection containing bryozoans and a few 

pelecypods (9724). This is followed by three collections 

(9725, 9726, 9739) predominated by Bathymyonia and 

some bryozoans. Still higher are more bryozoans, crinoid stems, and Pseudomonotis. Above the Pseudomonotis, three collections (9735, 9732, 9727) contain bryozoans predominately and a few spiriferoids. At the very 

top of the section is a collection of abundant bellerophontaceans (9731) that might actually represent the 

southwestern feather edge of the Ervay Member. None 

of the brachiopods at Pine Creek are like those at the 

nearby Basin Creek section, and in terms of fauna and 

lithology, the section is best correlated with the Brazer 

Canyon section in northern Utah.

In this same general area of southwestern Wyoming, 

a collection from Wheat Creek (110) (13324) contains 

only Orbiculoidea; at Deadline Ridge (107) (13345) 

only bryozoans occur. Just to the southwest, at Fontenelle Creek (108), four collections are available, but 

it is not clear where they stand in relation to the line 

of regression and transgression. At the base are bryozoan fragments in a clastic matrix; orbiculoids are 

above. Still higher, a collection (13340), contains a 

variety of pelecypods, a few Plagioglypta and bellerophontaceans. This collection is not particularly typical 

of the Plagioglypta facies of the Franson as found in 

the Uinta Mountains of Utah. Still higher are more 

orbiculoids.

In West-central Wyoming, a collection (12228) from 

Conant Creek (124) contains only fenestrate bryozoans. 

The lithology is similar to that of a collection from a 

pre-Meade Peak limestone at Bull Lake (82) (15153) 

which contains fenestrate bryozoans, among other fossils. While this is the lowest fossil collection in the 

section, it does occur near the top of the reported Franson, and fenestrate bryozoans are known to have been 

taken from the Franson at Crystal Creek (44) (12543). 

In the absence of any other information suggesting an 

older age, this Conant Creek collection is considered 

as Franson.

Some of the best-preserved fossils in the Franson 

Member occur in the Wind River Mountains, particularly along their east flank. Typically they are brachiopods and bryozoans rather than mollusks that characterize this member in Utah. The abundance and good 

condition of the fossils may be related both to their 

sturdiness and the fact that the shaliness of the rocks 

allowed chemical weathering to release the fossils from 

their matrix.

At Bull Lake (82), Orbiculoidea (12555) occurs 

below the line of maximum regression in the Franson. 

Above the line, three collections contain only bryozoans. 

These are followed (12259) by one predominated by 

Neospirifer, another predominated by Echinauris, and 

another predominated by Bathymyonia. The highest 

collection (18603) also contains Echinauris; this is a 

more recently obtained collection, and its exact relation 

to the other collections may not be as assumed. A similar situation is found at Dinwoody Lakes. Orbiculoid 

brachiopods and a few mollusks (12158), fish fragments 

(12159), and Lingula (12160) in that order occur below 

the line of maximum regression. Above the line, two 

collections (12161) (12162) contain abundant Spirif erina and Derbyia and lesser amounts of bryozoan material. These are followed by Echinauris (12164) and 

then by a Bathymyonia assemblage (12165).

To the northwest at Burroughs Creek (68), generally 

the same sequence of collections occurs above the line 

of maximum regression. It begins with bryozoans and 

a few mollusks (12182), and bryozoans and Derbyia 

(12184), and Spiriferina (12183). In the next collections, these two brachiopods are more abundant. They 

are followed by a Neospirifer assemblage. This is followed by three collections containing Echinauris. Overlying beds containing Bathymyonia are placed in the 

lower part of the Shedhorn.

At the South Fork of Gypsum Creek (79), ostracodes 

(12236) and a scanty Plagioglypta fauna (12237) are 

found. It is not certain where they occur in reference 

to the line of maximum regression. Above the line are 

two collections of bryozoans and a few pelecypods and 

three of bryozoans and a Derbyia and a Spirif erina.

The Tosi Creek (56) collections are quite different. 

They consist of fish fragments and a pelecypod (12205), 

fish fragments and bryozoans (12206), and a bryozoan 

fauna with a fairly large number of associated mollusks 

(12207). To the northwest at Crystal Creek (1323), a 

Plagioglypta faunule (12538) occurs below the line of 

regression. Above it are two small collections (12540, 

12541) containing one or two pelecypods and gastropods; above them another Plagioglypta sequence 

(12542) occurs. Both of the Plagioglypta beds are like 

those of the Uinta mountains. Above these are fenestrate bryozoans and fish (12543) and more ramose 

bryozoans. At Gros Ventre Slide (42), the sequence is
638 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

fish remains, orbiculoid brachiopods, a Plagioglypta 

fauna, and then bryozoans.

The few remaining scattered collection contribute 

little but tend to confirm the sequence observed eastward. At Hungry Creek (47), poorly preserved pelecypods (12662) occur below bryozoans and a few Orbiculoidea, Derby ia, and Spiriferina (12664). At Teton 

Pass (49) (12579), fenestrate bryozoans occur. The 

overlying lower part of the Shedhorn Sandstone 

(12580) contains Derbyia. Southeastward at Hoback, 

(57), two Plagioglypta collections are followed by one 

containing only Allorisma. An overlying lower Shedhorn collection also contains Derbyia.

Further southeast at Buck Creek (60), poorly preserved productoids occur below the line of regression. 

A Plagi&glypta faunule (12632) occurs above it and is 

succeeded in turn by a small collection of Derbyia, 

Spiriferina, and Bathymyonia. 'Steer Creek (67) contains only a few poorly preserved mollusks succeeded 

by a Bathymyonia-bYjozo&n collection.

To generalize, collections containing abundant varied 

brachiopods occur along the east flank of the Wind 

River Mountains and in southwestern Wyoming. West 

of these collections, in extreme southwestern Wyoming, 

are bryozoans, orbiculoid brachiopods, and mollusks. 

The last two assemblages are similar to those found in 

the Uinta Mountains of Utah. To the north, in the 

central part of western Wyoming, similar collections 

are intermixed with some articulate brachiopods and 

lie between the diversified brachiopod faunas of the 

Wind River Mountains to the east and the more limited 

brachiopod collections at Fall Creek (39) in Idaho.

BEX CHEET MEMBER OF PHOSPHOEIA FORMATION

Few collections are available from the Rex Chert 

Member except in Idaho where they are widely distributed. As there is a partial change of facies involved, 

their distribution is complementary to that of collections from the Franson Member. Rex collections are 

designated on the faunal distribution charts by the 

symbol R.

IDAHO

There are 34 collections available from the Rex 

Chert Member in Idaho distributed among 15 sections. 

Seven additional collections were found to be unfossiliferous and were discarded.

In the Mud Springs section (1351), far to the west of 

most of the sections from which Rex fossils were obtained, one collection (12640) has been referred to that 

member. The collection contains Grurithyris and Orbiculoidea in a brown mudstone matrix. It is identical 

to underlying collections reported to be from the Meade 

Peak Member. Possibly this should be referred to the

cherty shale member of the Phosphoria (E. R. Cressman, written commun., 1961).

The northernmost collection at Bear Creek (37) 

(12536) contains indeterminate scaphopods and abundant small indeterminate pelecypods. It is similar to 

the collections from the lower part of the Shedhorn 

Sandstone in nearby sections of Wyoming. To the 

southwest at Rocky Canyon (1304) (11639), a single 

relatively large fin ray of a fish constitutes the 

collection.

At Henry (1309) (11635), West Dairy (1208) 

(9940), and Lone Pine Springs (1298) (11517), sponge 

spicules are abundant in chert. Sponge spicules and 

orbiculoid brachiopods (10448) occur at North Rasmussen Valley (1233) in the same collection and separately (10449, 10450) in overlying collections. Spicules 

and bryozoans (11587) also occur in a single piece of 

chert from North Stewart (O). To the south of Snowdrift Mountain (1372) (12598), abundant spicules 

occur with fish scales. The same association occurs at 

Hot Spring (1317) (12605) above collections containing only spicules. At Deer Creek (1268) spicules are 

abundant, but one collection (12633) from a limestone 

contains abundant Anidantlvus; this collection could be 

from a limestone lens within the chert.

At Kendall Canyon (1258) (10483), Lingula, indeterminate articulate brachiopods, and Bdbylonites 

occur. A few feet higher (10484), Gancrinella, Streblochondria, and Nuculopsis occur in a phosphatic shale 

matrix. Just to the south at Mabie Canyon (1210) 

(10061), abundant Stre'blochondrm occur in a limy 

siltstone reported to be just above the base of the Rex. 

Streblochondria are common in limestone at North 

Stewart (O) (11584) and at Trail Canyon (1206) 

slightly to the west (9953).

In marked contrast to both the spicule and the 

Streblochondria assemblages are the faunas obtained 

from limestone lenses within the Rex. Probably the 

most varied fauna has been obtained at the South Fork 

of Sage Creek (L) (19532), in large part because the 

fossils are silicified. The fauna is dominated by larger 

productoids with occasional smaller brachiopods and 

mollusks. Bryozoans are rare as are large pieces of 

crinoid stems, even though much of the rock is crinoidal. 

Many of the shells are worn or bored as though this 

accumulation had been uncovered on the bottom for 

a long tune. In addition, a coral, one of the four known 

from the Phosphoria rock complex occurs in this 

collection.

The Montpelier Canyon (1207) collections include one 

(9983) that contains only two specimens of Gomposita 

and Strebtochondria, and two (9985, 9986) that contain 

indeterminate smaller productoids. The other two
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 639

(9984, 9989) contain fairly abundant larger productoids. In a smaller collection from the divide between 

Trail and Wood Canyon (K) (12261), the larger 

productoids are much less common than the abundant 

Anidanthus. In the brachiopod occurrence previously 

mentioned at Deer Creek (1268) (12633), only Anidanthus occurs. North Stewart (O) contains both. 

StreblocJiondria and sponge spicules but is particularly 

characterized by an abundant and varied productoid 

brachiopod fauna (11585, 11586, 11588).

Although more collections have been made from the 

Kex Chert Member in Idaho than in all other States 

combined, it is difficult to see any obvious geographic 

pattern. To the north, one collection of mollusks is 

similar to collections in western Wyoming. Southward, 

the collections are predominated by sponge spicules, 

except for several collections in the southeastern part 

of the State where brachiopod assemblages predominate. These brachiopods are bounded on the south by 

additional spicule-bearing beds near the Utah border 

and to the east by similar spiculites at Deadline Eidge 

(107) in Wyoming.

MONTANA

The second largest group of Kex collections, comprising 10 collections from 5 sections, were obtained from 

Montana. As in the collections elsewhere from this unit, 

the fauna shows relatively little diversity.

At Big Sheep Canyon (1224), one collection (9921) 

is similar to many of those from Idaho in containing 

sponge spicules and orbiculoids. To the south at Little 

Sheep Creek (1294) (11647), only fish remains were 

collected. Two of the collections from Sheep Creek 

(1234) contain only spicules, but a higher collection 

contains only fish remains. The highest collection 

(10810) contains a nuculoid pelecypod and an indeterminate gastropod. The lithology of this collection is 

limestone; therefore, it possibly could have come from 

the overlying Franson Member rather than the Kex.

Fish remains and inarticulate brachiopods, including 

Lingula (10840), characterize the two collections from 

Wadhams Spring (1246). Finally, the two collections 

from Little Water Canyon (13411) contain orbiculoids, 

poorly preserved small gastropods, and a few pelecypods. It is not possible to determine any meaningful 

geographic pattern from such a' small number of collections.

UTAH:

Only four collections from the Rex Chert Member 

were obtained in Utah. Three of these are from the 

Brazer Canyon section (1203); the fourth is from Laketown Canyon (1290). Another collection in the Craw269-092 68 6

ford Mountains (A) (16710), made before the Franson 

Member was defined, bears the field identification "Kex 

Chert near middle of section," but it is a limestone containing large pelecypods and has been transferred to 

the Franson Member. Two of the collections from 

Brazer Canyon are reported to be from the same bed. 

They are quite different and presumably were collected 

from slightly different intervals within the bed, though 

this cannot be determined from the field notes.

Of the four collections from the Kex} the first (10473) 

contains ramose bryozoans, rhychonelloid brachiopods, 

and Steblochondria; the second (10744) contains a few 

orbiculoid brachiopods, rhynchonelloids, and some fish 

remains; the third (10745), from somewhat higher in 

the section, contains poorly preserved Antiguatonia in 

a limestone matrix and may be a lense within the chert, 

as was suggested for a higher collection (10749); and 

the fourth (10965) from Laketown Canyon differs from 

all the others in containing only a few specimens of 

Ohonetes.

WYOMING

Seven collections, one of which is a re-collection, are 

available from four sections of the Kex Chert Member 

in Wyoming. A single collection from Basin Creek 

and one from Coal Canyon were found to be unfossiliferous and were discarded. Thirteen collections made 

earlier and one collection made by the writer from the 

Middle Fork of Pine Creek are assigned to the Franson Member. This outcrop was visited in 1959, and its 

predominate aspect is that of a limestone rather than 

a chert. In every case the matrix of the fossils is limestone, and the fossils are typical of the Franson Member elsewhere. Collections from Basin Creek also have 

been transferred to the Franson Member. All these 

earlier collections were assigned to the Rex but were 

obtained before the Franson Member was defined.

To the east, one collection (12260) at Bull Lake (82) 

contains two specimens of "Liosotella" in a limestone. 

Further west at Tosi Creek (56) (12204), there are 

only abundant specimens of large orbiculoids in a clastic limestone. Though referred to as being from the 

Rex Chert Member, these fossils may be from thin 

interbedded tongues of the Franson Member.

At Hungry Creek (47), sponge spicules are abundant 

in chert (12660). At Deadline Ridge (107), there are 

also abundant sponge spicules in chert (13343), above 

which are mollusks (13350, 18633). Scaphopods and 

bellerophontid gastropods are common and remind one 

strongly of the Franson Member where it is exposed 

in the Unita Mountain area. The rock is a veritable 

coquina of pelecypod shells cemented by silica. Of particular interest is the pelecypod Oeltoides which is 

known to have been found only in the Wind River
640 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

Mountain area between Bull Lake and DuBois and at 

this locality.

One collection from Coal Canyon (1201) (9747) contains a few fish scales and numerous small somewhat 

worn productoids in a limestone matrix. A higher collection (12618) contains one Cancrinella and one Rhynchopora. These collections do not resemble others in 

Wyoming but are similar to Rex collections from 

Brazer Canyon (1203) in Utah.

LOWER MEMBER OF SHEDHORN SANDSTONE

Throughout most of its outcrop area in Montana and 

Wyoming, the Shedhorn Sandstone is divisible into two 

tongues by the intervening Retort Phosphatic Shale 

and Tosi Chert Members of the Phosphoria Formation. The collections from the lower part of the 

formation are indicated by the symbol LS on the faunal 

distribution charts.

MONTANA

The fauna of the lower part of the Shedhorn Sandstone in Montana is known from only one collection 

from the Alpine Creek section (1307). This collection 

(11686) contains fragments of orbiculoid brachiopods.

WYOMING

In Wyoming 28 collections are available from 11 sections. One of these is a re-collection from the lower part 

of the Shedhorn Sandstone. Four others were unfossiliferous and discarded. Except for one collection from 

Deadline Ridge (107), all are from the northern half 

of western Wyoming. At only 2 of the 10 localities 

have fossils also been collected from the Rex Chert 

Member, but at 7 of these localities fossils were also 

obtained from the Franson Member. Thus the collections reflect the intertonguing of the facies.

The lowest collection at Tosi Creek (56) (12201) 

taken from directly above the Tensleep Sandstone is 

most peculiar in containing a coral, pectenoid pelecypods, and abundant fenestate bryozoans. It may be 

more comparable to the Grandeur at Dinwoody Lakes 

(75), Wyo., and Big Sheep Canyon (1224), Mont., than 

to any of the faunas from the Park City, Phosphoria, 

or Shedhorn Formations. The overlying collection 

(12202) from the same stratigraphic unit contains 

"fairy collar button" type of fish teeth, which presumably indicate a Permian age (Yochelson and others, 

1961), but it also contains a tooth of Dicrinotus, identified by D. H. Dunkle, heretofore only reported from 

the Mississippian.

The lowest collection at Hungry Creek (47) (12659) 

contains only a few scaphopods. The highest collection 

at Red Creek (2) (12550) contains scaphopods and a

more varied molluscan fauna. This Red Creek assemblage, although not quite like that typical of the Franson in the Uinta Mountain area of Utah, is more similar to it than are any of the other collections from the 

lower Shedhorn.

Fairly good larger brachiopod assemblages, characterized particularly by Neospirifer and Bathymyonia^ 

occur at Burroughs Creek (68) (12189, 12190, 12191), 

and a Derbyia assemblage occurs at Teton Pass (49) 

(12580). Orbiculoidea and a single specimen of Derbyia 

occur at Forellen Peak (4). A single specimen of Derbyia occurs at Hoback (57) (12143), and above that 

some pelecypods are found (12144). It is not certain 

that these Derbyia occurrences mark a single stratigraphic level within the lower part of the Shedhorn 

Sandstone. Orbiculoidea^ fish remains, and a single 

Derbyia occur at Crystal Creek (44) (12118).

The remaining collections, forming the bulk of the 

lower Shedhorn material, contain only fish remains or 

orbiculoid brachiopods. The only diversity from these 

two elements is at Forellen Peak (4) where one collection (18597) also contains small, moderately high 

spired gastropods and another (12554) also contains 

Lingula.

The brachiopods from Burroughs Creek are forms 

typical of the Franson Member throughout the Wind 

River area. Other collections from the lower part of the 

Shedhorn Sandstone containing Derbyia in almost 

every instance are associated with typical Franson 

brachiopod assemblages, either directly above or more 

commonly directly below. They fall into the same general sequence of fossil categories recognized within the 

Franson. It is possible that some, if not all, of these 

occurrences might be from thin tongues of the Franson Member not heretofore recognized. It was not possible to make a subsequent field check of stratigraphic 

relations; the collections are retained within the lower 

part of the Shedhorn Sandstone.

