Upper Paleozoic Rocks in 

The Oquirrh Mountains and 

Bingham Mining District, 

Utah

GEOLOGICAL SURVEY PROFESSIONAL PAPER 629 - A

Upper Paleozoic Rocks in 

The Oquirrh Mountains and 

Bingham Mining District, 

Utah

By E. W. TOOKER and RALPH J. ROBERTS 

with a section on

BIOSTRATIGRAPHY AND CORRELATION

By MACKENZIE GORDON, JR. and HELEN M. DUNCAN

GEOLOGIC STUDIES OF THE BINGHAM MINING 

DISTRICT, UTAH

GEOLOGICAL SURVEY PROFESSIONAL PAPER 629-A

A study of the structures, the lithologic successions, 

and the fossils of two sequences of rocks of the 

same age that are juxtaposed by thrust faults

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

WALTER J. HICKEL, Secretary

GEOLOGICAL SURVEY 

William T. Pecora, Director

Library of Congress Catalog Card No. 73-607760

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

Washington, D.C. 20402 Price $1 (paper cover)
CONTENTS

Abstract _________________________

Introduction _________________________

Acknowledgments ______________________

Geologic setting _____________________

Previous terminology and recommended changes 

Revised upper Paleozoic stratigraphy __________

Rogers Canyon sequence _____________

Green Ravine Formation ___________

Oquirrh Group ___________________

Lake Point Limestone _______

Erda Formation _________________

Kessler Canyon Formation _______

Park City Formation ______________

Grandeur Member __________

Bingham sequence ____________________

Oquirrh Group ________________

West Canyon Limestone _____ 

Butterfield Peaks Formation _____

Bingham Mine Formation _____ 

Clipper Ridge Member _______

Markham Peak Member ______

Page 

Al

1

2

2

5

9

9

10

11

11

14

18

21

21

23

23

23

27

33

33

35

Psge

Biostratigraphy and correlation of the Oquirrh Group 

and related rocks in the Oquirrh Mountains, Utah, 

by Mackenzie Gordon, Jr., and Helen M. Duncan __ A38 

Rogers Canyon sequence _ _ 39 

Green Ravine Formation ____________ 40 

Lake Point Limestone ______________"_ 42 

Erda Formation __________________ 46

Kessler Canyon Formation ___________ 48

Park City Formation, Grandeur Member __ 49 

Bingham sequence ___________ _ 50

West Canyon Limestone _____ 50

Butterfield Peaks Formation ______ 50

Bingham Mine Formation ___________ 53

Clipper Ridge Member ________ _ 53

Markham Peak Member ____ _ 53

Correlation and age of the Bingham Mine

Formation _______________ 55

Register of late Paleozoic megafauna collecting localities in the Oquirrh Mountains, Utah ______ 57 

Register of late Paleozoic fusulinid collecting localities 

in the Oquirrh Mountains, Utah, identification and 

comments concerning fusulinids by R. C. Douglass _ 66 

References ____________ 70

Index __________________________ 73

ILLUSTRATIONS

Pa<"e 

FIGURE 1. Index map showing the principal mountain ranges in the Great Basin region in northwestern Utah ___ /2

2. Sketch map of the Oquirrh Mountains and South Mountain showing the locations of the Rogers Canyon,

Bingham, and Curry Peak sequences _____.__________________________________ 3

3. Generalized columnar sections of the Rogers Canyon and Bingham sequences in the Oquirrh Mountains_ 4

4. Sketch map of the Oquirrh Mountains showing location of type and reference sections _______ _ _ 5

5. Columnar sections showing the development of upper Paleozoic rock-stratigraphic divisions in the Bingham

sequence ________________________.___________________________________ 6

6. Columnar sections showing the development of upper Paleozoic rock stratigraphic divisions in the Rogers

Canyon sequence __________________._____________________________________ 8 

7-12. Photographs of:

7. Typical exposures of Rogers Canyon sequence _____________________ _ 12

8. General features of the lithology of the lowermost part of the Lake Point Limestone _ __ __ ]"3

9. The upper two-thirds of Erda Formation and the basal part of Kessler Canyon Formation _ 15

10. Typical exposures of reference section of the West Canyon Limestone and the basal portion of the

Butterfield Peaks Formation in Soldier Canyon __________________-__________ 24

11. Typical exposures of the middle part of the Butterfield Peaks Formation at the head of White Pine

Canyon tributary of Middle Canyon __.________________________________ _ 27

12. Typical exposures of the Jordan (limestone) marker bed (a thick cherty limestone) within the base 

of the Clipper Ridge Member of the Bingham Mine Formation at the type locality of the 

member in Middle Canyon ______-______________________________ _ 28

13. Correlation chart of sections in the central Great Basin ____________________________ 56

III
IV

CONTENTS

TABLES

Page 

TABLES 1-6. Megafaunas:

1. Green Ravine Formation type section ___________________________________ A40

2. Lake Point Limestone type section _______________________________________ ' 43

3. Erda Formation type section __________________________________________ 46

4. Park City Formation, Grandeur Member reference section __________________ 49

5. West Canyon Limestone reference sections in West Canyon and Soldier Canyon ______ 51

6. Butterfield Peaks Formation type and reference sections in West Canyon and Soldier Canyon _ 52
GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS 

AND BINGHAM MINING DISTRICT, UTAH

By E. W. TOOKER and RALPH J. ROBERTS

ABSTRACT

Recent studies in the Oquirrh Mountains indicate that the 

rocks of late Paleozoic age may be divided into two main 

sedimentary sequences, one north of the North Oquirrh thrust 

fault and the other south of the Midas thrust fault. Upper 

Paleozoic stratigraphic sections, which make up most of the 

rocks in the range and in the Bingham mining district, are 

in the Bingham sequence, on the upper plate of the Midas 

thrust; a much thinner section of comparable age occurs 

in the Rogers Canyon sequence, on the upper plate of the 

North Oquirrh thrust. Underlying both the North Oquirrh 

and Midas thrusts is an areally small, stratigraphically incomplete, complexly folded, faulted, and altered sequence, 

which seems stratigraphically and structurally more akin to 

the Rogers Canyon sequence than to the Bingham sequence.