The remaining collections contain fish fragments, 

usually teeth or bone, orbiculoid brachiopods, and 

pelecypods. Except for the Deadline Ridge section, they 

are arranged in an approximate semicircle to the north 

and west of the brachiopod beds within this member. 

The northernmost collections contain scaphopods.

EETOET PHOSPHATIC SHALE MEMBEK OF

PHOSPHORIA FORMATION

Iii contrast to the Meade Peak Phosphatic Shale 

Member, the Retort Member has not been extensively 

searched for fossils. Even in Montana where the unit 

is economically important, the collections available are 

limited. The small number of collections and this lack 

of wide distribution, particularly in Wyoming, present
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 641

problems in interpretation. Collections from the Retort 

Member are indicated by the symbol Rt on the faunal 

distribution charts.

IDAHO

Four collections were made from the Retort where 

exposed in three sections. Two, however, were unfossiliferous and discarded. One collection (12613) 

from Hot Spring (1317) yielded only a few fish scales. 

The other, from Deer Creek (1268) (12634), might be 

an impression of part of a squid jaw (A. G. Fischer, 

written commun., 1961).

MONTANA

Seventy-two collections are available from the Retort 

collected from 13 measured sections. Half the collections, however, are from two sections, and most of these 

are from Sheep Creek (1234), the type locality of the 

member.

Collections from Kelley Gulch (1249) and Cave Creek 

(1257) are monotonous, containing only orbiculoid 

brachiopods and scattered fish remains, most of which 

are small teeth and bone fragments. These forms and 

a collection containing predominately Polid&vcia occur 

at the West Fork of Blacktail Creek (1302). A similar 

assemblage is found in the Retort collection from Little 

Sheep Creek (1294), except that Polidevcia is predominate in two of the four collections. Polidevcia, fish remains, and orbiculoid brachiopods occur also at Cedar 

Creek (1256). The highest collection from this section 

(10829) contains abundant Plagioglypta and bellerophantacean gastropods in a sandy matrix. Although 

this section is considered to be Retort, probably it is 

from the Shedhorn Sandstone; field notes, however, do 

not provide sufficient detail to confirm this possibility 

(E.R. Cressman, written commun., 1961). Fish remains 

are present at Canyon Camp (1311). Orbiculoid 

brachiopods alone are present at Sliderock Mountain 

(1301) and Sawtooth Mountain (1241).

A single collection from Wadhams Spring (1246) 

contains principally Polidevcia. This genus is also predominate in the more abundant collections from Dalys 

Spur (1222). The numerous collections from Sheep 

Creek (1234), for the most part, contain PoUdevcia. 

A few contain orbiculoid brachiopods, fish remains, and 

/Streblochondria. Of particular interest here is the presence of the tentacle hooks of squids, a faunal element 

seen elsewhere only in the Meade Peak Phosphatic Shale 

Member. Virtually the same fossils occur at Big Sheep 

Canyon (1224), although /Streblochondria is absent and 

Worthenial is present. The three collections from the 

nearby Little Water Canyon section (1341) contain predominately Streblochondria, Worthenia, and orbiculoid 

brachiopods; there is no indication of tentacle hooks.

The most fossiliferous and varied collections are in 

extreme southwestern Montana. These bear the closest 

resemblance to collections from the Meade Peak Member 

in Idaho. There is less variety to the north and northeast. In the easternmost and northernmost sections, 

mollusks are missing, and the fauna consists exclusively 

of orbiculoid brachiopods and fish remains. Northward, 

the fish remains tend to be increasingly more resistant.

WYOMING

Fifty-seven collections were made from the Retort 

at 19 sections, but 5 were unfossiliferous and discarded. 

As will be pointed out, some of the collections nominally 

from the Retort may actually represent other members.

At Conant Creek (124), the lower two collections 

contain only fish remains and orbiculoids. Above these, 

one collection (12231) contains a few large brachiopods 

so poorly preserved that they can be clearly interpreted 

as reworked. Still higher (12233), a few fragmentary 

bryozoans occur; this collection may represent the southeastern feather edge of the Franson Member. Two other 

collections contain nuculoid pelecypod steinkerns. These 

steinkerns, though commonly indeterminate, are different from those in the Franson Member, particularly 

from the Uinta Mountain area.

At Bull Lake (82), a collection (12264) contains a 

characteristic Franson Bathymyonia fauna but is designated as Retort. To the north at Dinwoody Lakes (75), 

the lowest Retort collection (12163) is interbedded with 

the Franson Member and the next collection (12166) 

above lies directly on the Franson. Again, it seems unlikely that these collections are truly representative of 

this member. The higher Retort collections contain 

pelecypod steinkerns similar to those at Conant Creek. 

At the South Fork of Gypsum Creek (79) and at Tosi 

Creek (56), fish remains, orbiculoid brachiopods, and 

nuculoid pelecypods occur in the Retort.

The stratigraphic position of the Basin Creek (1381) 

collections is also questionable. The lowest collection 

(13312) contains only orbiculoids, but the next highest 

collection (13309) contains fragments of clearly reworked bryozoans. The highest collection (13310) contains a small poorly preserved brachiopod fauna, which 

reasonably could be interpreted as being from a western edge of the Ervay. Similarly, at the Middle Fork 

of Pine Creek (1205) (9792A, 18897), a few Composita 

at the very top of the section are suggestive of the 

Ervay.

The lowest collection at Deadline Ridge (107) 

(13347) contains what appears to be a Franson brachiopod assemblage; their poor preservation adds support 

to the inference that they were reworked. The next collection (13348) above contains the characteristic nucu-
642 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

loid pelecypods, but the highest collection (13349) is 

unique to the Retort in containing Foraminifera.

The other scattered collections add little to the general picture, but two additional localities are worthy 

of comment. At Coal Canyon (1201), nuculoid pelecypods occur, but there is somewhat more diversity in the 

fauna. At Crystal Creek (44), a few collections contain 

Cancrinella, in addition to a slightly diversified mollusk 

assemblage; one collection (12122) contains orbiculoids 

and squid tentacle hooks. These sections, particularly 

Crystal Creek, show more diversity than has been found 

in the Idaho collections from the Retort. Except for 

these, the collections which are clearly from the Retort 

contain a limited assemblage.

CHERTY SHALE MEMBER OF PHOSPHORIA 

FORMATION

Only two collections have been made from this member. One collection each has been made from the Little 

Sheep Creek (1294) and Big Sheep Canyon (1224) sections in southwestern Montana. Both collections contain predominately Polidevcia and are similar to underlying Retort Member collections. The collections are 

indicated on the f aunal distribution charts by the symbol CS.

ERVAY CARBONATE ROCK MEMBER OF PARK 

CITY FORMATION

Collections from this member are limited to Wyoming, but collections thought to be from rocks of equivalent age in Utah are also treated here. In both states 

only a few scattered collections are available, and no 

obvious geographic changes in the faunas can be observed. The collections from Wyoming are indicated on 

the f aunal distribution charts by the symbol E; those 

from Utah are indicated by the symbol UF.

UTAH

As noted (p. 635), certain of the Franson collections 

were distinguished as being in the "upper Franson" on 

the basis of their stratigraphic position high in the member. The collections are similar to those found in the 

Ervay in Wyoming, but because the intervening Retort 

Shale is absent, they are stratigraphically considered as 

from the Franson. Seventeen collections, one of which 

is a re-collection, were considered to be "upper Franson;" these are distributed among nine localities.

To the east at Blind Stream (F), one collection 

(19408) contains abundant fragmentary fish remains 

and a few poorly preserved bryozoans and orbiculoid 

brachiopods. The stratigraphic significance of this occurrence has been discussed elsewhere (Yochelson and 

others, 1961). A few fish remains and bryozoans each

compose a small collection from Strawberry Valley 

(1371).

At Franson Canyon (1347), three small collections 

are best characterized as bryozo&n-$piriferina assemblages. The same assemblage occurs at the Right Fork 

of Hobble Creek (1271) (12623) and Mill Creek (D) 

(19413). At Fort Douglas (1350) (12529), there are 

fewer brachiopods.

At Cephalopod Gulch (C) (18891), small productoids are the predominate f aunal element. The locality 

is one of the few places where fossils were collected from 

a shale in the Ervay rather than a limestone, and this 

may account for the difference in the fauna. At Devils 

Slide (1345) (12488, 19412) bryozoans occur, but the 

predominate forms are large productoid brachiopods 

and large Composita. The fauna of this locality more 

closely resembles that of the Ervay outcrop in the Wind 

River Mountains than do any of the other localities in 

Utah.

Finally, in the Brazer Canyon (1203) collections the 

bryozoan-Spiriferina assemblage is again predominate. 

In this area the assemblage is particularly impressive 

because the bryozoans form beds several feet thick. 

Other fossils are present in small numbers, but the presence of rare forms is clearly the effect of large-scale collecting; these collections are four to five times larger 

than those from other outcrops of the "Upper Franson" 

in Utah.

WYOMING

The Ervay in Wyoming is represented by 30 collections, one of which is a re-collection, from 9 localities. 

In addition, several of the collections nominally from 

the Retort in southwestern Wyoming, contain a few 

fossils which may represent the thin southern extension 

of the Ervay Member. The fauna is most abundant in 

the Wind River Mountains, but for simplicity it is better to consider the other localities first.

Only fish remains are known to have been taken from 

the Ervay at Conant Creek (124) (12235) and South 

Fork of Gypsum Creek (79) (12246). A few large pelecypods, which may be Oeltoides^ and rare Bellerophon 

occur to the north at Togwotee Pass (41) (18600). To 

the west at Steer Creek (67), two small collections 

(12647, 12649) contain WeUerella and a few Chonetes. 

Overlying this is a collection (12648) containing mostly 

small productoids similar to those obtained at Cephalopod Gulch (C) in Utah.

At Tosi Creek (56) (12212), a small collection contains only bryozoans; these are mainly f enestrate rather 

than ramose growth forms. Just to the south at Bartlett 

Creek (66) (12219), a small collection contains mostly 

Spiriferina.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 643

The remaining three localities, Burroughs Creek 

(68), Dinwoody Lakes (75), and Bull Lake (82) show 

the most diversity. At Burroughs Creek, the lowest 

Ervay collections contain bryozoans and subordinate 

pelecypods. This is followed up the section by beds of 

Bathymyonia,) beds of Derbyia-Spiriferina^ and finally 

beds of bryozoans and subordinate numbers of 

pelecypods.

To the southwest at Dinwoody Lakes, the sequence 

starts with bryozoans and a few associated pectenoids 

and is followed by Bathymyonia collections. These are 

followed in turn by collections of bryozoans, Derbyia^ 

and Spiriferina and then collections of mostly Derbyla 

and /Spiriferina.

Even further southwest at Bull Lake, the sequence 

also starts with bryozoans, followed by bryozoans with 

subordinate Derbyia and Spiriferina. These are succeeded by bryozoans with subordinate pectenoids. This 

is followed by Derbyw-Spiriferina beds and finally, 

productoid beds predominated by Muirwoodia.

The only collection strikingly different is from Bull 

Lake (18604) at the top of the section. The faunule is 

a bellerophontsiC&SLn-Plagiog'l'ypta one, similar to that 

from the Shedhorn Sandstone at Big Timber (M) in 

Montana.

TOSI CHERT MEMBER OF PHOSPHORIA 

FORMATION

The limited distribution of collections from the Tosi 

Chert Member contrasts with that of the lithologically 

similar but older Kex Chert Member of the Phosphoria. 

Collections from the State of Montana are comparable 

in fauna and distribution, but only about one-fourth as 

many collections have been made from this unit as from 

the Kex. The Tosi Chert Member is missing in Idaho 

and most of Utah and is generally unsampled in Wyoming. Tosi collections are indicated by the symbol T 

on the f aunal distribution charts.

MONTANA

Thirteen collections of Tosi Chert fossils have been 

taken from 8 sections in Montana. One of these, from 

the West Fork of Blacktail Creek, is a re-collection 

made to obtain additional specimens of the peculiar attached brachiopod Leptodus (Dutro and Yochelson, 

1961). Another re-collection was made at Sheep Creek.

The southernmost collection at Little Sheep Creek 

(1294) contains only Polidevcia and is similar to many 

of the collections from the Retort phosphatic shale member. To the north, a single collection from Wadhams 

Spring (1246) contains only fish remains. Both of these 

collections are in a black shale. Orbiculoid brachiopods 

and fish scales occur at Dalys Spur (1222) in a gray

mudstone matrix. It is possible that all three collections 

are from the underlying Retort Member (E. R. Cressman, written commun., 1961).

At the West Fork of Blacktail Creek (1302) and 

Hogback Mountain (1299), the Tosi is characterized by 

a mixed brachiopod and pelecypod assemblage. Lingula 

occurs at each section. A similar fauna occurs at Sawtooth Mountain (1241) but has been referred to the 

underlying upper part of the Shedhorn Sandstone. All 

three collections occur in a calcareous mudstone matrix ; 

they are in neither chert nor sandstone. Brachiopods 

occur at Sheep Creek (1234), but the fauna is quite unlike that in the three localities mentioned because it is 

virtually limited to Chonetes and WeUerella.

Much further north at Sappington Canyon (1357), 

only tiny fish teeth occur in a sandstone. To the northeast at Logan (1367), fragmentary bryozoans and orbiculoid brachiopods were collected. This is the only 

collection from the Tosi that occurs in a true chert.

WYOMING

The Tosi Chert Member is represented in Wyoming 

by two collections from Burroughs Creek (68). At Burroughs Creek, one collection (12193) contains only fish 

remains and the other (12195) contains only nuculoid 

pelecypod steinkerns. Both are in a black shale or mudstone matrix rather than a chert matrix. The fauna of 

both is similar to that in the underlying shale of the 

Retort Member. Four other collections from three other 

sections were unfossiliferous and discarded.

UPPER MEMBER OF SHEDHORN SANDSTONE

Although collections are both more abundant and 

more widespread than in the underlying lower member, they are comparable to those from that unit. This 

approximate similarity is in contrast to the marked differences in number and distribution of collections between the Meade Peak and Retort Phosphatic Shale 

Members and between the Rex and Tosi Chert Members 

of the Phosphoria Formation. On the f aunal distribution charts, the collections from the upper member of 

the Shedhorn Sandstone are indicated by the symbol 

US.

MONTANA

Fourteen collections are available from Montana, 

three of which are re-collections from the upper part 

of the Shedhorn Sandstone; these are distributed 

among six sections. One other collection from Sheep 

Creek (1234) was unfossiliferous and was discarded. 

It seems likely that a collection (10829) from Cedar 

Creek (1256) should be referred to this unit, but it has 

been discussed under the Retort Member (p. 641).
644 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

A single collection (10857) from Sawtooth Mountain (1241) contains a mixed brachiopod and pelecypod 

fauna. Both f aunally and lithologically it is remarkably 

similar to collections from the nearby West Fork of 

Blacktail Creek and the Hogback Mountain sections 

which have been referred to the Tosi Chert Member 

of the Phosphoria Formation. The Sawtooth Mountain section is too incomplete to permit detailed correlation with these adjacent sections (E. R. Cressman, written commun., 1961).

To the north at Hogback Mountain (1299), two collections have been made: one contains sponge spicules, 

and the other contains small poorly preserved productoid brachiopods. At Alpine Creek (1307), the collections are composed almost entirely of pelecypod shells 

so abundant that the rock is nearly a coquina. The fauna 

is comparable to that at Forellen Peak in Wyoming 

but is more varied. In contrast, the Sheep Creek (1234) 

collection contains fragmentary bryozoans, spiriferoid 

brachiopods, and pectenoids; it bears a resemblance to 

a Tosi collection from Gros Ventre Slide (42) in 

Wyoming.

Two collections from the same bed at Cinnabar 

Mountain (1363) contain practically nothing but bellerophontacean gastropods. The easternmost collection 

of Phosphoria age fossils is from Big Timber (M). This 

locality was found by Ealph L. Imlay in 1943 and was 

not systematically investigated during the course of 

fieldwork for the Phosphoria project. The bed arbitrarily has been assigned to the upper part of the Shedhorn 

Sandstone. It consists of about 10 feet of sandy limestone and is crowded with mollusks. These are mostly 

Schizodus, bellerophontacean gastropods, and a few 

Plagioglypta. The overall aspect is similar to that of 

the Franson Member in the western part of the Unita 

Mountains in Utah. It is also similar to the upper bed 

of the Ervay Member at Bull Lake in western 

Wyoming.

The northernmost collections of the upper part of 

the Shedhorn Sandstone from Sappington Canyon 

(1357) contain a similar molluscan assemblage. The 

three common genera here, however, all have an average 

size larger than that of the genera at Big Timber, and 

the specimens form a smaller percentage of the total 

rock volume. There is some similarity in the collections 

from the three sections in this northeastern area, but 

the other collections show no clear geographic trends.

WYOMING

Eleven collections, two of which are re-collections, 

are available from the upper part of the Shedhorn 

Sandstone; they are distributed among seven sections. 

As might be expected from the nature of the formation,

distribution is limited to west-central Wyoming and 

makes no clear pattern.

Orbiculoid brachiopods occur to the north at Bed 

Creek (2) (12553). Slightly to the southwest at Forellen Peak (4), one collection (12559) contains fragmentary bryozoans and fish remains. The other two collections (12260, 18596) consist of a few pelecypods in 

a sandstone matrix. This locality is, perhaps, most comparable to Alpine Creek (1307) in Montana. Still 

further south at Hungry Creek (47) (12667), only fish 

remains occur. Bartlett Creek (66) (1220) contains 

mostly bellerophontacean gastropods and fish remains, 

and Flat Creek (50) (12226, 12628) contains a more 

varied molluscan fauna, pectenoids being the most 

obvious forms.

In sharp contrast, at Gros Ventre Slide (42) (12135) 

and Tosi Creek (56) (12213, 18592) bryozoans predominate. Most of the bryozoans at Tosi Creek are 

relatively thin, twiglike forms, as are the majority of 

the few bryozoans from the other Shedhorn localities. 

In contrast, they are strikingly different from the 

Ervay bryozoans which are more massive and less twiglike in their branching. At the Tosi Creek locality the 

fossils are silicified; the basal part of the colonies, the 

relatively large size of fragments, the occasional complete specimens, and the orientation in the rock leave 

no doubt that at this locality all specimens are in place. 

The bryozoans from other localities in the Shedhorn 

Sandstone are all small fragments; it is likely that they 

have been reworked.

REGISTER OF LOCALITIES

With few exceptions most of the collections made 

from the Phosphoria formation and its equivalents were 

reported in various circulars of the Geological Survey, 

and other details of the measured sections were given. 

Some of these collections were indicated by the field 

number, others by the permanently assigned locality 

number. Most of the Montana collections are also listed 

in the descriptions of measured sections given by Cressman and Swanson (1964). Part of those from sections 

in Wyoming and from two sections in Idaho are also 

listed by Sheldon (1963). In the descriptions of measured sections, where possible, these authors have indicated the position of collections on columnar sections.

In the following pages stratigraphic sections and unmeasured localities for each State are listed in alphabetical order as a summary which gives the primary 

source of geographic information and the numbers of 

the collections from that locality. Letters have been 

assigned to those sections or localities not listed in the 

circular series. For all others, the section number given 

in the appropriate circular is listed.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 645

The succeeding information gives the location of each 

section or locality and the source for information on the 

precise stratigraphic position of the individual collections. Some collections listed in the circulars do not 

give the member assignment, or it has been subsequently changed.

Idaho 

[USGS, U.S. Geological Survey]

Section

No. used 

in circular

1316. 

1353 

1261.. 

1260. 

1200 

1268 

K 

1293 

1267. 

1314.. 

1338. 

1308.. 

N 

1309 

1317 

1209 

1258. ...

1298. 

1210... ___

1207 

1351 

1259. 

1233. 

o

1230 

1266.. 

1303. 

1304. 

1372 

1211 

L

1232. _ - .

1306 __ .

1265 _ -

1310 

1206.- __ .

1385 

1208 

1264... __ .

1322.... .

1262. 

Name

Ballard Trench- _____

Bear Creek (Sheldon No. 

37).

Deer Creek (Dugway) . ... 

Divide between Trail and 

Wood Canyons.

East Georgetown Canyon. 

Enoch Valley __ ........

Fall Creek (Sheldon No. 

39). 

Gravel Creek Divide. __ 

Grizzly Creek ______

Montpelier Canyon. . .....

North Rasmussen Valley .

North Wooley Range. ....

South Fork of Sage Creek. 

South Rasmussen Valley.. 

South Stewart Canyon ....

Timber Creek... ........

Trail Canyon.. ...........

West Dairy.. _____ . .

West Georgetown Canyon.

USGS 

Circular

No.

305 

327

262 

208 

208 

208

304 

262 

305 

327

305

305 

304

301 

262 

304 

208

301 

327 

262 

301

301 

262 

304 

305 

327 

301

§61 

304 

208 

304 

301

301 

262 

327 

262

Page

28 

11-13

13-16 

11-13 

25-29 

46-49

25-28 

30-33 

24-27 5-7

16-18

20-23 

29-30

32-35 

20-23 

20-23 

14-19

50-58 

20-22 

17-19 

10-13

5-7 

34-37 

14-16 

9-12 

15-19 

38-43

16-18 

9-13 

42-45 5-8 

21-29

44-49 

27-29 

8-10 9-12

Collection

11695-11696 

12530-12536

10488-10506 

10525-10548 

9700-9711 

12473-12477; 12633-12634 

12620-12621

10986-10991 

10727-10729; 10910-10922 

11589-11606 

18594-18595; 12288-12296

11607-11618 

19533 

11619-11635 

12599-12613; 12650-12658; 

19531 

10027-10031; 10091-10109 

10452-10484 

10993-10999; 11501-11518 

10020-10025; 10033-10044; 

10049-10061; 10117-10118 

9761-9772; 9977-9990 

12635-12642 

10507-10524 

10441-10451 

11584-11588 

10411-10440 

10705-10726 

11564-11583 

11636-11639; 11697-11712 

12582-12598 

10045-10048; 10062-10090 

19532 

10485-10487 

11520-11546 

10577-10602 

11547-11563 

9773-9787; 9922-9925; 

9953-9975; 10121; 11640 

12630-12631 

9926-9952; 9976 

10565-10576 

12109-12115 

10549-10564

Ballard Trench, sec. 7, T. 7 S., R. 43 E., Caribou County. Colln. 

11695-11696, by R. G. Waring, 1949, were taken from beds 

given in USGS Circ. 305, p. 28, as follows: Colln. 11695, from 

bed P-l; 11696, P-9.

Bear Creek, NE% sec. 31, T. 1 S., R. 45 E., Bonneville County. 

Colln. 12530-12536, by J. E. Smedley, 1951, are listed in 

USGS Prof. Paper 313-B, p. 174-178. Also, colln. 12530-12531 

and 12534-12536 are listed in USGS Circ. 327, p. 11-13. In 

addition, collections were taken from beds given in USGS 

Circ. 327 as follows: Colln. 12532, from bed P-10; 12533, 

P-ll.

Blackfoot Narrows, sec. 24, T. 7 S., R. 43 E., Caribou County. 

Colln. 10488-10506, by J. E. Smedley, 1948, were taken from 

beds given in USGS Circ. 262, p. 13-16, as follows: Colln. 

10488, from bed P-8; 10489, P-25; 10490, P-30; 10491, P-31; 

10492, P-33; 10493, P-35; 10494, P-37; 10495, P-38; 10496,

P-38; 10497, P-74; 10498, P-85 ; 10499, P-86; 10500, P-87; 

10501, P-89; 10502, P-94; 10503, P-99; 10504, P-108; 10505, 

P-109 ; 10506, P-lll.

Caldwell Canyon, sec. 1, T. 8 S., R. 43 E., Caribou County. 

Colln. 10525-10548, by J. E. Smedley, 1948, were taken from 

beds given in USGS Circ. 208, p. 11-13, as follows: Colln. 

10525, from bed CW-1; 10526, P-2; 10527, P-3; 10528, P-4; 

10529, P-7; 10530, P-12; 10531, P-16; 10532, P-17; 10533, 

P-20; 10534, P-30; 10535, P-47; 10536, P-57; 10537, P-59; 

10538, P-61; 10539, P-63 ; 10540, P-64; 10541, P-67; 10542, 

P-68; 10543, P-71; 10544, P-73; 10545, P-74; 10546, P-78; 

10547, P-79 ; 10548, P-81.

Conda mine, sec. 13, T. 8 S., R. 42 E., Caribou County. Colln. 

9700-9711, by Helmuth Wedow, 1947, were taken from beds 

given in USGS Circ. 208, p. 25-29, as follows: Colln. 9700, 

from bed CW-1; 9701, P-l; 9702, P-19; 9703, P-48; 9704, 

P-53; 9705, P-77; 9706, P-80; 9707, P-133; 9708, P-137; 

9709, P-138 ; 9710, P-140 ; 9711, P-142.

Deer Creek, S^SW^ sec. 34, T. 9 S., R. 45 E., Caribou County. 

Colln. 12473-12477 and 12633-12634 were collected by J. E. 

Smedley, 1951. Colln. 12473 was taken from a 4.0-ft bed of 

dense, thin-bedded limestone in Rex Chert Member ; 12474, 

from a 26.0-ft bed of dark-gray chert with lighter gray and 

white mottlings in Rex Member ; 12475, from a 26.0-ft bed of 

chunky light-gray mottled chert in Rex Member ; 12476, from 

a 1-ft bed of platy dark brownish-gray argillaceous lime in 

Dinwoody Formation ; 12477, from a 16.0-ft bed of dark-gray 

chert and siliceous dolomite in Rex Member : 12633, from a 

slightly argillaceous and cherty limestone lens in Rex Member ; 12634, from a dark-gray mudstone in Retort Member.

Divide between Trail and Wood Canyons, sec. 26?, T. 8 S., 

R. 42 E., Slug Creek County. Colln. 12620-12621, collected 

by J. E. Smedley, 1951, were taken from a 5.0 ft bed of 

slightly argillaceous and cherty limestone in Wells (?) Formation ; and from a bioclastic limestone lens in Rex Member, 

respectively.

Dingle, SE% sec. 36, T. 14 S., R. 44 E., Bear Lake County. Colln. 

10986-10992, by J. E. Smedley, 1949, were taken from beds 

given in USGS Circ. 304, p. 25-28, as follows : Colln. 10986, 

from beds P-29 to P-31 ; 10987, P-35 ; 10988, P-41 ; 10989, 

P-43 ; 10990, P-48 ; 10992, P-77 ; 10991, P-82.

East Georgetown Canyon, NE^NW^ sec. 30, T. 10 S., R. 45 E., 

Bear Lake County. Colln. 10727-10729, by J. E. Smedley, 

1948, and 10910-10922, by J. E. Smedley, 1949, were taken 

from beds given in USGS Circ. 262, p. 30-33, as follows: 

Colln. 10727, from bed P-95; 10728, P-96; 10729, P-98; 

10910, P-20 ; 10911, P-22 ; 10912, P-23 ; 10913, P-24 ; 10914, 

P-25 ; 10915, P-33 or 34 ; 10916, P-34 or 35 ; 10917, P-40 ; 

10918, P-93 ; 10919, P-96 ; 10920, P-97 ; 10921, P-99 ; 10922, 

P-101.

Enoch Valley, SW% sec. 16, T. 6 S., R. 43 E., Caribou County. 

Colln. 11589-11606, by J. E. Smedley, 1949, were taken from 

beds given in USGS Circ. 305, p. 24-27, as follows : Colln. 

11589, from bed P-l ; 11590, P-3 ; 11591, P-29 ; 11592, P-30 ; 

11593, P-33; 11594, P-42; 11595, P-51; 11596, P-54; 11597, 

P-55 ; 11598, P-73 ; 11599, P-74 ; 11600, P-76 ; 11601, P-83 ; 

11602, P-104 ; 11603, P-90 ; 11604, P-94 ; 11605, P-97 ; 11606, 

P-52.
646 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

Fall Creek, SW% sec. 18, T. 1 N., R. 43 E., Bonneville County. 

Colln. 12288-12296, by J. E. Smedley, 1950, and 18594-18595, 

by E. L. Yochelson and R. P. Sheldon, 1959, are listed in 

TJSGS Prof. Paper 313-B, p. 165-173. Also, colln. 12288-12296 

are listed in TJSGS Circ. 327, p. 5-7.

Gravel Creek Divide, sec. 34, T. 5 S., R. 43 E., Caribou County. 

Colln. 11607-11618, by J. E. Smedley, 1949, were taken from 

beds given in TJSGS Circ. 305, p. 16-18, as follows: Colln. 

11607, from bed P-l; 11608, P-2: 11609, P-10; 11610, P-15 ; 

11611, P-19; 11612, P-27; 11613, P-31; 11614, P-46; 11615, 

P-60; 11616, P-63; 11617, P-71; 11618, P-74.

Grizzly Creek, sec. 30, T. 5 S., R. 40 E., Caribou County. Colln. 

19533, by E. L. Yochelson and T. M. Cheney, 1959, were 

taken from Grandeur limestone 25-30 ft above base.

Henry, SE% sec. 10, T. 6 S., R. 42 E., Caribou County. Colln. 

11619-11635, by J. E. Smedley, 1949, were taken from beds 

given in TJSGS Circ. 305, p. 20-23, as follows: Colln. 11619, 

from bed P-l; 11620, P-2; 11621, P-3; 11622, P-21; 11623, 

P-42; 11624, P-46; 11625, P-47; 11626, P-48; 11627, P-64; 

11628, P-81; 11629, P-83; 11630, P-89; 11631, P-99; 11632, 

P-100; 11633, P-101; 11634, P-106; 11635, R-3.

Hot Spring, sec. 13, T. 15 S., R. 44 E., Bear Lake County. Colln. 

12599-12613 and 12657-12658 were collected by J. E. Smedley, 1951; 12650-12656, by H. I. Saunders and J. A. Peterson, 

1951; 19531, by E. L. Yochelson and T. M. Cheney, 1959. 

Part of section given in TJSGS Circ. 304, p. 29-30. Colln. 

12599 was taken from a 1.0-ft oolitic phosphate bed in 

Meade Peak Member; 12600, from a 1.6-ft dark-gray and 

yellowish-brown, oolitic phosphate bed in Meade Peak Member; 12601, from a 0.7-ft argillaceous, thin-bedded, darkgray, carbonaceous limestone about 3.8 ft above colln. 12600 

in Meade Peak Member; 12602, from a 1.0-ft argillaceous, 

dark brownish-gray limestone immediately above a thick 

4.0-ft zone of phosphate in Meade Peak Member; 12603, 

from a 4.5-ft carbonaceous, dark-gray to black limestone 

approximately 7 ft below colln. 12602 in Meade Peak Member; 12604, from a 6.0-ft dark-gray chert at base of Rex 

Member; 12605, from a 0.7-ft medium-bedded chert about 

8.0 ft above base of Rex Member; 12606, from a 1.2 ft dolomitic, argillaceous, cherty? limestone about 29 ft above base 

of Rex Member; 12607, from a 0.6-ft dull brownish-gray to 

medium-gray chert about 4.7 ft above base of Rex Member; 

12608, from a 4.0-ft chert, containing crystalline, dark-gray 

limestone concretions about 129.0 ft above base of Rex Member ; 12609, from a 1.6-ft calcareous and phosphatic mudstone 

about 131.0 ft above base of Rex Member; 12610, from a 

9.4-ft calcareous, mostly platy mudstone about 132.0 ft above 

base of Rex Member; 12611, from a 7.0-ft calcareous mudstone and argillaceous limestone about 147.0 ft above base 

of Rex Member; 12612, from a 4.3-ft calcareous mudstone 

and argillaceous limestone about 167.0 ft above base of 

Retort Member; 12613, from a 0.8-ft cherty, calcareous and 

very slightly phosphatic mudstone about 210 ft above base 

of Retort Member; 12650, from a 19.7-ft black, calcareous 

mudstone about 9.0 ft above base of Meade Peak Member; 

12651, from a 13.2-ft phosphatic and calcareous mudstone 

about 30.3 ft above base of Meade Peak Member; 12652, 

from a 4.3-ft dense, medium-bedded, hard limestone about 

43.5 ft above base of Meade Peak Member; 12653, from a 

18.0-ft medium-bedded mudstone, calcareous near top, about

61.0 ft above base of Meade Peak Member ; 12654, from a 

9.3-ft mudstone about 80.3 ft above base of Meade Peak 

Member and containing limestone concretions about 7.3 ft 

above base of bed; 12655, from a 14.4-ft phosphatic mudstone containing limestone concretions about 91.4 ft above 

base of Meade Peak Member ; 12656, from a 1.5-ft pisolitic- to 

nodular-phosphate bed about 105.8 ft above base of Meade 

Peak Member ; 12657, from a 1.5-ft argillaceous and slightly 

phosphatic limestone about 105.8 ft above base of Meade 

Peak Member ; 12658, from a float near top of Meade Peak 

Member ; 19531, from limestone of Grandeur Member 10-15 

feet below top.

Johnson Creek, SE% sec. 23, T. 8 S., R. 43 E., Caribou County. 

Colln. 10026-10031 and 10091-10109, by Helmuth Wedow, 

1947, were taken from beds given in TJSGS Circ. 301, p. 32- 

35, as follows : Colln. 10026, from bed P-109 ; 10027, P-110 ; 

10028, P-112; 10029, P-113; 10030, P-114; 10031, P-118; 

10091, P-33 ; 10091, P-33 ; 10092, P-35 ; 10093, P-39 ; 10094, 

P-43; 10095; P-44; 10096, P-55; 10097, P-56; 10098, P-57; 

10099, P-58 ; 10100, P-73 ; 10101, P-77 ; 10102, P-79 ; 10103, 

P-89 ; 10104, P-90 ; 10105, P-91 ; 10106, CW-1 ; 10107, P-21 ; 

10108, P-23 ; 10109, P-38.

Kendall Canyon, sec. 28, T. 7 S., R. 44 E., Caribou County. Colln. 

10452-10484, by J. E. Smedley, 1948, were taken from beds 

given in USGS Circ. 262, p. 20-23, as follows : Colln. 10452, 

from bed CW-5 ; 10453, CW-4 ; 10454, CW-3 ; 10455, CW-2 ; 

10456, P-8; 10457, P-9; 10458, P-10; 10459, P-12; 10460, 

P-13 ; 10461, P-17 ; 10462, P-31 ; 10463, P-34 ; 10464, P-35 ; 

10465, P-37 ; 10466, P-39 ; 10467, P-40 ; 10468, P-41 ; 10469, 

P-43 ; 10470, P-48 ; 10471, P-58 ; 10472, P-61 ; 10473, P-62 ; 

10474, P-69 ; 10475, P-71 ; 10476, P-73 ; 10477, P-78 ; 10478, 

P-79 ; 10479, P-96 ; 10480, P-97 ; 10481, P-98 ; 10482, P-99 ; 

10483, R-2 ; 10484, R-5.

Lone Pine Spring, NE% sec. 4, T. 9 S., R. 45 E., Caribou County. 

Colln. 10993-10999 and 11501-11518, by J. E. Smedley, 1949, 

were taken from beds given in USGS Circ. 304, p. 20-23, 

as follows : Colln. 10993, from bed P-l ; 10994, P-4 ; 10995, 

P-ll ; 10996, P-29 ; 10997, P-31 ; 10998, P-35 ; 10999, P-37 ; 

11501, P-42 ; 11502, P-43 ; 11503, P-44 ; 11504, P-46 ; 11505, 

P-50; 11506, P-52; 11507, P-55; 11508, P-60; 11509, P-61; 

11510, P-73 ; 11511, P-74 ; 11512, P-91 ; 11513, P-105 ; 11514, 

P-108 ; 11515, P-109 ; 11516, P-110 ; 11517, R-l ; 11518, W-l.