The main stratigraphic unit of the Rogers Canyon and 

Bingham sequences, the Oquirrh Group, is composed of three 

mappable lithologic units: a lower clastic limestone; a middle 

unit consisting of cyclically repeated limestone, shale, and 

sandstone; and an upper unit of interlayered thick beds of 

quartz sandstone and thin beds of carbonate sandstone. 

Formal names are here proposed for the units in the Rogers 

Canyon sequence, and previous terminology is examined for 

comparable units in the Bingham sequence because of the 

distinctive sedimentary and faunal characteristics in each. 

In addition, some member units and marker beds of local 

significance are recognized. These lithologic units have been 

useful in the preparation of new geologic maps of the Oquirrh 

Mountains and in making regional correlations with comparable rocks elsewhere in the Great Basin.

The Rogers Canyon sequence consists of the following 

formational units, in ascending order: the Green Ravine 

Formation (new) of Late Mississippian age; the Oquirrh 

Group comprising the Lake Point Limestone (new) of Late 

Mississippian and Early Pennsylvanian age1 , the Erda Formation (new) of Middle Pennsylvanian age, and the Keesler 

Canyon Formation (new) of Late Pennsylvanian and Early 

Permian (?) age; and the Grandeur Member of the Park 

City Formation of Early Permian age.

The part of the Bingham sequence overlying the Manning 

Canyon Shale of Late Mississippian and Early Pennsyl1 Since the preparation of this report, it has been determined that 

paleontologic evidence shows a slight difference in the boundary of the 

Lower and Middle Pennsylvanian Series as uspd in the midcontinent 

when correlated with the type Pennsylvanian in the Appalachian 

region. Indications are that part of the Morrow is Middle Pennsylvanian in age.

vanian age consists of the following formational units in the 

Oquirrh Group: the West Canyon Limestone (redefined) of 

Early Pennsylvania age; the Butterfield Peaks Formation 

(new), of Middle Pennsylvanian age; and the Bingham Mine 

Formation (redefined) of Late Pennsylvanian age, which is 

divided into the Clipper Ridge and overlying Markham Peak 

Members (new).

. The Carboniferous and Early Permian rocks of the Oquirrh 

Mountains are very fossiliferous locally and provide a reasonable basis for dating these rocks. They also provide a 

faunal and biostratigraphic framework for correlating the 

formations of the Rogers Canyon and Bingham sequences with 

each other and with similar rock sequences elsewhere in the 

Great Basin and border areas to the east.

INTRODUCTION

The stratigraphy of sedimentary rocks in different 

parts of the Oquirrh Mountains, Utah, has been tl °. 

subject of many reports during the past 70 years 

(Spurr, 1895; Keith, 1905; Gilluly, 1932; Nygreen, 

1958; Bissell, 1959; Welsh and James, 1961; Tooker 

and Roberts, 1961, 1963). Several systems of stratigraphic nomenclature have been proposed in the?e 

reports for rocks in specific areas within the range, 

but no comprehensive definitive stratigraphic terminology for the whole range has been published. 

The investigations by Welsh and James (1961) in 

the central and southern parts of the range, particularly near the Bingham ore deposits, and tl n 

studies by Tooker and Roberts (1961; 196F) 

throughout the range are updated in the present 

report and new stratigraphic and faunal data are 

included. The revised stratigraphic data provide 

standard units for geologic quadrangle maps of the 

Oquirrh Mountains.

The stratigraphic nomenclature used in this report is largely based on the measured sections and 

maps of Welsh and James (1961, pis. 2 and 5), tH 

measured sections and map by Tooker and Roberts 

(1961) and Roberts and Tooker (1961), our unpublished maps, and the stratigraphic sections and faunal data in this report. A section listing and describ-
A2 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

ing the characteristic fauna present and the biostratigraphy and correlation of Oquirrh Mountains 

rocks is by Mackenzie Gordon, Jr., and Helen M. 

Duncan. The topography of the northern part of the 

Oquirrh Mountains is shown on the following 7l/2- 

minute quadrangle maps: Mills Junction, Garfield, 

Magna, Tooele, Bingham Canyon, and Lark. The 

southern part of the range is shown on the Stockton 

and Fairfield 15-minute quadrangles.

ACKNOWLEDGMENTS

We deeply appreciate the assistance of colleagues 

who helped provide and assemble the data for this 

report: Rudolph W. Kopf, William J. Moore, and 

Mackenzie Gordon, Jr., helped measure stratigraphic 

sections; Helen M. Duncan, Mackenzie Gordon, Jr., 

Raymond C. Douglass, and Ellis L. Yochelson collected many of the fossils and made all of the fossil 

determinations; and comments by Norman J. Silberling and Ralph L. Miller have materially helped to 

improve the presentation of these data. We gratefully acknowledge also the helpful criticisms of 

Alien H. James and John E. Welsh of the Kennecott 

Copper Corporation and the use of Welsh's extensive 

stratigraphic and paleontologic data (Welsh and 

James, 1961). Their interpretations, however, do 

not fully agree with all of our interpretations.

GEOLOGIC SETTING

The Oquirrh Mountains are in north-central Utah 

(fig. 1) in the eastern part of the Great Basin. The 

range is chiefly made up of folded and thrust-faulted 

sedimentary rocks of Paleozoic age that have been 

intruded by rocks of Tertiary age and later uplifted 

and tilted eastward by basin and range faulting. Of 

lesser extent are volcanic rocks of Tertiary age that 

crop out along the central part of the east side of 

the range.

Most of the 12,000-18,000 feet of upper Paleozoic 

strata exposed in the northern and central parts of 

the Oquirrh Mountains consist of varying combinations of carbonate- and quartz-rich clastic sediments 

ranging in age from Late Mississippian through 

Permian. These in large measure constitute the 

Oquirrh Formation of Gilluly (1932) or the Oquirrh 

Group of Welsh and James (1961). The lithology of 

the Oquirrh Group in the range (as well as in many 

other places in the Oquirrh basin of deposition) can 

generally be divided into three distinct units: (1) a 

lower clastic limestone, (2) a medial unit consisting 

of cyclical beds of limestone, shale, and sandstone, 

and (3) an upper unit consisting predominantly of 

interbedded quartzite and sandstone (Tooker and

80 MILES 

I

FIGURE 1. Principal mountain ranges in the Great Basin 

region in northwestern Utah. The area covered by the 

dashed rectangle (area of figs. 2 and 4) includes the 

Oquirrh Mountains and South Mountain.

Roberts, 1963). However, the thickness and age of 

these units vary from place to place, and the sedimentary characteristics of key beds cannot he traced 

with certainty across thrust faults in the Oquirrh 

Mountains or from range to range elsewhere in the 

Great Basin.

The authors are convinced that structurally the 

Oquirrh Mountains make up a part of the imbricated 

upper plate of the Charleston-Nebo thrust plate, 

which is exposed in the southern part of the adjacent Wasatch Mountains (Crittenden, 1961; Roberts 

and others, 1965). Near Bingham two thrust faults, 

the North Oquirrh and Midas,2 separate thr^e struc2 The North Oquirrh thrust was mapped independently by .lames. 

Smith, and Welsh (1961. p. 5S) and by Roberts and Tcoker (1961, 

p. 40) and jointly named. A second fault, the Midas thrust, was first 

mapped in thp Lark mine by geologists of the United States Smelting, 

Refining, and Mining Co.. where It was called the North fault. In 1951 

C. L. Thornburg recognized it as a thrust fault, but his information 

was not published (oral commun., 1965; Hewitt. 1966). In 1956 this 

fault was mapped independently by Allan James and was1 named the 

Midas thrust (James, Smith, and Welsh, 1961, p. 62). To avoid confusion of a North thrust fault with the similarly named North Oquirrh 

thrust, the name Midas is retained in this report.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH

112° 30' 15' 112°00'

EXPLANATION

A3

40°45' 

40° 15'

5 MILES

i i i I

SEDIMENTARY ROCK 

SEQUENCES

Intrusive porphyry

Contact

Fault 

Dashed where approximately located

A A A A A A

Thrust fault

Dashed where approximately located. 

Sawteeth on upper plate

-ftNormal Overturned 

Axis of anticline

Normal Overturned 

Axis of syncline

FIGURE 2. Sketch map of the Oquirrh Mountains and South Mountain showing the locations of the Rogers Canyon,

Bingham, and Curry Peak sequences.

tural blocks containing at least two distinct sedimentary sequences3 (figs. 2, 3). Tooker believes

8 The term "sequence" is used here in the sense of Silberling and 

Roberts < 19R2. p. 6) as "units of major rank * * * set apart from 

underlying or overlying sequences by unconformities * * * . Sequences 

are discrete rock units, some of which, though lithologirally distinct. 

were deposited under much the same environmental conditions."

that the rocks on South Mountain, a transverse 

range adjoining the Oquirrh Mountains on the west, 

may constitute a separate structural block.

The North Oquirrh thrust, which separates the 

Rogers Canyon sequence on the upper plate from the 

more disturbed but possibly related sequence on the 

lower plate, tentatively called the Curry Peak
A4 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

sequence, strikes nearly southeast across the range, 

dips northward about 35°, and is offset locally by 

normal faults. In the upper plate of this thrust, 

asymmetric folds plunge northeastward and are 

locally overturned southward; thus, the apparent 

movement on the thrust was from the northwest or 

north. The Midas thrust, separating the Bingham 

and Curry Peak sequences, strikes northwest-southeast and dips about 45° SW. Asymmetric folds in the 

upper plate plunge northwestward and are locally 

overturned to the northeast; they indicate, therefore, that movement on the thrust was from the 

southwest. The complexly folded and faulted, stratigraphically incomplete Curry Peak sequence locally

exposes two sets of folds on imbricate thrust fault 

structures, one striking northwestward and the 

other northeastward.

Granite, granite porphyry, and monzomte stocks 

and dikes, which intrude the sedimentary rocks in 

the central and southern parts of the Oquirrh Mountains, have been described by Boutwell (1905), Gilluly (1932), Schwartz (1947), Stringhart (1953), 

James, Smith, and Welsh (1961), and Peters, James, 

and Field (1966). The Bingham and Last Chance 

stocks, the largest intrusive bodies, are exposed in 

the central part of the Bingham mining district in 

the east-central part of the range. Other intrusive 

bodies crop out in and near the Ophir, Stockton,

BINGHAM SEQUE'NCE

ROGERS CANYON SEQUENCE

SYSTEMS

CO

O

u_

O

CD

<

O

SYSTEM

z:

<

^

OL 

LJ 

Qz

<

z

^

fe

z

QCO <

8£ 

^co

SERIES

c

Mo E

- iff

^

=5 g.ra

 5- a>5

'^

0 c ro 

~1 Q. >

Upper Mississippian

GROUP

c

,_ 'c 

2 § SI1

QL

%

.C

CT 

O

FORMATION

o

-* ^"^ 

v- -P* <o

£oE

^ 

*- C O

« >. (O m c E

*u£

c

uj E

£

£ c 1

5 -1

Green Ravine

Formation

MEMBER

randeur

C5 I

»£

tfe^;

^^m

;W-*: : ' ;' :: ' .