Mabie Canyon, NW%NE% sec. 10, T. 8 S., R. 44 E., Caribou 

County. Colln. 10020-10025, 10033-10044, 10049-10061, and 

10117-10118, by Helmuth Wedow, 1947, were taken from 

beds and float given in USGS Circ. 208, p. 14-19, as follows : 

Colln. 10020, from bed 10-14 ft below top of Wells formation ; 10021, CW-1 ; 10022, P-l ; 10023, P-12 ; 10024, P-13 ; 

10025, P-21 ; 10033, P-34 ; 10034, P-45 ; 10035, P-51 ; 10036, 

P-55 ; 10037, P-56 ; 10038, P-57 ; 10039, P-58 ; 10040, P-59 ; 

10041, P-60; 10042, P-61; 10043, P-88; 10044, P-106; 10049, 

P-107; 10050, P-122; 10051, P-145; 1052, P-149; 10053, 

P-154 ; 10054, P-155 ; 1055, P-159-160 ; 10056, P-161 ; 10057, 

P-161; 10058, P-165; 10059, P-168; 10060, P-169; 10061, 

R-2; 10117, from float near top of Meade Peak Member; 

10118, P-112.

Montpelier Canyon, sec. 31, T. 12 S., R. 45 E., Bear Lake County. 

Colln. 9761-9772 and 9977-9990, by Helmuth Wedow, 1947, 

were taken from beds and float given in USGS Circ. 301,
BIOSTRATIGRAPBY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 647

p. 50-58, as follows: Colln. 9761, from bed CW-1; 9762, P-8; 

9763, P-12; 9764, P-167; 9765, P-159; 9766, P-160; 9767, 

P-166; 9768, P-158; 9769, P-151; 9770, P-47; 9771, P-8; 

9772, P-ll; 9977, P-64; 9978, P-96; 9979, P-97; 9980, P-104; 

9981, P-139; 9982, P-141; 9983, R-10; 9984, R-25; 9985, 

R-26; 9986, R-27; 9987, V-12; 9988, Trd-1; 9989, from float 

in Rex Chert Member; 9990, from float in Retort Phosphatic 

Shale Member.

Mud Spring, sec. 7, T. 12 S., R. 29 E., Cassia County. Colln. 12635- 

12642, by H. I. Saunders, 1951, are listed in USGS Circ. 327, 

p. 20-22.

North Dry Valley, sec. 31, T. 7 S., R. 44 E., Caribou County. 

CoUn. 10507-10524, by J. E. Smedley, 1948, were taken from 

beds given in USGS Circ. 262, p. 17-19, as foUows: Colln. 

10507, from bed P-21; 10508, P-23; 10509, P-25; 10510, P-^31; 

10511, P-37; 10512, P-48; 10513, P-61; 10514, P-65; 10515, 

P-69; 10516, P-71; 10517, P-74; 10518, P-82; 10519, P-83; 

10520, P-84; 10521, P-89; 10522, P-98; 10523, P-100; 10524, 

P-101.

North Rasmussen Valley, sec. 6, T. 7 S., R. 44 E., Caribou County. 

Colln. 10441-10451, by J. E. Smedley, 1948, were taken from 

beds given in USGS Circ. 301, p. 10-13, as follows: Colln. 

10441, from bed P-5; 10442, P-22; 10443, P-40; 10444, P-55; 

10445, P-62; 10446, P-77; 10447, P-79; 10448, R-15; 10449, 

R-17; 10450, R-23; 10451, R-24.

North Stewart, NW% sec. 31, T. 8 S., R. 45 E., Caribou County. 

Colln. 11584-11588 were collected by J. E. Smedley, 1949. 

Colln. 11584 was taken from a 6.3-ft brownish-black to black, 

muddy and cherty limestone in Rex Chert Member; 11585, 

from a 44.0-ft bed of alternating dark-gray chert and medium-gray limestone layers in Rex Chert Member; 11586, 

from a 16.0-ft medium- to dark-gray limestone and cherty 

limestone in Rex Chert Member; 11587, from a 10.5-ft chert 

in Rex Chert Member; 11588, from a 18.0-ft cherty and 

argillaceous limestone in Rex Chert Member. All collections 

are thought to be from near middle of Rex Chert Member.

North Wooley Range, sec. 24, T. 6 S., R. 42 E., Caribou County. 

Colln. 10411-10440, by J. E. Smedley, 1948, were taken from 

beds given in USGS Circ. 301, p. 5-7, as follows: Colln. 

10411, from bed CW-1; 10412, P-2; 10413, P-4; 10414, P-10; 

10415, P-12 ; 10416, P-22; 10417, P-31; 10418, P-32; 10419, 

P-34; 10420, P-35; 10421, P-36; 10422, P-47; 10423, P-50; 

10424, P-57; 10425, P-59; 10426, P-61; 10427, P-63; 10428, 

P-65; 10429, P-69; 10430, P-70; 10431, P-72; 10432, P-73; 

10433, P-75; 10434, P-76; 10435, P-79; 10436, P-84; 10437, 

P-85; 10438, P-86; 10439, P-87; 10440, P-88.

Paris Canyon, sec. 8, T. 14 S., R. 43 E., Bear Lake County. 

Colln. 10705-10726, by J. E. Smedley, 1948, were taken from 

beds given in USGS Circ. 262, p. 34-37, as follows: Colln. 

10705, from bed P-8; 10706, P-9; 10707, P-26; 10708, P-28; 

10709, P-29; 10710, P-30; 10711, P-33; 10712, P-36; 10713, 

P-41; 10714, P-43; 10715, P-48; 10716, P-49; 10717, P-50; 

10718, P-55; 10719, P-57; 10720, P-58; 10721, P-59; 10722, 

P-77; 10723, P-79; 10724, P-81; 10725, P-106; 10726, P-116.

Pole Canyon, SW% sec. 31, T. 8 S., R. 46 E., Caribou County. 

Colln. 11564-11583, by J. E. Smedley, 1949, were taken from

beds given in USGS Circ. 304, p. 14-16, as follows: Colln. 

11564 from bed CW-1; 11565, P-l; 11566, P-ll; 11567, P-13; 

11568, P-15; 11569, P-20; 11570, P-24; 11571, P-31; 11572, 

P-34; 11573, P-36; 11574, P-46; 11575, P-49; 11576, P-57; 

11577, P-64; 11578, P-70; 11579, P-72; 11580, P-79; 11581, 

P-81; 11582, P-82; 11583, P-84.

Rocky Canyon, NE% sec. 1, T. 6 S., R. 38 E., Bannock County. 

Colln. 11636-11639, by J. E. Smedley, 1949; 11697-11704, by 

H. W. Peirce, 1949; and 11705-11712, by R. G. Waring, 1949, 

were taken from beds and float given in USGS Circ. 305, 

p. 9-12, as follows: Colln. 11636, from bed P-78; 11637, 

P-27; 11638, P-41; 11639, from limestone float in Rex Chert 

Member; 11697, from Wells Formation; 11698, from bed 

P-l; 11699, P-2; 11700, P-5; 11701, P-41; 11702, P-43; 

11703, P-47; 11704, P-49; 11705, P-66; 11706, P-71; 11707, 

P-79; 11708, P-80; 11709, P-82; 11710, P-83; 11711, P-84; 

11712, P-86.

Snowdrift Mountain, NW%NW% sec. 8, T. 10 S., R. 45 E., Caribou County. Colln. 12582-12598 were collected by J. E. 

Smedley, 1951. Colln. 12583-12595 are listed in USGS Circ. 

327, p. 15-19. In addition, collections were taken from beds 

given in USGS Circ. 327 as follows: Colln. 12582, from bed 

CW-1; 12586, P-5; 12596, P-88?; 12597, from Rex Chert 

Member about 10 ft above base of member; 12598, from Rex 

Chert Member about 60 ft above base of member.

South Dry Valley, NW%SE% sec 14, T. 9 S., R. 44 E., Caribou 

County. Colln. 10045-10048 and 10062-10090, by Helmuth 

Wedow, 1945, were taken from beds given in USGS Circ. 301, 

p. 38-43, as follows: Colln. 10045, from bed CW-1; 10046, 

CW-3; 10047, P-12; 10048, P-16; 10062, P-27; 10063, P-31; 

10064, P-45; 10065, P-47; 10066, P-50; 10067, P-53; 10068, 

P-54; 10069, P-79; 10070, P-81; 10071, P-86; 10072, P-107; 

10073, P-108; 10074, P-110; 10075, P-113; 10076, P-116; 

10077, P-118; 10078, P-122; 10079, P-125; 10080, P-127; 

10081, P-131; 10082, P-148; 10083, P-165; 10084, P-170; 

10085, P-171; 10086, P-172; 10087, P-173; 10088, P-178; 

10089, P-181; 10090, P-182.

South Fork of Sage Creek on north side of South Fork of Sage 

Creek in SW%SE%NW^ sec. 18, T. 9 S., R. 45 E., Stewart 

Flat quadrangle, Caribou County. Colln. 19532, by E. L. 

Yochelson and T. M. Cheney, 1959, was taken from a limestone lens near middle of Rex Chert Member.

South Rasmussen Valley, sec. 9, T. 7 S., R 44 E., Caribou County. 

Colln. 10485-10487, by J. E. Smedley, 1948, were taken from 

beds given in USGS Circ. 301, p. 16-18, as follows: Colln. 

10485, from bed P-5; 10486, P-20; 10487, P-42.

South Stewart Canyon, SE%SE% sec. 31, T. 8 S., R. 45 E., Caribou County. Colln. 11584-11588 and 11520-11546, by J. E. 

Smedley, 1949, were taken from beds given in USGS Circ. 

304, p. 9-13, as follows: Colln. 11520, from beds P-l to P-2; 

11521, P-20; 11522, P-24; 11523, P-27; 11524, P-55; 11525, 

P-56; 11526, P-57; 11527, P-58; 11528, P-59; 11529, P-60; 

11530, P-61; 11531, P-62; 11532, P-74; 11533, P-77; 11534,
648 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

P-78; 11535, P-98; 11536, P-109; 11537, P-124; 11538, 

P-150; 11539, P-151 ; 11540, P-152; 11541, P-156; 11542, 

P-157; 11543, P-158; 11544, P-159; 11545, P-160; 11546, 

P-164.

Swan Lake Gulch, NB%SW% sec. 29, T. 9 S., R. 43 E., Caribou 

County. Colln. 10577-10602, by J. E. Smedley, 1948, were 

taken from beds given in USGS Circ. 208, p. 42-45, as 

follows : Colln. 10577, from bed CW-1 ; 10578, P-4 ; 10579, 

P-7; 10580, P-8; 10581, P-9; 10582, P-31 ; 10583, P-33; 

10584, P-38 ; 10585, P-43 ; 10586, P-45 ; 10587, P-49 ; 10588, 

P-54 ; 10589, P-63 ; 10590, P-72 ; 10591, P-75 ; 10592, P-76 ; 

10593, P-77 ; 10594, P-78 ; 10595, P-81 ; 10596, P-82 ; 10597, 

P-89 ; 10598, P-90 ; 10599, P-92 ; 10600, P-93 ; 10601, P-94 ; 

10602, P-97.

Timber Creek, S% sec. 21, T. 8 S., R. 45 E., Caribou County. 

Colln. 11547-11563, by J. E. Smedley, 1949, were taken from 

beds given in USGS Circ. 304, p. 5-8, as follows: Colln. 

11547, from bed P-l ; 11548, P-3 ; 11549, P-4 ; 11550, P-5 ; 

11551, P-16 ; 11552, P-27 ; 11553, P-33 ; 11554, P-37 ; 11555, 

P-41 ; 11556, P-48 ; 11557, P-56 ; 11558, P-94 ; 11559, P-102 ; 

11560, P-103; 11561, P-104; 11562, P-107; 11563, P-110 to 

P-112.

Trail Canyon, SW%NW%NW% sec. 30, T. 8 S., R. 43 E., Caribou 

County. Colln. 9773-9787, 9922-9925, 9953-9975, 11640, and 

10121, by Helmuth Wedow, 1947, were taken from beds and 

float given in USGS Circ. 301, p. 21-29, as follows : Colln. 

9773, from bed P-13 ; 9774, P-44 ; 9775, P-45 ; 9776, P-50 ; 

9777, P-55 ; 9778, P-67 ; 9779, P-68 ; 9780, P-86 ; 9781, P-92 ; 

9782, P-102 ; 9783, P-124 ; 9784, P-131 ; 9785, P-142 ; 9786, 

P-149 ; 9787, P-165 ; 9922, P-210; 9923, P-205 ; 9924, P-204; 

9925, from float in upper 10 ft of Meade Peak ; 9953, from 

bed R-15; 9954, P-202; 9955, P-201; 9956, P-187; 9957, 

P-186 ; 9958, P-184; 9959, P-183 ; 9960, P-182; 9961, P-181 ; 

9962, P-180; 9963, P-179; 9964, P-174; 9965, P-174; 9966, 

P-173 ; 9967, P-172 ; 9968, P-171 ; 9969, P-170 ; 9970, P-169 ; 

9971, P-168; 9972, P-167; 9973, P-209; 9974, P-199; 9975, 

P-31 ; 10121, P-12 ; 11640, P-179.

Waterloo Phosphate pit, SE^NW^ sec. 6, T. 13 S., R. 45 E., 

Bear County. Colln. 12630-12631, by J. E. Smedley, 1951, 

were taken from float in "cap lime" of Meade Peak Member.

West Dairy, SE. cor. NE^SEM sec. 19, T. 9 S., R. 44 E., Caribou 

County. Colln. 9926-9952 and 9976, by Helmuth Wedow, 

1947, were taken from beds given in USGS Circ. 301, p. 44-49, 

as follows: Colln. 9926, from bed CW-11; 9927, CW-12; 

9928, CW-10; 9929, CW-9 ; 9930, CW-8; 9931, P-l; 9932, 

P-34 ; 9933, P-67 ; 9934, P-78 ; 9935, P-91 ; 9936, P-94 ; 9937, 

P-103; 9938, P-92; 9939, P-29; 9940, R-4; 9941, P-189; 

9942, P-188; 9943, P-187; 9944, P-180; 9945, P-178; 9946, 

P-175 ; 9947, P-150 ; 9948, P-140 ; 9949, P-124 ; 9950, P-122 ; 

9951, P-120 ; 9952, P-117 ; 9976, P-144.

West Georgetown Canyon, SE% sec. 1, T. 10 S., R. 44 E., Bear 

Lake County. Colln. 10565-10576, by J. E. Smedley, 1948, 

were taken from beds given in USGS Circ. 262, p. 27-29, as 

follows: Colln. 10565, from bed P-2; 10566, P-16; 10567, 

P-42; 10568, P-43; 10569, P-46; 10570, P-47; 10571, P-57;

10572, P-58; 10573, P-59; 10574, P-72; 10575, P-82; 10576, 

P-83.

Wolverine Canyon, SE%NW% sec. 31, T. 1 S., R. 39 E., Bingham 

County. Colln. 12109-12115, by J. E. Smedley, 1950, are listed 

in USGS Circ. 327, p. 8-10.

Woodall Creek, NW% sec. 26, T. 7 S., R. 42 E., Caribou County. 

Colln. 10549-10564, by J. E. Smedley, 1948, were taken from 

beds given in USGS Circ. 262, p. 9-12, as follows: Colln. 

10549, in bed CW-3; 10550, P-24; 10551, P-36 ; 10552, P-43; 

10553, P-51; 10554, P-53; 10555, P-55; 10556, P-67; 10557, 

P-68; 10558, P-69; 10559, P-71; 10560, P-73; 10561, P-87 

10562, P-88; 10563, P-89; 10563, P-91.

Montana 

[USGS, U.S. Geological Survey]

Section

No. used 

in circular

1307 

1224 

M-- 

1311 

1359 

1257 

1OK£

1363 

1296- ___

1OOO

1299 

1355 

1249 

1366 

1341 

1294 

1367. _

1358 _ -

1357 

124L ....

1234 

1301 

1246 _ 

1300- _

1302 

Name

Big Timber 

Canyon Creek No. 3. __

Kelley Gulch- . _____

Little Water Canyon. _.._ 

Little Sheep Creek--

North Big Hole Canyon. . 

Sappington Canyon. ___

Sliderock Mountain ___

Warm Springs Creek _ 

West Fork of Blacktail 

Creek.

USGS 

Circular

No.

303 

209

303 

326 

260 

260 

326 

302 

209 

302 

326 

260 

326 

302 

302 

326 

326 

326 

260 

209

303

260 

303 

302

Page

16-17 

25-31

8-10 

18-19 

19-20 

21-22 

26 

20-22 

14-15 5-9 

10-11 

16-18 

16-17 

14-15 

16-20 

9 

20-22 

12-13 

23-26 

16-19

18-20 

28-30 

11-12 

10-12

Collection

11685-11689; 18578-18580 

9901-9921; 18581-18582 

18843 

11682-11684 

12694 

10832-10836 

10824-10829 

12695 

11690-11694 

9788-9799; 9900 

11673-11680 

12693 

10830-10831 

12696 

12297-12307 

11641-11652, 11655-11663 

12699 

12692; 18583-18584 

12697; 18587-18589 

10851-10857 

11713-11715; 10891-10909; 

10807; 10823; 18573-18575 

11671-11672 

10837-10850 

11681 

11664-11670; 18576-18577

Alpine Creek, N1^ sec. 26, T. 10 S., R. 2 W., Madison County, 

Colln. 11685-11689, by W. R. Record, 1949, and 11578-18580, 

by E. L. Yochelson and E. R. Cressman, 1959, are listed in 

USGS Prof. Paper 313-C, p. 506-509. Also, Colln. 11685-11689 

are listed in USGS Circ. 303, p. 16-17.

Big Timber, sec. 23, T. 5 S., R. 12 E., Snodgrass County. Colln. 

18843 were collected by E. L. Yochelson and R. W. Swanson, 

1959, from dip slope on west side of road cut 0.6 mile north 

of Gallatin Forest entrance in upper part of Shedhorn 

Sandstone.

Big Sheep Canyon, sec. 26, 25 and 11, T. 14 S., R. 10 W., Beaverhead County. Colln. 9901-9921, by Helmuth Wedow, 1947, 

and 18581-18582, by E. L. Yochelson and E. R. Cressman, 

1959, are listed in USGS Prof. Paper 313-C, p. 414-425. 

Also, the section, but not position of collections, is given in 

USGS Circ. 209, p. 25-31.