:-^.\::*::y. :::.

i i i

1 1 1 1

III 1

^J^J.J-LJ

X

CURRY PEAK SEQUENCE

(Section undivided, 

not diagrammed)

EXPLANATION £

 ftShale

- * ^^-

Eroded top 

Covered base 

Age correlation

0 2000 4000 FEET

rr^sTv^ . - .V-.-:/-;^: : :

:-VA:'-'-vv/

 \WX\

 ' . ': -.' : '£ :

:#f-,.--:^.:'

 :: : :. : : : . /. :

i i i

.' ' :' - .' 7 ' :. ::{ :.-:^:-'.

1,1,1

^. ":.\v-.---

1 1 1 

 : : *-. :

1 1 1

: : ': ./ :: ' ': : 

' :: '. '^ ':.-.

1,1,1, 1 l''"l"'

1 1 1

 1 1 1 

1 1

1 1

I.I.I 1 1

.. . . . T ..

1 I 1

MEMBER

^

TO

£

m

^

2

m 0) 

Q. 60

n<*

FORMATION

c 

o

TO

E

o

LL.

?

ig

E

(0

.c

c

^

£§

"01=

£E

Q> O

3

ill

5 <D c

|l<3"--|

3 c

f?l

*£M

GROUP

^ 

o

.c

3

s

SERIES

£1

>

&

Q_

S.

a.

<o

>

&

?

2

sig

5 J£= Ss

c

a

«%5

o

g

3

SYSTEM

<

z:

§

CO

z:

LJ 

Q_

z

QCO

^

SYSTEMS

CO

O

OL 

LJ 

LL.

z:

o

OQ

OL 

<

O

VERTICAL SCALE

FIGURE 3. The Rogers Canyon and Bingham sequences in the Oquirrh Mountains showing relative proportions and general 

character of lithologic units and their structural relationship to the Curry Peak sequence.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A5

and Mercur mining districts in the southwestern 

part of the range (Gilluly, 1932). Tertiary extrusive 

flows, breccias, and water-laid tuffaceous rocks, 

which have been described by Gilluly (1932) and 

Smith (1961), are found in two distinct areas on 

the margins of the central part of the Oquirrh 

Mountains (fig. 2). The smaller of these two areas 

lies at the northeast base of South Mountain; the 

larger lies 12 miles to the east along the eastern

112°30'

40° 45' 

flanks of the Oquirrh Mountains and extends over 

much of the adjoining western Traverse Mountains.

PREVIOUS TERMINOLOGY 

AND RECOMMENDED CHANGES

The Oquirrh Formation has been studied in several localities in the central and southern parts of 

the Oquirrh Mountains during the past 70 yesrs 

(fig. 4), but only recently in the northern part.

112°00'

EXPLANATION

SEDIMENTARY 

ROCKS

Marine rocks 

IGNEOUS ROCKS

i^^A :;&i\i

s- ^ v > !*".»*«**

Extrusive rocks Intrusive rod s

m

General area of measured 

section

40°15' 

5 MILES

Approximate location of 

measured section

STRAT1GRAPHIC SECTIONS 

CITED:

1. Mercur district Spurr 

(1895)

2. Bingham district-Keith 

(1905)

3. Stockton-Fairfield-Gilluly 

(1932)

4. West Canyon Nygreen

(1958)

5. Lewiston Peak Bissell

(1959) 

6a. Butterneld Peaks-Welsh

and James (1961) and

this report 

6b. South Mountain Welsh and

James (1961) 

7a. West Canyon-Middle

Canyon Welsh and Jamei?

(1961) and this report 

7b. Markham Peak Welsh and

James (1961) and this

report 

8. Eogers Canyon-Tooker and

Roberts (1961) and this

report 

9a. Black Rock Canyon-Tooker

and Roberts (1961) and

this report 

9b. Kessler Canyon-Little

Valley-Tooker and

Roberts (1961) and this

report

10. Coon Canyon-Tooker and 

Roberts (1961) and this 

report

11. Soldier Canyon Tooker, 

Gordon, and Roberts 

inthis report

FIGURE 4. Sketch map of the Oquirrh Mountains showing the location of type and reference sections.
A6 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Many formational and member names have been 

applied to the formation in the southern part of the 

range; the complex evolution of stratigraphic terminology shown in figure 5 is summarized chronologically in the following paragraphs.

In 1895 Spurr referred to rocks at the Mercur 

mining district as the Great Blue Limestone and the 

overlying upper intercalated series (fig. 5, section 

1). Keith (1905) named the rocks in the immediate 

vicinity of the Bingham mining district the Bingham Quartzite, but he was not able to designate a 

top or bottom to the formation; part of the Bingham 

Quartzite is now known to correspond to the upper 

part of Spurr's upper intercalated series (fig. 5,

sections 1 and 2). Because these rocks have subsequently been reassigned by later workers to the 

Oquirrh Formation as defined by Gilluly (1932), the 

name Bingham Quartzite is here considered abandoned. Keith also designated several prominent limestones in his Bingham Quartzite as members and 

lentils. Among these are the Tilden (which h^ designated the Petro on pis. 1 and 2) and Phoenix Limestone Lentils and the Butterfield, Lenox, Jordan, 

Commercial, Highland Boy, and Yampa Limestone 

Members. He suspected that the last four members 

represented only two units, a fact since substantiated (Hunt, 1924, p. 861). These names and others 

used in the mines to designate marker b^ds we

EXPLANATION

Age correlation Incomplete section

Lithologic correlation Eroded contact

Welsh and James (1961) 

(Composite at 

6a, 6b, and 7a)

VERTICAL SCALE

3

Ke.th (1932)

(1905 .^x~-v^-^i

p. 33-35,

pis. 1 and 2)

1

Spurr 

(1895)

K^~'-^^^x'v*'^!

Upper 

intercalated 

series

tu

c 

o

$

5 

tu

3 

CO

3

Upper 

shale

-i

Members:

Yampa

Limestone

Highland

Boy 

v Limestone 

N Commercial

}g Limestone

p Limestone

 Lenox

 £, Limestone

c Butterfield

00 Limestone

Lentils: 

Phoenix 

Limestone 

Tilden 

_ _ _ Limestone

Aower shale

"""" --^^

~ Lower i nterc? ~~ ~ . 

. lated series 

Vower mestone

Oquirrh

Formation

Manning 

Canyon 

Shale

"iu a* 

ml

si

Humbug 

Formation

\

\

\ /

i ,'

\ (» 

*, / ,'

\

% /

* % c1-' "

4?/

^/

.' S1

*' ' c1 '

5

4 ^ Bissell 

Nygreen \ (1959)

i Pole 

| Canyon

i -. . « u Mprnhpr

2 Lewiston

= * . tS Peak 

2 "Sandy '-.._ § Member

^ member £ Cedar

^ ^ Member

t cr Meadow

= ' ^n ' ^ ^^

Member Member

Manning Manning 

Canyon Canyon

Great 

Blue 

Limestone

 ' t V

/

J «

;

/

lO **

(Atoka

and 

Morrow)

(Chester)

Kirkman

| Formation |

Clinker 

Formation

Formation

^sr~-^^~

Q.

5 

cr 

O

Bingham

Mine 

Formation

Butterfield 

Formation

"White

Pine"

Formation

Formation

Manning 

Canyon 

Shale

7

Th s report 

(Composite at 

6a, 7a, and 7b)

,-'

..- '

f » f

, 

_..- "

,.- '

"»-..w

"*

D 

O

^

t

8

c

-2

E

o

tu

c

E

^

00

c 

CD

tu

ro E

ro

^

0)

u0-S

Butterfield 

Peaks 

Formation

West

Canyon 

Limestone

Manning 

Canyon Shale

Great 

Blue 

Limestone

 Long Trail Shale 

Member

SERIES

'c

>

v>

c

a

<r

c.

<r

c

(T

5) 

c 

a

s:

 =i

c

u£

Upper |1

ississippian

2>

LJ

7

_J

£

7*-

LU 

Q.

SISSIPPIAN]

CO

SYSTEM

V)

OiRBONIFERC

o

FIGURE 5. Development of upper Paleozoic rock-stratigraphic divisions in the Bingham sequence. Section numbers indicate

locations in figure 4.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A7

herein consider informally named marker beds 

rather than formally named units of member rank.

Gilluly (1932) formally named the Oquirrh Formation. He placed the base at the top of the Manning 

Canyon Shale (fig. 5, section 3), a lithologically uncertain transitional boundary, but did not define the 

top as it is not exposed in the southern part of the 

Oquirrh Mountains. He estimated the exposed thickness of the formation to be 16,000-18,000 feet, but 

he did not designate a type section. All faunas collected by him from the southern part of the Oquirrh 

Mountains proved to be Pennsylvanian, but Bissell 

(1936), Baker (1947), and Welsh and James (1961) 

recognized Permian faunas from Oquirrh strata 

nearby in the Wasatch Mountains and South Mountain.

Nygreen (1958) was the first to study the lower 

part of the Oquirrh Formation in detail in the 

southern Oquirrh Mountains area; he named the 

lower limestone unit the West Canyon Limestone 

Member (fig. 5, section 4). We retain this name, 

but raise it to formational rank the West Canyon 

Limestone. Nygreen (1958) also used the term 

"Sandy Oquirrh" for the overlying strata. This term 

is not considered a formal name.

Bissell (1959) described five time-stratigraphic 

subdivisions of the Oquirrh Formation in the southern Oquirrh Mountains in the vicinity of Lewiston 

Peak (fig. 5, section 5) ; their boundaries coincide 

with those of the provincial series of the Pennsylvanian. These units are well exposed south of Ophir, 

where they are broken and offset by numerous faults. 

As defined by Bissell, these units did not have lithologically recognizable tops and bottoms, which disqualifies them as rock-stratigraphic units (Code of 

Stratigraphic Nomenclature, Art. 4). Although it is 

difficult to trace individual beds, generally recognizable lithologic units in the West Canyon Limestone and the lower part of the Butterfield Peaks 

Formation can be traced northward from the Lewiston Peak area to West Canyon and can be correlated 

with their stratigraphic and age equivalents. A Morrow to Des Moines age is established for these rocks 

throughout the lower part of the Bingham sequence 

on the basis of the fusulinid, brachiopod, coral, and 

bryozoan assemblages (Mackenzie Gordon, Jr., H. 

M. Duncan, and R. C. Douglass, this report, and 

written comm., 1965). This age designation conflicts 

with the age designation Morrow through Virgil 

reported by Bissell (1959), an age designation 

based on fusulinids. BisselPs (1962, p. 37, 40, and 

43) suggestion of abnormal thickening of the stratigraphic section in the southern part of the Oquirrh

Mountains north of Lewiston Peak is believed to be 

invalid.

Welsh and James (1961) elevated the Oquirrh 

Formation of Gilluly (1932) to the Oquirrh Group. 

We support this designation because the Oquirrh 

consists of thick but extremely variable litholoTic 

units that can be recognized elsewhere in the Gr^at 

Basin and Wasatch Mountains. The relationships of 

the lithologic units require a complex nomenclature. 

Welsh and James restricted the Oquirrh Group to 

rocks of Pennsylvanian age and included in it four 

formational units, from oldest to youngest, the 

Maple, "White Pine," Butterfield, and Bingham 

Mine Formations (fig. 5, section 6).