Canyon Carnp, NE% sec. 18, T. 9 S., R. 3 W., Madison County. 

Colln. 11682-11685, by W. R. Record, 1949, are listed in
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 649

USGS Prof. Paper 313-B, p. 509-513. Also, collections are 

listed in USGS Circ. 303, p. 8-10.

Canyon Creek No. 3, NW^ sec. 13, T. 2 S., R. 10 W., Beaverhead 

County. Colln. 12694, collected by J. A. Peterson, 1951, is 

listed in USGS Circ. 326, p. 18-19.

Cave Creek, NW^NW^ sec. 10, T. 6 S., R. 10 W., Beaverhead 

County. Colln. 10832-10836, by K. P. McLaughlin, 1948, are 

listed in USGS Prof. Paper 313-C, p. 473-475. Also, the 

section, but not the position of the collections, is given in 

USGS Circ. 260, p. 19-20.

Cedar Creek, sec. 26, T. 9 S., R. 11 W., Beaverhead County. 

Colln. 10824-10829, by K. P. McLaughlin, 1948, are listed in 

USGS Prof. Paper 313-C, p. 470-473. Also, the section, but 

not the position of the collections is given in USGS Circ. 260, 

p. 21-22.

Cinnabar Mountain, sec. 31, T. 8 S., R. 8 E., Park County. Colln. 

12695, by J. A. Peterson, 1951, is listed in USGS Prof. Paper 

313-C, p. 547-548, and in USGS Circ. 326, p. 26. Colln. 18844, 

by E. L. Yochelson and R. W. Swanson, 1959, is listed in 

USGS Prof. Paper 313-C, p. 547.

Crooked Creek, SW% sec. 1, T. 15 S., R. 8 W., Beaverhead 

County. Colln. 11690-11694, by W. R. Record, 1949, are 

listed in USGS Circ. 302, p. 20-22.

Dalys Spur, SW%SW% sec. 36, T. 8 S., R. 10 W., Beaverhead 

County. Colln. 9788-9799 and 9900, by Helmuth Wedow, 

1947, are listed in USGS Prof. Paper 313-C, p. 408-413. Also, 

section, but not position of collections, is listed in USGS 

Circ. 209, p. 14-15.

Hogback Mountain, S%NW% sec. 8, T. 11 S., R. 4 W., Madison 

County. Colln. 11673-11680, by W. R. Record, 1949, are listed 

in USGS Prof. Paper 313-C, p. 486-494. Also, collections are 

listed in USGS Circ. 302, p. 5-9.

Jefferson Canyon, SE% sec. 13, T. 1 N., R. 3 W., Madison County. 

CoUn. 12693, by J. A. Peterson, 1951, is listed in USGS Circ. 

326, p. 10-11.

Kelley Gulch, sec. 2, T. 6 S., R. 11 W., Beaverhead County. Colln. 

10830-10831, by K. P. McLaughlin, 1948, are listed in USGS 

Prof. Paper 313-C, p. 457-460. Also, section, but not position 

of collections, is listed in USGS Circ. 260, p. 16-18.

La Marche Gulch, sec. 32, T. 1 S., R. 9 W., Beaverhead County. 

Colln. 12696, by J. A. Peterson, 1951, is listed in USGS Circ. 

326, p. 16-17.

Little Water Canyon, SE% sec. 4, T. 13 S., R 10 W., Beaverhead 

County. Colln. 12297-12307, by J. E. Smedley, 1950, are 

listed in USGS Prof. Paper 313-C, p. 519-523.

Little Sheep Creek, SW% sec. 34, T. 14 S., R. 9 W., Beaverhead 

County. Colln. 11641-11653 and 11656-11663, by W. R. 

Record, 1949, are listed in USGS Prof. Paper 313-C, p. 476- 

481. Also, collections are listed in USGS Circ. 302, p. 16-20.

Logan, sec. 26, T. 2 N., R. 2 E., GaUatin County. Colln. 12699, by 

J. A. Peterson, 1951, is listed in USGS Circ. 326, p. 9.

North Big Hole Canyon, NE% sec. 3, T. 5 S., R. 8 W., Madison 

County. Colln. 12692, by J. A. Peterson, 1951, and colln. 

18584, by E. L. Yochelson and R. W. Swanson, 1959, are 

listed in USGS Prof. Paper 313-C, p. 537-540. Also, colln. 

12692 is listed in USGS Circ. 326, p. 20-22.

Sappington Canyon, sec. 25, T. 1 N., R. 2 W., Gallatin County. 

Colln. 12697 was collected by J. A. Peterson, 1951, and 

18587-18589, by E. L. Yochelson and R. W. Swanson, 1959. 

Colln. 12697 is listed in USGS Circ. 326, p. 12-13. Colln. 

18587 was taken from phosphate sandstone near base of 

upper member of Shedhorn Sandstone; 18588, from upper 

member of Shedhorn Sandstone, 2 ft above base; 18589, 

from upper member of Shedhorn Sandstone, 5-6 ft above 

base.

Sawtooth Mountain, NE^SW^i sec. 10, T. 12 S., R. 5 W., 

Beaverhead County. Colln. 10851-10857 are listed in USGS 

Prof. Paper 313-C, p. 444-449. Also, section, but not position of collections, is given in USGS Circ. 260, p. 23-26.

Sheep Creek, NW%SW% sec. 23, T. 9 S., R. 9 W., Beaverhead 

County. Colln. 10807-10823, by K. P. McLaughlin, 1948; 

11713-11715 and 10891-10909, by J. E. Smedley, 1949 ; and 

18573-18575, by E. L. Yochelson and E. R. Cressman, 1959, 

are listed in USGS Prof. Paper 313-C, p. 426-438. Also, colln. 

10807-10823, 11713-11715, and 10891-10909 were taken from 

beds given in USGS Circ. 209, p. 16-19, as follows : Colln. 

10807 from bed 0.9 ft above base of Grandeur Member; 

10808, 1.8 ft above base of Grandeur Member ; 10809, 3.0 ft 

above base of Grandeur Member; 11713, C-l; 11714, C-2; 

10810, C-3; 11715, C-5; 10891, C-6; 10811, C-12; 10812, 

D-l; 10892, D-4; 10893, D-5 to D-9; 10813, D-10; 10895, 

D-11-; 10896, D-ll ; 10814, D-12 ; 10815, D-15; 10897, D-17 ; 

10898, D-20; 10816, D-20; 10899, D-21; 10900, D-22; 

10901, D-23 ; 10902, D-24 to D-27 ; 10817, D-27 ; 10903, D-30 ; 

10904, D-42 ; 10905, D-43 ; 10906, D-44 ; 10907, D-45 ; 10818, 

D-45; 10819, D-46; 10908, D-46; 10909, D-47; 10820, D-47; 

10821, E-l ; 10822, E-8 ; 10823, E-ll.

Sliderock Mountain, N% sec. 25, T. 10 S., R. 4 W., Madison 

County. Colln. 11671-11672, by W. R. Record, 1949, are listed 

in USGS Prof. Paper 313-C, p. 496-500. Also, collections are 

listed in USGS Circ. 303, p, 18-20.

Wadhams Spring, sec. 22 and 28, T. 13 S., R. 7 W., Beaverhead 

County. Colln. 10837-10850, by K. P. McLaughlin, 1948, are 

listed in USGS Prof. Paper 313-O, p. 450-457. Also, section, 

but not position of collections, is given in USGS Circ. 260, 

p. 28-30.

Warm Springs Creek, NW^ sec. 22, T. 9 S., R. 3 W., Madison 

County. Colln. 11681, by W. R. Record, 1949, 11681 is listed 

in USGS Circ. 303, p. 11-12.

West Fork of Blacktail Creek, SE% sec. 26, T. 12 S.t R. 6 W., 

Beaverhead County. Colln. 11664-11670, by W. R. Record, 

1949, and 18576-18577, by E. L. Yochelson and E. R. Cressman, 1959, are listed in USGS Prof. Paper 313-C, p. 500- 

505. Also, colln. 11664-11670 are listed in USGS Circ. 302, 

p. 10-12.
650 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

Utah 

[USGS, U.S. Geological Survey]

Section

No. used 

in circular

G. 

F__ __ 

1203.. _ 

1219...- _ .

C _ .

H. 

A 

1345. 

B 

1229.. _ ...

1350. .

1347. 

E

1339

1235 

1290.. 

1221 

D.

19Q9

1271. _ .

t99f»

J .. 

1371.. 

1228.. 

1270. ...

1231.... ....

Name

Bennett Ranch..... _

Cephalopod Gulch ____

Franson (Pinyon) Canyon.

Laketown Canyon _ . ...

Little Brush Creek. ___

Mill Creek. 

Bight Fork of Hobble 

Creek.

Upper Brazer Canyon .....

Wolf Creek. 

USGS 

Circular

No.

211 

211

306

211 

306 

306

306 

211 

306 

211

306 

211

211

306 

211 

211 

211

Page

5-10 

35

11-17

29-30 

25-31 

18-21

22-24 

31-32 5-6 

36

7-10

37-41

33-34

35-39 

21-24 

42-47 

25-26

Collection

19402 

10803-10806; 19408-19409 

10110-10116; 10119-10120; 

10730-10754; 15014, 19414 

10000-10001, 19405 

18890-18891; 18076-18077 

10018; 19406 

16710 

12478-12488 ',19411 ,19412 

19415 

10790-10795 

12502-12529 

12489-12501

12627 

19403, 19404; 12270-12287 

10796-10802 

10959-10965 

10012-10018 

17657, 19413 

10966-10985 

10654-10704; 12623-12624

9991-9999 

19407 

12669-12691 

10755-10780 

10603-10653 

10781-10789

Bennett Ranch, west side Sheep Creek, 9.8 miles south of Manila 

on Utah Highway No. 44, Daggett County. Colln. 19402, by 

E. L. Yochelson and T. M. Cheney, 1959, was taken from 

limestone in Grandeur Member 3 ft above top of Weber 

Sandstone.

Blind Stream, SW%SW% sec. 14, T. 1 N., R. 8 W., Duchesne 

County. Collns. 10803-10806 were collected by K. P. McLaughlin, 1948; 19408-19409, by E. L. Yochelson and T. M. 

Cheney, 1959. Colln. 10803 was taken from Meade Park Phosphatic Shale Member at middle of 4.5-f t sandstone, the basal 

bed of Meade Peak Member; 10804, from top of 4.5-ft basal 

sandstone of Meade Peak Member; 10805, from a 0.2-ft 

oolitic phosphate bed 5.5 ft above base of Meade Peak Member; 10806, from a 1.9-ft dolomitic limestone 10.5 ft above 

base of Meade Peak Member; 19408, from limestone in upper 

part of lower part of Franson Member 5 ft below top of cliff; 

19409, from Mackentire Tongue, of Williams (1939), of 

Woodside Formation as used by Thomas (1939), from a 

50- to 60-ft interval of shale and limestone about 200 ft above 

cliffs formed by Franson Member.

Brazer Canyon, NW^L sec. 9, T. 11 N., R. 8 E., Rich County. 

Collns. 10110-10116 and 10119-10120 were collected by Helmuth Wedow, 1947; 10730-10754, by J. E. Smedley, 1948; 

15014, by Helen Duncan, 1954; and 19414, by E. L. Yochelson, 

1959. Collns. 10110-10116 and 10119-10120 are listed in 

USGS Circ. 211, pp. 5-10. Also, Collections were taken from 

beds given in USGS Circ. 211, as follows: Colln. 10730, from 

bed P-17; 10731, P-19; 10732, P-20, P-21; 10733, P-36; 

10734, P-37; 10735, P-42; 10736, P-58; 10737, P-64; 10738, 

P-70; 10739, P-83; 10740, P-91; 10741, P-138; 10742, P-139; 

10743, R-3; 10744, R-3; 10745, R-8; 10746, R-12; 10747, R14; 10748, R-15; 10749, R-18; 10750, R-20; 10751, R-20;

10752, R-35; 10753, R-35; 10754, R-35. Colln. 15014 was 

taken from the upper part of the Franson Member ; colln. 

19414, from the Grandeur Member about 25 ft above base 

of member.

Brush Creek Gorge, SW&NW% sec. 32, T. 2 S., R. 22 E., Uintah 

County, Collns. 10000-10011, by Helmuth Wedow, 1947, and 

19405, by E. L. Yochelson and T. M. Cheney, were taken 

from beds given in USGS Circ. 211, p. 35, as follows : Colln. 

10000, from bed P-5 ; 10001, P-10 ; 10002, P-13 ; 10003, P-14 ; 

10004, P-15 ; 10005, P-17 ; 10006, P-18 ; 10007, P-19 ; 10008, 

P-20; 10009, P-21; 10010, P-22; 10011, P-25. Also, colln. 

19405 was taken from the lower part of Franson Member 

about 10 ft below base of Mackentire Tongue, of Williams 

(1939), of the Woodside Formation as used by Thomas 

(1939).

Cephalopod Gulch, NW&SW&SW^ sec. 27, T. 1 N., R. 1 E., 

Salt Lake County. Colln. 18076-18077 were collected by 

T. M. Cheney, 1958 ; and 18890-18891, by E. L. Yochelson and 

T. M. Cheney, 1959. Colln. 18076 was taken from lowest 

exposed beds of Grandeur Member ; 18077, Grandeur Member 15 ft above 18076; 18890 (re-collection of 18077) ; 18891, 

uppermost bed in Franson Member 20 yd down canyon from 

18890.

Coulter Ranger Station, wya sec. 12, T. 2 S., R. 21 E. Uintah 

County. Colln. 10019, by Helmuth Wedow, 1947, and 19406, 

E. L. Yochelson and T. M. Cheney, 1959, were taken from 

Franson Member, a fine-grained calcareous sandstone about 

50 ft above the base of Park City Formation.

Crawford Mountain, SW% sec. 5, T. 11 N., R. 8 E (SLM), Rich 

County. Colln. 16710 was collected by W. C. Gere, 1955, from 

Rex Chert Member near middle of section. (Collection is 

probably from Franson Member rather than the Rex).

Devils Slide, NW% sec. 26, T. 4 N., R. 3 E., Morgan County. 

Colln. 12478-12488, by J. E. Smedley, are listed in USGS 

Circ. 306, p. 11-17. Colln. 19411 and 19412 were collected by 

E. L. Yochelson and T. M. Cheney, 1959, Colln. 19411 was 

taken from uppermost beds of Grandeur Member 50 ft above 

base of member.

Dry Bread Hollow, sec. 14, T. 7 N., R. 3 E., Weber County, about 

300 ft above floor of Canyon. Colln. 19415, by T. M. Cheney, 

1959, was taken from Franson Member.

Dry Canyon, S%SW% sec. 3, T. 1 N., R. 6 W., Duchesne County. 

Colln. 10790-10795, by K. P. McLaughlin, 1948, correspond 

to field numbers 48-KPM-3 to 48-KPM-8 found in USGS 

Circ. 211, p. 29-30.

Fort Douglas, E%NE% sec. 17, T. 1 N., R. 2 E., Salt Lake 

County. Colln. 12502-12510 and 12513-12514 were collected 

by J. E. Smedley, 1951 ; 12511-12512, by J. E. Smedley and 

H. I. Saunders, 1951 ; and 12515-12529, by H. I. Saunders, 

1951. Colln. 12502-12514 and 12517-12528 are listed in USGS 

Circ. 306, p. 18-21. Also, the following collections were 

taken from beds and float given in USGS Circ. 306, p. 18-21,
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 651

as follows: Colln. 12515, from bed L-19; 12516, L-19; 

12529, from float 225 ft stratigraphically above bed M-242.

Franson (Pinyon) Canyon, sec. 17, T. 1 S., R. 6 E., Summit 

County. Colln. 12489-12500, by J. E. Smedley, 1951, are listed 

in 1}SGS Circ. 306, p. 18-21. Colln. 12501, by J. E. Smedley 

and R. L. Swanson, 1951, was taken from float near top of 

Franson Member.

Geneva Steel Co. pit, on ridge between Little Diamond and 

Wanrhodes Creeks, Wasatch National Forest. Colln. 12627 

was collected by R. G. Waring, 1951, from Meade Peak 

Member.

Horseshpe Canyon, sec. 36, T. 3 N., R. 20 E., Daggett County. 

Colln. 12270-12287 were collected by J. E. Smedley, 1950; 

and 19403-19404, by E. L. Yochelson and T. M. Cheney, 1959. 

Colln. 12270-12287 are listed in USGS Circ. 306, p. 22-24. 

Colln. 19403 was taken from approximately the same bed 

as 12270; 19404, from approximately the same bed as 12284.

Lake Foyk, NE%NW% sec. 34, T. 2 N., R. 5 W., Duchesne County. 

Collin. 10796-10802, by K. P. McLaughlin, 1948, correspond to 

field numbers 48-KPM-9 to 48-KPM-15 listed in USGS Circ. 

211.

Laketowrn Canyon, sec. 32, T. 13 N., R. 6 E., Rich County. Colln. 

10959-10965, by J. E. Smedley, 1949, were taken from beds 

given in USGS Circ. 306, p. 5-6, as follows: Colln. 10959, 

from beds P-18, P-19; 10960, P-28; 10961, P-2; 10962, P-7; 

109^3, P-15; 10964, P-50; 10965, R-l.

Little Brush Creek, NW%SE% sec. 22, T. 2 S., R. 22 E., Uintah 

County. Colln. 10012-10018, by Helmuth Wedow, 1947, were 

taken from beds given in USGS Circ. 211, p. 36, as follows: 

Colln. 10012, from bed P-8; 10013, P-14; 10014, P-16; 10015, 

P-18; 10016, P-19; 10017, P-20; 10018, P-22.

Mill Creek, sec. 36, T. 1 S., R. 1 E., on the north side and near 

the mouth of Mill Creek Canyon, Salt Lake County. Colln. 

17657 was collected by Katherine Dennison and T. M. 

Chepey, 1955, from Grandeur Member; colln. 19413, by E. L. 

Yochelson and T. M. Cheney, 1959, 30 ft from top of upper 

part of Franson Member.