Nomenclatural difficulties and our attempt here to 

emphasize comparable regionally recognizable lithologic units now prompts us to modify that formational terminology. The lower part of the Maple 

Formation is a lithologically distinct clastic limestone that Nygreen (1958) named West Canyon 

Limestone Member; it is herein raised to formation 

rank. The cyclic limestone, shale, and sandstone of 

the upper part of the Maple closely resemble comparable beds in the overlying White Pine and Butterfield Formations, which are herein combined into 

a single formation. (The formational name White 

Pine is now known to be preempted because of prior 

usage for an upper Paleozoic formation in Nevada.) 

Owing to confusion arising from the fact that the 

Butterfield Limestone of Keith (1905) occurs in the 

"White Pine" Formation of Welsh and James but 

not in the Butterfield Formation, the combined unit 

is here renamed the Butterfield Peaks Formation 

(fig. 5, section 7). Finally, the Bingham Mine Formation of Welsh and James (1961) is broadened to 

include all of the comparable predominantly qur.rtzite-sandstone beds of Pennsylvanian age above the 

Jordan marker bed; as such it includes some ba.ds 

considered to be of Early Permian age by Welsh and 

James (1961). The formation is terminated upward 

by erosion and the Midas thrust fault. Thus, the 

Oquirrh Group is defined in the Oquirrh Mountains 

to denote rocks that possess a distinctive three-part 

lithologic succession that ranges in age from Early 

to Late Pennsylvanian.

Welsh and James (1961, p. 8), following Keith 

(1905), suggested names for individual prominent 

limestone beds in the Bingham mining district but 

said that, "In a later paper the individual limestones 

will be formally named." We propose here to derignate them informal marker beds; they are locally 

very important ore-forming horizons in the Bing-
A8 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

8-10

Tooker and Roberts _ n _ 

(1961) 0-iU

f

o

re

fc

8

Po 7

PPo6

PlPOg

Po4

-3

Po2

IPOj

 

Q_JQ This report

Tooker and Roberts

(1963)

Canyon (?) 

Shale

1

g

£c3E Member

Uc

u_

sz

§

cr

Upper

member

Middle 

member

Lower

Unnamed 

formation

Permian

__.- -"""""

Pennsylvanian

and 

Permian

Pennsylvanian

--..

Mississippian

§ 

-£>, = Grandeur

£oE Member

o.

P

O

 F

°

Kessler 

Canyon

Formation

Erda 

Formation

Lake Point

Limestone

Green

Ravine

Formation

__ __ __ __

EXPLANATION

Age correlation

Lithologic correlation

Incomplete section

Eroded contact

0 1000 

I I I I I

2000 FEET

VERTICAL SCALE

FIGURE 6. Development of upper Paleozoic rock-stratigraphic divisions in the Rogers Crnyon 

sequence. Composite of sections measured in localities 8, 9a, 9b, and 10 (fig. 4).
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A9

ham mining district but are often difficult to trace 

outside the district.

Above the Oquirrh Group, Welsh and James 

(1961) also named two younger units, the Permian 

Curry and Clinker Formations, and designated 

overlying even younger rocks as the Permian Kirkman, Diamond Creek, and Park City Formations. 

More recent mapping of the Curry Peak sequence 

rocks in the structurally complex area north of the 

mining district by Tooker and Roberts (unpub. 

data) has shown these rocks to be lithologically 

similar to rocks of the Rogers Canyon sequence 

although they are locally highly altered and sheared, 

and their fossils destroyed. We have not been able 

to confirm the Early Permian age for these rocks 

that was reported by Welsh and James (1961), who 

correlated them with the type Curry and Clinker 

Formations on South Mountain. There is a similarity of lithology and age between the Kessler Canyon 

Formation of the Rogers Canyon sequence, the unnamed upper quartzite unit of the Curry Peak 

sequence, and the Bingham Mine Formation of the 

Bingham sequence. Their separation is based largely 

on the structure discontinuities and their separation by the North Oquirrh and Midas thrust faults. 

The Grandeur Member of the Park City Formation, 

however, is restricted to the upper plate of the North 

Oquirrh thrust and is in the Rogers Canyon 

sequence. We find no rocks equivalent to the Kirkman Limestone or Diamond Creek Sandstone in the 

Bingham sequence. The formational units that have 

been correlated with the Kirkman Limestone and 

Diamond Creek Sandstone [type localities are in the 

Timpanogos sequence (Tooker and Roberts, 1963) 

in the Wasatch Mountains] and with the Clinker 

and Curry Formations of Welsh and James (1961) 

[type localities 'are on South Mountain], which 

Welsh and James (1961) reported in the Curry 

Peak sequence, are not considered here. Because of 

as yet incompletely understood internal structural 

and stratigraphic complexities, the irregular alteration of strata, and the scarcity of well-preserved 

fossils in Curry Peak sequence rocks and their superficial resemblance to rocks of the Rogers Canyon 

sequence, we defer further discussion of the stratigraphy of these lower plate rocks.

Tooker and Roberts (1961) mapped and described 

the stratigraphic units of the Rogers Canyon 

sequence at the north end of the Oquirrh Mountains. 

Changes in stratigraphic terminology of these rocks 

are summarized in figure 6. The informal recognition of seven mappable units of the Oquirrh Formation (Tooker and Roberts, 1961, p. 24) was subsequently revised (Tooker and Roberts, 1963, p. 

E33) into a lower, middle, and upper series of distinctive mappable units. The lower shale and limestone, tentatively called the Manning Canyon (?) 

Shale (Tooker and Roberts, 1961), was later designated an unnamed formation when the pre-Manning 

Canyon age of the shale was confirmed (Tooker and 

Roberts, 1963, p. E33). An unnamed unit was designated the Grandeur Member of the Park City Formation following the usage of Welsh and James 

(1961, p. 4).