North Crawford, NE}4NE%, sec. 32, T. 12 N., R. 8 E., Rich 

County. Colln. 10966-10985, by J. E. Smedley, 1949, were 

taken from beds given in USGS Circ. 306, p. 7-10, as follows: 

Colln. 10966, from bed OW-1; 10967, CW-1; 10968, P-l; 

10969, P-2; 10970, P-ll; 10971, P-14; 10972, P-23; 10973, 

P-23; 10974, P-26; 10975, P-52; 10976, P-54; 10977, P-61; 

10978, P-72; 10979, P-77; 10980, P-81; 10981, P-85; 10982, 

P-86; 10983, P-88; 10984, P-91; 10985, P-102.

Right Efork of Hobble Creek, sec. 19(?), T. 7 S., R. 5 E., Utah 

County. Colln. 10654-10701, by J. E. Smedley, 1948, and 

12623-12624, by J. E. Smedley, 1950, were taken from beds 

given in USGS Circ. 211, p. 37-41, as follows: Colln. 10654, 

from bed L-l; 10655, P-2; 10656, P-3; 10657, P-4; 10658,

P-5; 10659, P-8; 10660, P-9; 10661, P-12; 10662, P-13; 

10663, P-14; 10664, P-33; 10665, P-30; 1066, P-36; 10667, 

P-37; 10668, P-38; 10869, P-41; 10670, P-44; 10671, P-45; 

10672, P-47; 10673, P-55; 10674, P-60; 10675, P-66; 10676, 

P-67; 10677, P-69; 10678, P-70; 10679, P-71; 10680, P-76; 

10681, P-77; 10682, P-78; 10683, P-81; 10684, P-82; 10685, 

P-83; 10686, P-90; 10687, P-91; 10688, P-92; 10689, P-95; 

10690, P-98; 10691, P-99; 10692, P-100; 10693, P-101; 10694, 

P-102; 10695, P-103; 10696, P-104; 10697, P-105; 10698, 

P-106; 10699, P-107; 10700, P-120; 10701, P-123; 10702, 

P-124; 10703, P-125; 10704, P-144; 12623, above upper shale 

member, "upper part of Franson"; 12624, bed P-44 or P-45.

Rock Canyon, SW%SE%, sec. 6, T. 3 S., R. 21 E., Uintah County. 

Colln. 9991-9999, by Helmuth Wedow, 1947, were taken from 

beds given in USGS Circ. 211, p. 33-34, as follows: Colln. 

9991, from bed P-l; 9992, P-2; 9993, P-5; 9994, P-15; 9995, 

P-18; 9996, P-23; 9997, P-24; 9998, P-25; 9999, P-26.

Split Mountain, Split Mountain Gorge on north side of gully 

about 100 yd west and up from camp grounds in Dinosaur 

National Monument. Colln. 19407 was collected by E. L. 

Yochelson and T. M. Cheney, 1959 from lower part of 

Franson Member on dip slope.

Strawberry Valley, NW% sec. 14, T. 2 S., R. 12 W., Wasatch 

County. Colln. 12669-12691, by J. E. Smedley, 1951, were 

taken from beds given in USGS Circ. 306, p. 35-39, as follows : Colln. 12669, from bed U-17; 12670, U-17; 12671, U-6; 

12672, P-74 to P-71; 12673, P-69; 12674, P-34; 12675, P-31; 

12676, P-30; 12677, P-27; 12678, P-24; 12679, L-21; 12680, 

L-23; 12681, L-24; 12682, L-25; 12683, L-26; 12684, L-38; 

12685, L-42; 12686, L-46; 12687, L-48; 12688, L-49; 12689, 

P-22; 12690, U-4; 12691, P-16.

Upper Brazer Canyon, sec. 30, T. 11 N., R. 8 E., Rich County. 

Colln. 10755-10780, by J. E. Smedley, 1948, correspond to 

field numbers listed 48-JES-23 to 48-JES-48 in USGS 

Circ. 211, p. 21-24.

Wanrhodes Canyon, sec. 22, T. 8 S., R. 4 E., Utah County. Colln. 

10603-10653, by J. E. Smedley, 1948, were taken from beds 

given in USGS Circ. 211, p. 42-47, as follows: Colln. 10603, 

from bed L-l; 10604, P-3; 10605, P-4; 10606, P-5; 10607, 

P-6; 10608, P-7; 10609, P-8; 10610, P-10; 10611, P-ll; 

10612, P-12; 10613, P-14; 10614, P-15; 10615, P-17; 10816, 

P-20; 10617, P-32; 10618, P-58; 10619, P-64; 10620, P-65; 

10621, P-66; 10622, P-69; 10623, P-73; 10624, P-74; 10625, 

P-75; 10626, P-76; 10627, P-77; 10628, P-79 ; 10629, P-82; 

10630, P-83; 10631, P-85; 10632, P-86; 10633, P-87; 10634, 

P-88; 10635, P-91; 10636, P-93; 10637, P-95; 10638, P-97; 

10639, P-102; 10640, P-104; 10641, P-123; 10642, P-151; 

10643, P-172; 10644, P-175; 10645, P-182; 10646, P-183; 

10647, P-187; 10648, P-192; 10649, P-198; 10650, P-199; 

10651, P-205; 10652, P-208; 10653, P-217.

Wolf Creek, NE%SE% sec. 20, T. 1 N., R. 9 W., Wasatch County. 

Colln. 10781-10789, by K. P. McLaughlin, 1948, were taken 

from beds given in USGS Circ. 211, p. 25-26, as follows: 

Colln. 10781, from bed P-2; 10782, P-3; 10783, P-6; 10784, 

P-ll; 10785, P-26; 10786, P-28; 10787, P-30; 10788, P-35; 

10789, U-4.
652 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

Wyoming 

[USGS, U.S. Geological Survey]

Section

No. used 

in circular

1334.......

1381 ....

1332.......

1328 

1329 

1201 

1289- ...

1330.......

1323 

1346 

1380 

1325 __

1335 

1369 

1379- 

1326 

1324- ...

1375 

1202......

1205- ...

1204. _ ...

1331 

1368 

1336 

1352 

1370 

1327 

1333 

1378 

Name

Burroughs Creek. ..

Deadline Bidge.- 

Dinwoody Lakes. .. 

Flat Creek ___ ...

Fontenelle Creek ... 

Gros Ventre Slide _

Hungry Creek. ..... 

Layland Canyon __ 

Middle Fork of Pine 

Creek.

North Fork of Pine 

Creek

South Fork of Gypsum Creek.

Togwotee Pass ...... 

Tosi Creek-. 

USGS 

Circular

No.

307 

325

307 

307

307 

210

307

307 

324

324

325

307 

307

324

325 

307 

307 

324 

210 

210

210

307 

324 

307

324

324 

307 

307 

325

Page

30 

15-18

25-25 

31-34

7-9 

11-15

41-45

35-36 

11-13

20-22 8-10

16-17 

13-15

7-8

11-14 

10-12 

21-23 

9-10 5-8 

28-31

24-26

37-39 5-6 

26-29

17-19 

14-16 5-6 

18-20 

20-22

Section 

no. used 

in USGS 

Prof. 

Paper 

313-B

66

60 

82

68

124 

44

147

107

75 

50

4

108 

42 

57 

47

2

79

67 

49 

41 

56 

110

Collection

22114-12220 

13300-13312; 10032; 

18898 

12145-12151; 12632 

12248-12269; 18601- 

18604 

12179-12200 

12614-12619; 9733-9734; 

9741-9748; 18896 

10923-10954; 12470- 

12472 

1228-12235 

12116-12124; 12537- 

12545 

12561-12573 

13342-13349; 18632- 

18633 

12152-12178; 18605 

12221-12227; 12628- 

12629 

12554-12560; 18596- 

18598 

13325-13341 

12125-12136 

12137-12144; 12622 

12659-12668 

9754-9760 

9712-9713; 9721-9732; 

9735-9739; 18842- 

18897 

9714-9720; 9740; 9750- 

9753 

12308-12316 

12546-12553, 18593 

12236-12247

12643-12649 

12574-12581 

18859-18860 

12201-12213 

13313-13324

Bartlett Creek, sec. 23, T. 38 N., R. Ill W., Sublette County. 

Colln. 12214-12220, by J. E. Smedley, 1950, are listed in 

USGS Prof. Paper 313-B, p. 212-213. Also, collections are 

listed in USGS Circ. 307, p. 30.

Basin Creek, sees. 12 and 13, T. 26 N., R. 117% W., Lincoln 

County. Colln. 10032 were collected by Helmuth Wedow, 

1947; 13300-13312, by J. E. Smedley, 1952; and 18898, by 

E. L. Yochelson, J. T. Dutro, Jr. and T. M. Cheney, 1959. 

Section, but not position of collections, is given in USGS 

Circ. 325, p. 15-18.

Buck Creek, SW%SE% sec. 1, T. 38 N., R. 115 W., Teton County. 

Colln. 12145-12151, by J. E. Smedley, 1950, and 12632, by 

J. E. Smedley, 1951, are listed in USGS Prof. Paper 313-B, 

p. 208-210. Also, collections are listed in USGS Circ. 307, 

p. 24-25.

Bull Lake, sec. 6, T. 2 N., R. 3 W., Fremont County. Colln. 12248- 

12269, by J. E. Smedley, 1950, are listed in USGS Prof. Paper 

313-B, p. 229-234. Also, collections are listed in USGS Circ. 

307, p. 31-34.

Burroughs Creek, NE*4 sec. 14, T. 43 N., R. 107 W., Fremont 

County. Colln. 12179-12200, by J. E. Smedley, 1950, are listed 

in USGS Prof. Paper 313-B, p. 217-220. Also, collections are 

listed in USGS Circ. 307, p. 7-9.

Coal Canyon, sec. 7, T. 26 N., R. 119 W., Lincoln County. Colln. 

9733-9734 and 9741-9748, by Helmuth Wedow, 1947; 12614- 

12618, by J. E. Smedley, 1951; and 18896, by E. L. Yochelson

and J. T. Dutro, Jr., 1959, were taken from beds and float 

given in USGS Circ. 210, p. 11-15, as follows: Colln. 9733 

from float in beds P-67 to 74; 9734, from bed P-68; 9741, 

P-75; 9742, P-81; 9743, P-98; 9744, P-99; 9745, P-104; 

9746, R-l; 9747, R-3; 9748, U-16; 12614, U-7; 12615, U-12; 

12616, U-15; 12617, U-21 to 22; 12618, R-5, R-6, R-7; 18896, 

from calcareous mudstone in Meade Peak Member.

Cokeville; NE%NW% sec. 4, T. 24 N., R. 119 W., Lincoln County. 

Colln. 10923-10954, by J. E. Smedley, 1949, and 12470-12472, 

by J. E. Smedley, 1951, were taken from beds given in USGS

Circ. 307, p. 41-45, as follows 

10924, P-144; 10925, P-143; 

10929, P-134: 

10933, P-117 

10937, P-191 

10941, P-146

10928, P-135 

10932, P-127 

10936, P-193 

10940, P-145 

10944, P-lll 

10948, P-176

Colln. 10923, from bed P-145; 

10926, P-143; 10927, P-136;

10931, P-129;

10935, P-194;

10939,

10943,

10930, P-133; 

10934, P-116; 

10938, P-190; 

10942, P-148; 

P-31; 10946, P-171; 

10950, P-162;

10947,

P-188; 

P-112; 

P-174;

10951, P-164;

10945,

10949, P-178;

10952, P-166; 10953, P-167; 10954, P-160 ; 12470, P-148. 

Colln. 12471 and 12472 were taken near old phosphate mill 

from outcrops identified in the field as Rex Chert Member, 

here called Franson Member.

Conant Creek, S%SE% sec. 31, T. 33 N., R. 93 W., Fremont 

County. Colln. 12228-12235, by J. E. Smedley, 1950, are listed 

in USGS Prof. Paper 313-B, p. 258-260. Also, collections are 

listed in USGS Circ. 307, p. 35-36.

Crystal Creek, S^NW% sec. 34, T. 42 N., R. 113 W., Teton 

County. Colln. 12116-12124, by J. E. Smedley, 1950, and 

12537-12545, by J. E. Smedley, 1951, are listed in USGS 

Prof. Paper 313-B, p. 184-187. Also, collections are listed in 

USGS Circ. 324, p. 11-13.

Cumberland, SW%NEi/4 sec. 19, T. 19 N., R. 117 W., Lincoln 

County. Colln. 12561-12573, by J. E. Smedley, 1951, are listed 

in USGS Prof. Paper 313-B, p. 263-266. Also, collections are 

listed in USGS Circ. 324, p. 20-22.

Deadline Ridge, sec. 7, T. 27 N., R. 114 W., Lincoln County. 

Colln. 13342-13349, J. E. Smedley, 1952, and 18632-18633, 

by E. L. Yochelson and T. M. Cheney, 1959, are listed in 

USGS Prof. Paper 313-B, p. 250-253.

Dinwoody Lakes, SW%SW% sec. 6, T. 4 N., R. 5 W., Fremont 

County. Colln. 12152-12178, by J. E. Smedley, 1950, and 

18605, by E. L. Yochelson and R. P. Sheldon, 1959, are listed 

in USGS Prof. Paper 313-B, p. 221-224. Also, collections 

12152-12178 are listed in USGS Circ. 307, p. 16-17.

Flat Creek, sec. 1, T. 41 N., R. 115 W., Teton County. Colln. 

12221-12227, by J. E. Smedley, 1950, and 12628-12629, by 

J. E. Smedley, 1951, are listed in USGS Prof. Paper 313-B, 

p. 192-198. Also, collections are listed in USGS Circ. 307, 

p. 13-15.

Forellen Peak, south slope of Forellen Peak in northern part of 

Grand Teton National Park. Colln. 12554-12560, by J. E. 

Smedley, 1951, and 18596-18598, by E. L. Yochelson and 

R. P. Sheldon, 1959, are listed in USGS Prof. Paper 313-B, 

p. 162-164. Also, colln. 12554-12560 are listed in USGS Circ. 

324, p. 7-8.
BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 653

Fontenelle Creek, sec. 35, T. 27 N., R. 116 W., Lincoln County. 

Collri. 13325-13341, J. E. Smedley, 1952, are listed in USGS 

Prof j Paper 313-B, p. 245-250. Section, but not position of 

collections, is given in USGS Circ. 325, p. 11-14.

Gros Ventre Slide, SE% sec. 5, T. 42 N., R. 114 W., Teton County. 

Colln. 12125-12136, by J. E. Smedley, 1950, are listed in 

USGS Prof. Paper 313-B, p. 181-184. Also, collections are 

listed in USGS Circ. 307, p. 10-12.

Hoback, SW%NE% sec. 33, T. 39 N., R. 117 W., Teton County. 

Colln. 12137-12144, by J. E. Smedley, 1950, and 12622, by 

J. E.| Smedley, 1951, are listed in USGS Prof. Paper 313-B, 

p. 204-207. Also, collections are listed in USGS Circ. 307, 

p. 211-23.

Hungry Creek, sec. 97, T. 41 N., R. 118 W., Teton County. CoUn. 

1265^-12668, by H. I. Saunders, 1951, are listed in USGS 

Prof Paper 313-B, p. 188-189. Also, collections are listed in 

USQS Circ. 324, p. 9-10.

Layland Canyon, sec. 30, T. 27 N., R. 119 W., Lincoln County. 

Colin. 9754-9760, by Helmuth Wedow, 1947, were taken 

froni beds given in USGS Circ. 210, p. 5-8, as follows: Colln. 

9754^ from bed, P-86; 9755, P-83; 9756, P-83; 9757, P-75; 

9758, P-66; 9759, P-63; 9760, P-l.

Middle Fork of Pine Creek, sec. 35, T. 25 N., R. 118 W., Lincoln 

County. Colln. 9712-9713, 9721-9732, and 9735-9739, by Helmuth Wedow, 1947, and 18842 and 18897, by E. L. Yochelson 

and R. P. Sheldon, 1959, were taken from beds and float 

given in USGS Circ. 210, p. 28-31, as follows: Colln. 9712, 

fronf bed P-l; 9713, P-15; 9721, P-59; 9722, R-13; 9723, 

R-13; 9724, R-15; 9725, R-16; 9726, R-17; 9727, R-26; 

972$, U-l; 9729, U-30; 9730, from Dinwoody Formation; 

973|, from float above Meade Peak Member; 9732, from bed 

R-2£; 9735, R-23; 9736, R-21; 9737, R-20; 9738, R-18; 

9739^, R-18; 18842, from upper part of Franson Member; 

18807, from uppermost phosphate unit just below Dinwoody 

Formation.

North Fork of Pine Creek, sec. 13, T. 25 N., R. 118 W., Lincoln 

County. Colln. 9714-9720, 9740, and 9750-9753, by Helmuth 

Wedow, 1947, were taken from beds given in USGS Circ. 210, 

p. 2f-26, as follows: Colln. 9714, from bed P-35; 9715, P-42; 

9716, P-50; 9717, P-55; 9718, P-65; 9719, P-72; 9720, P-73; 

9740, P-43; 9750, P-78; 9751, P-79; 9752, P-80, 9753, P-81.

Poison Creek, W% sec. 24, T. 30 N., R. 117 W., Lincoln County. 

Colln. 12308-12316 were collected by J. E. Smedley, 1950; 

18816, by E. L. Yochelson and R. P. Sheldon. Colln. 12308- 

123^.4 are listed in USGS Circ. 307, p. 37-39. Also, the following collections were taken from beds indicated to be in this 

section: 12315, approximately 50 ft stratigraphically above 

top of logged phosphatic shale; 12316, approximately 35 ft 

stratigraphically above colln. 12315; 18816, Franson Member, about 50 ft above Rex Chert Member.

Red Creek, on Red Creek about half a mile from juncture with 

Snake River, NE%SE*4 Shoshone Quad., Yellowstone National Park. Colln. 12546-12553, by J. E. Smedley, 1951, and

18593 by E. L. Yochelson and R. P. Sheldon, 1959, are listed 

in USGS Prof. Paper 313-B, p. 160-162. Also, colln. 12546- 

12553 are listed in USGS Circular 324, p. 5-6. In addition, 

Colln. 18593 is from a conglomerate in lower part of Shedhorn Sandstone and is a re-collection of 12549.

South Fork of Gypsum Creek, NW% sec. 22, T. 38 N., R. 109 W., 

Sublette County. Colln. 12236-12247, by J. E. Smedley, 1950, 

are listed in USGS Prof. Paper 313-B, p. 225-229. Also, collections are listed in USGS Circ. 307, p. 26-29.

Steer Creek, sec. 9, T. 36 N., R. 116 W., Lincoln County. Colln. 

12643-12649, by H. I. Saunders, 1951, are listed in USGS 

Prof. Paper 313-B, p. 213-217. Also, collections are listed in 

USGS Circ. 324, p. 17-19.

Teton Pass, sec. 23, T. 41 N., R. 117 W., Teton County. Colln. 

12574-12581, by J. E. Smedley, 1951, are listed in USGS 

Prof. Paper 313-B, p. 190-192. Also, collections are listed in 

USGS Circ. 324, p. 14-16.

Togwotee Pass, sec. 2, T. 44 N., R. Ill W., Teton County. Colln. 

18859-18600, by E. L. Yochelson and R. P. Sheldon, 1959, are 

listed in USGS Prof. Paper 313-B, p. 180-181.

Tosi Creek, sec. 24(?) T. 39 N., R. Ill W., Sublette County. 

Colln. 12201-12213, by J. E. Smedley, 1950, are listed in 

USGS Prof. Paper 313-B, p. 200-203. Also, collections are 

listed in USGS Circ. 307, p. 18-20.

Wheat Creek, sec. 4, T. 23 N., R. 116 W., Lincoln County. Colln. 

13313-13324, by J. E. Smedley, 1952, are listed in USGS Prof. 

Paper 313-B, p. 254-258. Also, section, but not position of 

collections, is given in USGS Circ. 325, p. 20-22.

UNSTUDIED AND DISCARDED COLLECTIONS

At the time the Permian Phosphoria project collections were obtained, a few collections were made from 

both older and younger strata. The post-Permian fossils 

have not been studied in detail. Some of the collection 

numbers have appeared on measured sections published 

in Geological Survey circulars. In order that there be 

no question regarding the disposition of these collections, those not studied in detail are listed below in 

alphabetical order of section name.

Section name

Deer Creek __ _ __ _

Flat Creek. __ ___

Gros Ventre Slide--

Do.. __________

North Fork, Pine

Creek. 

Three Forks __

State

___do._-___-

__do _ _ _

___do_._____

___do_______

_._do_______

Montana _

___do ....

Collection

12535_.__

12476____

12227 . _

12125 __

12136 __

12668. ___

9730-- 

12698 _ .

10850- -

Stratigraphic unit

Dinwoody Fm.

Do.

Do.

Tensleep Ss.

Dinwoody Fm.

Do.

Do.

Ellis Fm.

Dinwoody Fm.
654 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

Scattered collections made during field studies contained no megaf ossils and none of the more common 

microfossils. These nominally unfossiliferous collections were discarded during the first stages of this 

study. However, some of the collection numbers have 

been listed on stratigraphic sections published in U.S. 

Geol. Survey circulars, and others, though not published, occur in numerical order with those on the 

f aunal distribution charts.

So that there be no question as to their disposition, 

all discarded collections are listed as follows under 

each State in alphabetical order of the name of the 

sections from which they were collected. These collections otherwise are not referred to in this paper or in 

any of the illustrations.

Section name Collection Stratigraphic unit

Idaho

Bear Creek.. _______

Conda mine ___- _ _

Do. ...

Deer Greek- _ ___ _

Gravel Creek Divide

Hot Spring. ______ _

Do 

Kendall Canyon_____

Lone Pine Spring____

Mabie Canyon____ _

Montpelier Canyon _

Do 

North Rasmussen

Valley. 

Snowdrift Mountain. _

Do 

South Rasmussen

Valley. 

Swan Lake Gulch. _ _

Trail Canyon _ ____

West Georgetown

Canyon. 

Wolverine Canyon___

12530 _ 

9700____--_-_-_._

Q7fl1 Q7O9 Q7nfi

12473

11613, 11615 ___

12604, 12606,

12608, 12610, 

12611. 

12613. 

10104, 10106,

10109. 

10453___-_- __ -.

11507 

10022, 10118______

9741_____. _______

QQS7

10445 __ ___ ______

12584.. __________

1OKQ7

10487 ---------

10585-- _ ____ .

9956 

10567______---_._

12115 _ ___

Grandeur.

Wplla TpTvi

TVTaafla "Ppolr

Wpllq TP 

TVTpc*r^p T*t»5ilr

Do.

WpHe Tp-m

Retort.

TVTf*5iHp T^paV

Do.

Tv^eade Peak

Do.

Do.

Do.

Do.

Sheep Creek__ _ __ _

Little Sheep Creek. __

Montana

10821 ... ________

11641______._____

Upper member of

Shedhorn.

Utah

Brush Creek. _______

Devils Slrde_ _ _

Franson Canyon.. ___

Laketown Canyon __

North Crawford

Mountains. 

Rock Canyon _ ____

Wanrhodes Canyon. _

10000, 10003,

10004. 

12487 _.- ________

12495 ___ ______

10964... _________

10980 _____ .

9992, 9993- ______

10622, 10653. ___

TV^Qorlo "Ppalr

Do.

TM"ocir1p "Ppcilr

Do.

Do.

Do.

Section name Collection Stratigraphic unit

Wyoming

Basin Creek __ ___ _

Do ___

Buck Creek_________

Coal Canyon __

Do ______ .

Do _-__-_____

Cokeville _ _ ___

Crystal Creek. ____ _

Deadline Ridge ___

Flat- ___ _ _

Forellen Peak ____

Gros Ventre Slide. __

Do _-. -._.

Hungry Creek ______

Middle Fork of Pine

Creek. 

Poison Creek_ _ __ _

Do __________

Steer Creek ___ __

Teton Pass

Do --._--__

Do __________

Tosi Creek.. _______

13300, 13302,

13305. 

13311 ________

12146 ____ _ _____

9744 ___ _ _______

9748 ___ _ _______

12615, 12615- ____

10935 ____ _ _ _

12539 ____ _ __ _

13346___ __ _____

12225, 12629. ____

12558 _ ____

12127 ____________

12134 ____ _ _____

12139 __ _ ____

12663 __ _______

9760 __ _____

9728, 9729 _ __

12312, 12313 _

12546_ ___ _ _____

12547, 12551 ...

12643 _______ .-

12574 ____ . ____

12577 _ -__---__-

12578.- -__

12203 ___ _ __ .__

Meade Peak.

Rex.

Meade Peak.

Do.

Rex.

Retort.

Meade Peak.

Lower member of

Shedhorn. 

Retort.

Tosi.

Do.

Lower chert member of Phosphoria. 

Tosi.

Franson.

Do.

Meade Peak.

Retort.

Meade Peak.

Tensleep Ss.

Lower member of

Shedhorn. 

Meade Peak.

Tensleep Ss.

Meade Peak.

Lower member of

Shedhorn. 

Lower chert member of Phosphoria.

Even though the remaining collections do contain 

fossils, many are of extremely limited usefulness. At 

least one-third of the collections contain fossils that are 

indeterminate as to species. Although it is possible to 

draw general conclusions from the overall aspect of 

these collections, their value for detailed morphologic 

and statistical studies of the fauna is negligible. For 

this reason, upon completion of this study, 502 collections were discarded. The collections containing better 

preserved fossils and other collections representative of 

the fossils from each stratigraphic unit have been 

retained.

REFERENCES

Allan, R. S., 1936, New records of the genus Lingula (Braehiopoda) from Tertiary strata in New Zealand: Royal Soc. 

New Zealand Trans., v. 65, pt. 4, p. 383-385.

Boutwell, J.M., 1912, Geology and ore deposits of the Park City 

district, Utah: U.S. Geol. Survey Prof. Paper 77, 231 p.

Branson, C. C., 1930, Paleontology and stratigraphy of the 

Phosphoria formation: Missouri Univ. Studies, v. 5, no. 2, 

p. 1-99.

 1933, The fish fauna of the middle Phosphoria formation : Jour. Geology, v. 41, p. 173-184.

Branson, B. B., 1916, The lower Embar of Wyoming and its 

fauna: Jour. Geology, v. 24, p. 639-644.

Cheney, T. M., 1957, Phosphate in Utah and an analysis of the 

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BIOSTRATIGRAPHY OF PHOSPHORIA, PARK CITY, AND SHEDHORN FORMATIONS 655

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656 GEOLOGY OF PERMIAN ROCKS IN THE WESTERN PHOSPHATE FIELD

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INDEX

A Page

Abundance of fossils. ____________ 575,577 

Acantkopecten alatus........................ 620,628

delawarensis-........................... 620,628

sp... . .......... _____ 620

Acknowledgments_______________ 574 

Acrolepid scales_ ___________ 591,629,630 

Acrolepis.-................................... 591

Actinocoelm maeandrina..................... 580,625

Adrianites sp............................... 621,628

Age, Ervay Carbonate Rock Member. ___ 684 

Franson Member..____________ 624 

Grandeur Member____________ 634 

lower chert member, Phosphoria Formation..... .. ... .......... ess

Meade Peak Phosphatic Shale Member.. 622

Park City Formation.__________ 684

Phosphoria Formation_________ 617,628

Betort Phosphatic Shale Member____ 688

Bex Chert Member____________ 623

Shedhorn Sandstone___________ 626

Tosl Chert Member____________ 623

Age relationships_______________ 627

alatus, Acanthopecten.. ___________ 620,628

albequus, Permophorus...................... 620,628

Allorisma......________________ 593,638

Alpine Creek__________________ 648 

alternatus, Acicidopecten.................... 620,628

Ancistriodus sp.._______________ 629,630 

Anidanthut!- ........ 584,585,593,602,615,638,639

echaris..............................__ 619,628

sp. _ ___._____ 619

annettae, Pseudopermophorus............... 620,627

Annuliconcha............................... 620,624

Antiguatonia........................ 615,635,636,639

sulcatus-............................ 618,623,628

Apachella sp__________________ 621,627 

arcuatus, Cmrithyris...... ............... 618,628

Arthropoda.___________________ 590 

Astartella........................______ 588,592

subquadrata............................. 620,627

sp-________._____________ 620 

Aviculopecten................... 586,587,592,593,594

alternatus 620,628

girtyi................................... 620,628

kaibabensis.............................. 620,628

phosphaticus.-- ...................... 620,628

vanvleeti................................ 620,628

sp._______ ________...__ 620,628 

Amculopinna sp_._______________ 619

B 

Babylonttes................................... 582,

588, 589, 593, 594, 602, 614, 622, 631, 

633,634,638 

conoideus...... ...................... 621,627

fenieri.................................. 621,627

sp___ .._....._ __ 621

BakeveUfa sp _________________ 619 

Ballard Trench______._________ 645 

Bartlett Creek__________._____ 652 

Basin Creek___________.______ 652 

Bothy my onia................................. 583,

584, 592, 593, 598, 599, 600, 615, 618, 

637, 638, 640,641, 643 

nevadensis-. 618,623,627

sp_______________________ 618

[Italic page numbers Indicate major references]

Page 

(Bathymyonfa) netadensis..................... 626

Bear Creek___ _________.____ 645 

Belemnite.____________.______ 621,628 

BeUerophon................................. 589,642

deflectus............................ 621,625,627

sp 621

beUistriata, Polidevcfa....................... 619,628

Bennett Ranch.....__.__.... . 650

Bibliography______________.__. 654 

bifidus, Schizodus. ._._ 620,627

Big Sheep Canyon______________ 648 

Big Timber __ 648

Blackfoot Narrows.._____ __ _ 645

Blind Stream.________________ 650

Bone______________________ 629,630

Brachiopoda... __.._ .. _ 588

articulata __ __.__.. 583

inarticulata. __ __-___ ___ 588

Bradyodont teeth..________.___ 629,630

Brazer Canyon. . - 650

Brush Creek Gorge..__.... . . 650

Bryozoa_____ __.__.__.__ 581 

Bryozoans, fenestrate... _ - 618 

ramose..._ .__..__._--_.-.-. 618 

Buck Creek-___... __. .. 652 

BuU Lake_____.._ 652

Burroughs Creek...__._ . . .. 652

Calcified cartilage.... 629,630

Caldwell Canyon ..- ._ . 645 

Camptonectessp. ......__________- 620

canalis, Schhodus._______-______ 620,627 

CanerineUa 575,

583, 584, 585, 592, 593, 594, 596, 602, 

614, 633, 634, 638, 640, 642 

phosphatica............. 575,592,619,622,626,627

sp-. ... ... ... 575,619

canna, Plagioglypta_____. _______ 621,627 

Canyon Camp.. __.__ 648

Canyon Creek No. 3.. 649

Cap lime.._..__..__ .... 573,602

carbonaria, Lingula. _________ 618 

Sanguinolttes.................- ......... 621,627

Castfandlasexradiata....................... 619,627

Cave Creek...__._.-... . .- 649 

Cedar Creek_.. __ _ - 649 

Cettoides. ................. 639.642

sp-.. ___.... .. - 620,627

Cephalopod Gulch-.-. - 650

Cephalopoda. -___._ - - 589 

Cherty shale member, Phosphoria Formation,

distribution of fossil collections... 648 

Chondrichthyes_______________- 629,630 

Chonetes- -___ 582,

583, 584, 585, 592, 593, 594, 596, 602, 

614, 632, 633.634,639,642,643 

ostiolatus............................... 619,628

sp....._.____._____ 619

Cinnabar Mountain__.__ - - 649 

Cladodus sp................................. 629,630

Coal Canyon. . 652

Cochliodontteeth..___ ______ 629,630 

Coelenterata. ___ . 580

Coelogasteroceras sp______ .__ 621,627 

Cokeville 652

Page 

Collecting of fossils.----- - _ _ 575

Collections, fossil. See Fossil collections.