REVISED UPPER PALEOZOIC STRATIGRAPHY

Revision of the Oquirrh Formation to the rank 

of Oquirrh Group and its subsequent division into 

lithologically distinct formational units in ttn 

Oquirrh Mountains permits us to make systematic 

regional stratigraphic correlations. Several correlative lithologic formational units have already been 

designated elsewhere. The Round Valley Limestone 

and Weber Quartzite in the Wasatch Mountains 

(Crittenden, 1959) represent the lower limestone 

and middle cyclical limestone, shale, and quartzite 

shelf facies of Pennsylvanian age. The Ely Limestone of eastern Nevada contains a similar lower 

limestone and overlying cyclic limestone, shale, and 

quartzite basin unit of Pennsylvanian age; thes^ 

beds in turn are overlain by the Arcturus Formation containing sandstone of Early Permian age (A . 

Brokaw, oral commun., 1964). The revision of th? 

stratigraphic division into two main sequences cf 

the Oquirrh Group in the Oquirrh Mountains, the 

Rogers Canyon and Bingham sequences, is briefly 

described in the following sections and is shown in 

figure 3. The type sections of the Rogers Canyon 

and Bingham sequences are designated, respectively, 

the Rogers, Black Rock, and Kessler Canyons, at the 

north end of the range, and the West, Middle, and 

Bingham Canyons, in the vicinity of the Bingham 

mining district. The type section of the Oquirrh 

Group is designated the composite of the type sections of its formations in the Bingham sequence.

ROGERS CANYON SEQUENCE

The Rogers Canyon sequence, named for the area 

of excellent exposures of these rocks in and adjr.- 

cent to Rogers Canyon at the northwest end of the 

range, is divided into four new formations. The 

Green Ravine Formation at the base is overlain by 

the Oquirrh Group, consisting of the Lake Poirt 

Limestone and the Erda and Kessler Canyon Formations. The Grandeur Member of the Park City 

Formation (Tooker and Roberts, 1963) overlies the
A10 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Oquirrh Group with apparent conformity, but there 

may have been an erosion interval separating them.

GREEN RAVINE FORMATION

The Green Ravine Formation, here named for 

exposures near the mouth of Green Ravine (fig. 4, 

section 8), is composed of a basal 290 feet of interbedded limestone and calcareous shale section overlain by more massive cherty and sandy limestone. 

The formation, whose previous informal designations are shown in figure 6, is exposed only in the 

core of the Kessler anticline (Roberts and Tooker, 

1961, p. 40). The type section of the formation is 

on the west side of Kessler Peak at the north end 

of the Oquirrh Mountains, south of the mouth of 

Green Ravine in the SE*4 sec. 1, T. 2 S., R. 4 W., 

and the NW^4 sec. 6, T. 2 S., R. 3 W., Garfield quadrangle, Utah.

The total thickness of the Green Ravine Formation is uncertain because the base is concealed by 

alluvium at the range front; a thickness of about 

1,400 feet was measured in the exposed part of the 

type section. The formation is conformably overlain 

by the Oquirrh Group.

The Green Ravine Formation is mostly a limestone and consists of two parts. The lower part is 

dominantly 1-2-foot-thick limestone beds and shale 

layers. The limestone is medium and dark gray to 

light olive gray or yellowish gray and is locally very 

fossiliferous; the shale is black and dark gray to 

olive gray. In the lowest part, variegated argillaceous limestone is composed of rounded medium-dark 

gray crystalline limestone "nodules" that are as 

much as 3 inches in average diameter; the nodules 

are embedded in a medium-light-gray silty to sandy 

carbonate matrix. The lower contacts of individual 

beds are commonly scoured and may indicate short 

erosion intervals. Thin beds and partings of shale 

between thicker limestone layers in the lowest exposed part of the formation locally show welldeveloped cleavage.

The upper part consists of medium-bedded to massive 2-3 foot-thick medium-gray locally fossiliferous 

limestone and banded nodular black cherty limestone 

at the base, and interbedded medium- to thickbedded fossiliferous limestone and thin- to mediumbedded argillaceous and fossiliferous limestone at 

the top. The upper contact of the formation is placed 

above a thick series of argillaceous and fragmentedfossil limestones that underlie a crossbedded limestone that contains quartz sand; this sandy limestone is characterized by brown-weathering wispy 

sand lenses or streaks in a gray limestone matrix 

a characteristic which is common in the cyclically 

bedded Lake Point Limestone of the Oquirrh Group.

TYPE SECTION OF GREEN RAVINE FORMATION (see fig. 4, section 8)

West side of Kessler Peak from 4,700-ft altitude in unnamed 

drainage south of KSL-TV television transmitter tramway 

line northeast across Green Ravine to unnamed drainage 

north of hill whose altitude is 5,244 ft, SEV± sec. 1, T. 2 S., 

R. 4 W., and 2VFR4 sec. 6, T. 2 S., R. 3 W., Garfield 

quadrangle, Utah

[Measured by K. W. Tooker and R. J. Roberts]

Thidtnens 

(ft)

Oquirrh Group:

Lake Point Limestone 

Conformable contact.

Green Ravine Formation:

12. Argillaceous limestone, limestone, cherty limestone, and bioclastic limestone, interbedded; 

medium to dark gray; weather medium gray 

to tan and buff; locally variegated; thin to medium bedded; clastic limestone is crossbedded; 

shale partings are found in the limestone; 

sparse layered chert nodules are present; 

limestones contain abundant brachiopods, 

corals, bryozoans, and crinoids (USGS colln. 