unfossiliferous. . . _ 654 

Compostta.................................... 583,

592, 593, 594, 598, 600, 635, 636, 638, 

641, 642

rofro____________________ 618,628 

subtUita.. ............................ 618,628

sp_ _ __ __. . 618 

spp-__ _... ........ 618,628

Conant Creek.__ __-__-__ _ 652 

concinnus, Scaphettina...........-............ 620

Conda mine_______________.__ 645 

Conocardium sp-__ __ _ __ 620 

conoideus, Babylonites....................... 621,627

Conularids __________________ 618 

coronatum, Glabrocingulum~~.............. 621,627

Costatorfa sexradiata......................... 620.627

Coulter Ranger Station . ................ 650

Crassidonta sp____________-_ 629,630 

Crawford Mountain.___ ..._ ... 650 

crewulatus, Euphemites...................... 621,627

Crinoids ._.___ - - 580 

Crooked Creek______..._ _ 649 

Crurithyris.................................... 582,

583, 584, 585, 593, 594, 596, 602, 614, 

633, 634, 638 

arcuatus-. . 618,628

sp_ ___-_ . - 618 

Crystal Creek.... 652

Ctenocanthus sp....._._ 629,630

Cumberland - 652 

Cydites .................................... 592

sp . 621

Cyrtorostra varicostata...............- 620

D 

Dalys Spur_____.-_----- -- 649

Deadline Bidge...____ 652 

Death assemblages-. - 594 

Deer Creek_________-___----- - 645

deflectus, Betterophon................... 621,625,627

delawarensis, Acanthopeden...... . 620,628

Dettodut sp _ . 629,630

Dentalium sp. 621

spp.._________________. 621,627 

Depth ranges of fossils__ .. 595,596,599,614 

Derbyia-.......... 583,

584, 587, 592, 593, 598, 599, 600, 617, 

631,637,638,640,643 

magna.............. .... 619,628

sp__..... ......... ..._ ___ 619

Devils Slide 650

Dicrenodis (Pristicladodus') sp. ........ 629,630

Dicrinotus ..... 640

Dingle 645

Dinwoody Lakes.- . - 652 

Divide between Trail and Wood Canyons 645 

Dolophonodus sp............................ 629,630

Donaldina................ - 621

Dry Bread Hollow---. - 650 

Dry Canyon..------- - 650

E

East Georgetown Canyon_- 645 

echaris, Anidanthus.... 619,628

657
658 INDEX

Page

Echinauris.__ __ 583,584,593,598,600,637 

sp______________________ 618,628 

subhorrida........... ... .. 618,628

Echinoconchus.____.__ _________ 626

Echinodermata__._.____________ 580

Edmondta gibbosa___-___________ 620,627

phosphoriensis------------_____-__ 620,627

stuchburia.........-____________ 620

elongatus, Sanguinolites... . ............ 621,627

Elonichthid scales______-________ 629,630 

Enoch Valley...____.____________ 645 

Eoastarte subcircularis- .... ._____.__ 620,627

Ervay Carbonate Rock Member, age____ 624 

distribution of fossil collections __ 6$ 

paleoecology . __________. B98

crenulatus.- .______________ 621,627 

sp_______________________ 621

Euphemitopsis-... _._._________ 589 

paucinodosus.-- 621,627

subpapillosus...._ _._____ 621,625,927

ezimia, Knightites (RetUpira). .. . 621,628

F

Fairy collar buttons______________ 629,630 

Fall Creek... ..._....___....._...... 646

Fauna, Phosphoria rock complex_______ 577 

Faunal distribution charts.____._____ 574 

Fenestrate bryozoans_.-___________ 618 

errieri, Babylonites.- . 621,627

Fin-ray_____________________ 629,630 

Fish, by Dianne H. Van Sickle._____.... 691

Fish remains-.._.__.__ ________ 621 

Fish-scale marker bed...__________ 582,596 

fissus, Warthia.............................. 621,627

Flat Creek. __________________ 652 

Fontenelle Creek_________________ 653 

Forellen Peak.._ __.__________ 652 

Fort Douglas___._______________ 650 

Fossil categories________________ 691 

Fossil collecting_________________ 575 

Fossil collections, discarded __._____ 654 

Idaho....__.____.... 631,633,635,638,641

Montana. . 631,633,635,639,640,641,643

post-Permian_______________ 653

register of localities ____________ 644

Idaho.-_________________ 645

Montana.. __-___________ 648

Utah. ..._____________... 650

Wyoming. ...._._____ 652

unstudied . ...._._____ 653

Utah ____ ____ 632,633.635,639,642

Wyoming..._.__.___________ 632,

634,636,639,640,641,642,643,644

Fossils, abundance of____________ 575,577

depth ranges of_________ 595,596,599,614

sorting of___________________ 594

Franson Member, age_____________ 624

distribution of fossil collections- _____ 634

paleoecology,_______________ 698

Franson (Pinyon) Canyon._________ 651

G

Gastropoda____________________ 588 

Geneva Steel Co________________ 651 

Geographic distribution of fossil collections... 630 

cherty shale member, Phosphoria Formation . ...._______ 642 

Ervay Carbonate Rock Member..___ 64® 

Franson Member_____________ 634 

Grandeur Member.____________ 630 

lower chert member, Phosphoria Formation.- _____________ 632 

lower member, Shedborn Sandstone___ 640 

Meade Peak Phosphatic Shale Member.. 633 

Park City Formation_______ 630, 

Phosphoria Formation..632,633,638,640, 

Retort Phosphatic Shale Member. ___ 640 

Rex Chert Member____________ 638 

Shedborn Sandstone_________

Geographic distribution of fossil collections Continued 

Tosi Chert Member _ Slfl 

upper member, Shedhorn Sandstone. 643 

i, Edmondia...................-_... 620,627

i, Aviculopecien_. 620,628

Girtypecten sp._ _ . . - 620 

Girtyspira........_..... . . 621,627

Glabrocingulum.________... .. . 589,594 

coronatum.......................-___ 621.627

sp ____. _...._ - 621,627

Goniatite .___-__ 621,628

Grandeur Member, age.-. - . 624

distribution of fossil collections.-- - 630

paleoecology _ 597

Gravel Creek Divide.__. ... 646

Grizzly Creek. _ . . 646

Gros Ventre Slide...___ -_ _ - 653

guadalupensis, Streblochondria........ .... 620,628

Hamatus sp_____.... ......_ 629,630

Haplistion................... ...... 580,624

sp.____________________ 618,624 

Helkoprion.................... ... . 602

sp-. _- . - 629,630

Helodus sp_______________-__- 629,630 

Henry_______________________ 646 

HexactineUid spicules-.. . - 580 

hispidus, Sphenosteges ....... -... 618,628

Hoback.. 653

Hogback Mountain...-. 649 

Horn coral_._____________ 618 

Horridonia.............. ....... .. ... 593

Horseshoe Canyon... 651 

Hot Spring_____..._ . 646 

Hungry Creek.____._____._ ... 653 

Hustedia . ......... ..... ..... ... 583,593,600

phosphoriensis.... 619,628

sp._________-_-.... _ 619

Hystricula............................__ 592

Hystriculina.. . . 618,624,632 

wabashensis...... . 618,624

sp__.______._ . 618

Inarticulata, brachiopoda B82 

ivesi, Squamaria.......... ...__ 618,624,628

Janassa sp________________.__ 629,630 

(Jedria) sp., Naticopsis....................... 621

Jefferson Canyon________________ 649 

Johnson Creek..___________.___ 646 

Juresania sp ....._..... 618

K 

kaibabensis, Aviculopecten................... 620,628

Kelley Gulch ............... . 649

Kendall Canyon_________ ____... 646 

kentuckensis, Spiriferina.................... 619,628

Knightites (Retispira) eximia..... .. ... 621,628

sp-___________ _ _ _... 621 

Kochiproductus.. .. ~ -.... 584,593,623

longus- .. .- ... . 618,623,628 

sp.-.-...______________..._._ 618

Lake Fork...____.__.________.. 651 

Laketown Canyon______________ 651 

LaMarche Gulch,______________ 649 

Larvae.._____________________ 615 

Layland Canyon_______________ 653 

Leiorhynchus................................. 582,

583,584,585,593,594,596, 602, 614, 626, 

633, 634 

weeksL............................__ 618,628

sp._____________________ 618 

Leptodus-- - 583,623,643

sp.____________.._.._____ 619,628

Page

Life associations ________________ 

Lingula.. ............. ... ____ ..

592, 593, 595, 596, 602, 615, 632, 633, 

635, 636, 637, 638, 639, 640, 643 

carbonaria ... . .. .. . ... __ 618,

sp.

Linoproductus ................ . .. 593,

prattenianus. ......_.._____.__ 619,

Liosotetta ........... ......... 584,598,637,

sp. ........................ 

Lithistid spicules_______________ 

Little Brush Creek______________ 

Little Sheep Creek _____________ 

Little Water Canyon_____________ 

Logan______ _ _.____.__ 

Lone Pine Spring... __.__.__.__ 

longus, Kochiproductus.................. 618,623: Lower chert member, Phosphoria Formation,

594

582,

634,

628

618

624

624

639

580

651

649

649

628

Phosphoria Formation, distribution of

fossil collections-._________ 632 

paleoecology_____________ 614

M

Mabie Canyon... _ . ... 646 

maeandrina, Actinocoelia..... _ ...._ 580,625 

magna, Derbyia ________.__-__.__ 619,628 

mcchesneyana, Paleoneilo.... _ .. .. 619 

Meade Peak Phosphatic Shale Member, age.. 622

distribution of fossil collections______ 633

paleoecology________________. 600 

meeki, Myalina (Myalinella). .....__.... 619,628 

Meekospira. ...__.__ ____ 621,627

sp._____________.___.____. 621 

Middle Fork of Pine Creek...________ 653 

MU1 Creek.- 651 

mira, Composite-.___ . _ . . 618,628 

missouriensis, Orbiculoidea-...__.._____. 618

Orbiculoidea (Orbiculoidea'). 582,628 

Mollusca________ _ _-_- 585

Pelecypoda,__________.____. 686 

Montpelier Canyon.... _. . _. ... 646 

montpelierensis, Nuculopsis... .... ........ 619

Streblochondria.-.-....... _ . 620,628

Mooreoceras sp_ 621 

Mud Spring____._____ ...._. 647

Muirwoodia...... __ 583,584,593,598,643

muUistriatus 619,628

multistriatus, Muirwoodia,.......... . 619,628

Myalina,.................................... 587,593

(Myalina) sinuata........................ 619

wyomingensis thomasi_________ 619

(Myalinella,) meeki............. ...... 619,628

(Myalina) sinuata, Myalina........ ........ 619

wyomingensis thomasi, Myalina,-. ....... 619

Myalinella.__-________________ 593 

(Myalinella) meeki, Myalina_________ 619,628 

Mytiloids- _- 687

N

Naticifonn gastropod______________ 621 

Naticopsis.. ......__-._ .. _ 592

(Jedria) sp.________________ 621 

Nautilus... . 590

Neospirifer.... .... _ 583,

584,593,595,598,599, 600,635, 636, 637, 

640

pseudocameratus..... _-__.__ _ 618,628

sp- ...... ... . 618

nevadensis, Bathymyonia................ 618,623,627

(Bathymyonia)....... ..._____.__ 626

North Big Hole Canyon.. _______.__ 649 

North Crawford.-___ _._____.__ 651 

North Dry Valley ._.___._...._ 647

North Rasmussen Valley____________ 647 

North Stewart__________________ 647 

North Wooley Range__ _____....._ 647

NueuU ................................ 586,589

Nuculana 586,602,614
INDEX 659

Nuculopsis......................... 586,593,595,638

montpelierensis----_____________ 619

poposiensis-............... ...... 619,628

pukhra. ............__..._..__. 619,628

sp. A..._____ ____ 619.628

sp. B______.... ____._ 619,628

sp. C____________._________ 619 

sp - -. - -. - 619

O

obesa, Polidevcia.-.......................... 619,628

oecidentalis, Rugatia......................... 619,628

Onychites_______.__.. _ 621 

Orbiculoidea........ ..................... 582,

583, 589, 593, 596, 599, 602, 614, 625, 

628, 632, 633, 637, 638, 640 

missouriensis-......- - 618

utahensis........ ....... _ 168

(Orbiculoidea) missouriensis-..-......... 582,628

(Roemerella)........... ............. 598

utahensis- __ 582,618,628

sp._ __ -_ - 618 

(Orbkuloidea) missouriensis, Orbiculoidea..-. 582,628 

Orthonema 588,592,598,631,632

socorroense.............. ............. 621,628

osagensis, Wetterella.................... 618,628

Osteichthyes-_________________ 629,630 

ostiolatus, Chonetes.... 619,628

Ostracodes..._ . - _ 621

Palaeoniscoid fragments-.- - 591,629,630 

Paleoecological interpretations - 577, 597 

Ervay Carbonate Rock Member. 598 

Franson Member______.___... 598 

Grandeur Member.___________ 697 

lower chert member, Phosphoria Formation.... 614

Meade Peak Phosphatic Shale Member.. 600 

Park City Formation. . _ 597 

Phosphoria Formation.._ _ _. 500 

Eetort Phosphatic Shale Member. ___ 600 

Rex Chert Member.___________ 614. 

Shedhom Sandstone_________-...- 616 

Tosi Chert Member . . 614 

Paleoneilo mcchesneyana. -.................... 619

parvaradiatus- _ __ ---- -- 619

Paris Canyon..._____ ___ .. 647

Park City Formation, age 624

distribution of fossil collection._.. 630.634, 648

paleoecology.. 597

panaradfatus, PaleoneOo_________-__ 619 

patictnodosus, Euphemitopsis_____ 621,627 

Pectenoids._____-____.__ . 587 

Pelecypods-______________ . 585 

Pemmalites.- --........ . 624

Peripetoceras sp________________ 621,627 

Permophorus................... 586,588,616,627,635

albequus... ...__ , 620,628 

sp.._____ ......__ ._... 620,628

phosphatica, Cancrinella..... 575,592,619,622,626,627

phosphaticus, Aviculopecten--. _____ .- 620,628

Phosphoria Formation, age_________ 617,6%%

cherty shale member, distribution of fossil

collections_____________ 64%

distribution of fossil collections... _._ 63%,

638,638,640,642,643

lower chert member, age_. __. _. _ 6%S

distribution of fossil collections..__ 638

paleoecology______.___ _ 614

paleoecology -______.__ _ 600

Phosphoria rock complex___..__ ... 573

fauna.___________________ 677

phosphoriensis, Edmondia............... . 620,627

Hustedia. ............................ 619,628

Scapallina.............. . 620

Phricodothyris.....-.......... __ ... 593

sp. . ..... . . ..

Page

Placodermi._______________.__ 629,630 

Placoid scales.________________ 629,630 

Plagioglypta.................................. 581,

587, 588, 589, 592, 598, 599, 616, 627, 

632,635,636,637,638,641, 643,644 

canna................................... 621,627

sp....______ ._.___.......__ 621

Plathyworthenia_______________ 621 

Platycrinites.-.............................. 624,631

Platysomid scales..________._-_ 629,630 

Poison Creek__________________ 653 

Pole Canyon.____________..... 647

Polidevcia..................................... 585,

586, 587, 593, 594, 596, 633, 634, 641, 

642, 643 

bellistriata.......................... ._ 619,628

obesa...................___.......__ 619, 628

sp __________.________._ 619 

poposiensis, Nuculopsis__________ 619,628 

Porifera-...________..__.... ...._ 680

prattenianus, Linoproductus,_______ 619,624 

(Pristicladodus") sp., Dicrenodis........... ... 629,630

Protobranchs___________________ 688 

Protozoa...______.____________ 679 

pseudocameratus, Neospirifer..............-- 618,628

Pseudogastrioceras............ 589,590,602,633,634

simulator.. 622

sp. 621,627

Pseudomonotis.................. 587,592,593,636,637

sp-______________.______... 620 

Pseudopermophorus annettae.............. 620,627

pulchra, Nuculopsis......................... 619,628

Spiriferina-.-...................... 619,626,628

R

Ramose bryozoans... 

Red Creek____________.__......

(Retispira) eximia, Knightites.. .. 621,

Retort Phosphatic Shale Member, age .__

distribution of fossil collections.- ~

paleoecology. __ __... 

Rex Chert Member, age___ ____ 

distribution of fossil collection........_.._

paleoecology 

Rhadinichthid scales..__ . 629, 

Rhynchopora.................... 583,584,593,594,

taylorL-_________ ____ 619,

618

653

628

sp.

614 

630 

640 

628 

619 

Right Fork of Hobble Creek 651

Rock Canyon.... . 651

Rocky Canyon_ __ __ .. 647

(Roemerella), Orbiculoidea... ._ 598

utahensis, Orbiculoidea.............. 582,618,628

Rubey, W. W___.___._.._.___ 572,600 

Rugatia................. ... ........ 584,593

oecidentalis-... .... ..... -- 619,628

S

Salinity-___.__-_..__ 595,599,614 

Sanguinolites carbonaria.. .. ........... 621,627

elongatus............................... 621,627

Sappington Canyon_____._______ 649 

Sawtooth Mountain...__ __ _ 649 

Scales...___.___._. 629,630 

Scapallina phosphoriensis-............. _ 620

Scaphellina concinnus ...................... 620

sp.__.__.__.___.__.__ . 620,627 

Scaphopoda. 688 

Schizodus- ... ... ... ...... ..... ... ... 586,

587,588,689,592,693,598,599,616,632, 

636,636,644 

bifidus . ...... ...... 620,627

canalis-.............. . 620,627

subovatus. ..... ~~ .......... 620,627

wheeleri................................... 620

sp__ - ... 620

sexradiata, Castianella....................... 619,627

Costatoria...-. ....................... 620,627

Shedhorn Sandstone, age 686 

lower member, distribution of fossil collections_ _ __ 640

paleoecology_._._ ___ .. 618 

upper member, distribution of fossil collections________________ 643 

Sheep Creek 649

simulator, Pseudogastrioceras...... 622

sinuata, Myalina (Myalina)............. 619

Sliderock Mountain_.___ ___.__ 649 

smedleyi, Sphaenalosia. 618,628

Snowdrift Mountain.___ ..______ 647 

socorroense, Orthonema..........______ 621,628

Sorting of fossils________________ 594 

South Dry Valley_______________ 647 

South Fork of Gypsum Creek________ 653 

South Fork of Sage Creek _ .. 647 

South Rasmussen Valley_ __. . .. 647 

South Stewart Canyon____________ 647 

Sphenalosia................... ___ 584, i

Sphenosteges - 583,584,593,598,599,600,635

sp-_________-____-_______ 618

Spines.______________.______ 629,630 

Spiriferina... ......___._-__ 583,

584,587,593,598,599,600,637, 638, 642, 

643 

kentuckensis..... ..... 619,628

pulchra... ....__ __. 619, 626,628

sp..________.___ _____._ 619 

Split Mountain________________ 651 

Sponge spicules_________.____ 580,618 

Squamaria....... ...... _.. 584,593,624

ivesi. - 618,624,628

sp._______._____ _______ 618 

Stearoceras sp__ __ __._ .. 621 

Steer Creek.....__________._____ 653

Str atigr aphic sections, register of localities.... 644

register of localities, Idaho..._______ 645 

Montana .___ ____ .. 648 

Utah.. ........ ............ 650

Wyoming_._____._______ 652 

Strawberry Valley... ___ ___ . _. 651 

Streblochondria .................... 582,

585, 586, 587, 592, 593, 594, 596, 602, 

614,634,638,639,641 

guadalupensis.............._______ 620,628

montpelierensis........ . .... 620,628

tubicostata. 620,628

sp _ _ __ 620 

Strobeus-. ........ ....... .... 621

stuchburia, Edmondia............... . 620

subcircularis, Eoastarte...... ___ . 620,627

subhorrida, Echinauris.... . . 618,628

subovatus, Schi2odus-........ .. . 620,627

subpapillosus, Euphemitopsis......... 621,625,627

subquadrata, Astartella-........--.. ....... 620,627

subtilita, Composita......................... 618,628

sulcatus, Antiquatonia... ________ 618,623,628 

Swan Lake Gulch. . . 648

T

Tabantaloceras sp__.._ _ ... 621 

taylori, Rhynchopora.. 619,628

Teeth... 629,630

Teton Pass____ __ _ ... 653

thomasi, Myalina (Myalina) wyomingensis,... 619

Timber Creek ________-_____._ 648

TogwoteePass--.. . . 653

Tosi Chert Member, age.. . ... 623

distribution of fossil collections. _ 643

paleoecology- 6/4

Tosi Creek. __________.____.__ 653

Trachydomia 621,627

Trail Canyon 648 

Trilobites.__ ___... __- ._ 621 

Trochus.... .... . 589

tubicostata, Streblochandria............. . 620,628
660 INDEX

U

Upper Brazer Canyon_____________ 651 

utahensis, Orbkuloidea........................ 618

Orbieuloidea (Roemerella)........... 682,618,628

V

Vanadium________ _________ 572,600 

sanvleeti, Aefcidopecten...................... 620,628

varicostata, Cyrtorostra........................ 620

Vertebrate ________________ 629,630

W

Waagenoceras___________________ 622 

wabashensis, Hystriculina.._________ 618,624

Page

Wadhams Spring_______________ 649 

Wanrhodes Canyon.._ . 651 

Warm Springs Creek. __ 649 

Warthiafissus.............................. 621,627

sp_.______________ ___.... 621

Waterloo Phosphate pit____________ 648 

weeksi, Leiorhynchus__-____ ---- 618,628

Wetteretta...................._ 683,585,593,642,643

osagensis............................__ 618,628

sp _ - 618

West Dairy...__________________ 648 

West Fork of Blacktail Creek.- , 649

Page

West Georgetown Canyon.._.. 648 

Wheat Creek.__._.___ _._...... 653

wheeleri, Schizodus........ _____.___ 620

Waktngia............................... 588,592,593

sp - 620 

Williams, J. Steele, quoted. - 625 

Wolf Creek...... . . 651

Wolverine Canyon___ ___._____ 648 

Woodall Creek._..__ 648

Worthenia...................... 589,593,594,634,641

sp __ - 621 

wyomingensis thomasi. Myalina (Mvalina).... 619

U.S. GOVERNMENT PRINTING OFFICE: 1968