16333-PC, 21132-PC, 17144-PC, and 20254- 

PC) ______________________-_ 215

11. Limestone, medium-gray; weathers medium 

light gray to light gray; thin to medium 

bedded; locally platy; interbedded thinbedded cherty limestone, crossbedded bioclastic limestone, and argillaceous limestone; 

shale partings throughout unit; abundant 

productid brachipods, Caninia corals, and 

chaetetiform bryozoans (USGS colln. 27256- 

PC, 16331-PC, 17143-PC, 20253-PC, 27257- 

PC, 16330-PC, 20258-PC, 21131-PC, 21130- 

PC, 20248-PC, 16329-PC, 20249-PC, 21251- 

PC, 20250-PC, 20252-PC, and 16332-PC) __ 331

10. Cherty (banded) limestone, dark-gray; weathers light gray; thin to medium bedded; interlayered bioclastic limestone in basal part; 

black chert nodules present; abundant Caninia corals (USGS colln. 16335-PC) ___ 82

9. Limestone, dark-gray; weathers light gray; 

medium to thick bedded; interbedded thin 

arenaceous often bioclastic limestone, argillaceous limestone, shale, and black cherty 

limestone (nodules in bands and irregular 

lenses) ; sparse coral fauna. Lower half of 

unit is mostly covered slope; section crosses 

a fault of small but unknown displacement, 

and a small part of the section may be 

missing ______ ___ 500

8. Limestone and shale, interbedded; medium 

dark gray and gray; weather light gray; 

thin to medium bedded; bioclastic limestone 

limestone lenses and shale partings in the 

limestone. Unit is mostly covered 145
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH All

Thickness 

(ft)

7. Shale, dark-gray to black; weathers medium 

dark gray; thin bedded and fissile; calcareous.. Unit is mostly covered slope ______ 17

6. Shale and limestone, interbedded; dark gray 

. and black; weather light olive gray; thin to 

medium bedded; ferruginous stains along 

bedding; platy. Shale parts of unit are mostly covered slope. Abundant bryozoans, brachiopods, and crinoids in limestone layers 

(USGS colln. 20247-PC, 20246-PC, 20243- 

PC, 21129-PC, and 20228-PC) ________ 61

5. Limestone, yellowish-gray; weathers yellowish 

orange and tan; thick bedded; sparse lightgray chert nodules ________________ 8

4. Limestone intraformational conglomerate, 

medium-gray; matrix weathers dark yellow 

orange, and rounded limestone fragments 

weather light gray; medium to thick bedded; 

shale partings locally ______________ 5

3. Limestone and arenaceous and argillaceous 

limestone, interbedded; light gray and light 

olive gray; weather grayish orange; thin 

bedded ________________________ 34

2. Bedded chert, pale-yellowish-brown; weathers

olive gray and grayish orange ________ 2

1. Arenaceous limestone, olive-gray; weathers 

light olive gray; thin bedded; locally contains 

brownish-gray chert lenses in upper part _ 17

Total thickness measured 

Covered at base by alluvium, faults.

1,417

The Green Ravine Formation contains an abundant, well-preserved brachiopod, coral, and bryozoan 

fauna of Late Mississippian (fairly early to late 

Chester) age. Mackenzie Gordon, Jr., and H. M. 

Duncan in the section on biostratigraphy and correlation list and discuss details of fossil collections 

from the type locality, their biostratigraphic relations, and correlation with similar rocks elsewhere. 

They separate the formation into three parts: a 

pre-Caninia Zone containing a predominantly bryozoan-brachiopod fauna; the Caninia, Zone with 

corals and chaetetiform bryozoans predominant; 

and a post-Caninia Zone with brachiopods predominant. These rocks may be correlative with those 

in the upper part of the Great Blue Limestone in 

the Bingham sequence near the Ophir mining district and with those in the lower part of the Doughnut Formation in the Mount Raymond sequence 

(Tooker and Roberts, 1963) in the Wasatch Mountains. The Green Ravine, however, is neither lithologically similar to the Great Blue Limestone nor 

to the overlying Manning Canyon Shale in the type

localities. The lower part may correlate with one 

of the shaly units of the Great Blue Limestone.

OQUIRRH GROUP

The Oquirrh Group in the Rogers Canyon 

sequence consists of three new formations: the Lake 

Point Limestone and the Erda and Kessler Canyon 

Formations.

LAKE POINT LIMESTONE

The Lake Point Limestone is here named for the 

small farming community of Lake Point immediately south of the Great Salt Lake; the nearby 

northwestern ridge of the Oquirrh Mountains in the 

Mills Junction and Garfield quadrangles is also 

called Lake Point. These rocks previously were 

designated an unnamed unit, which subsequently 

was informally referred to as the lower member of 

the Oquirrh Formation (fig. 6). The rocks crop out 

in the core of the Kessler anticline 1 mile east of 

Lake Point, on the north side of Lake Point Ridge, 

in the upper part of Bates Canyon, on the upper 

plate of the North Oquirrh thrust fault at Nelson 

Peak, and in small downfaulted klippen on the lower 

plates of the thrust near the mouth of Bates Canyon 

(Tooker and Roberts, 1961, pi. 6; Welsh and James, 

1961, pi. 2).

The type section of the formation is on the west 

side of Kessler Peak and extends from the bottom 

of an unnamed ravine at an altitude of 5,200 feet 

northeastward to near the top of the hill whose 

altitude is 6,231 feet in the NE*4 sec. 6, T. 2 S., R. 

3 W., and SW^ sec. 31, T. 1 S., R. 3 W., of the 

Garfield quadrangle, Utah (fig. 4, section 8). The 

formation is 1,700 feet thick in the core of the Kessler anticline. The Lake Point Limestone conformably ( ?) overlies the Green Ravine Formation and is 

conformably overlain by the Erda Formation. The 

upper contact is at the base of the lowest red-brownweathering quartzite bed in the Erda Formation.

The rocks are chiefly interbedded medium-gray 

light-gray- to tan-weathered medium-grained thinto medium-bedded limestone and massive (thickbedded) gray limestone; locally the limestone is 

cherty and contains bioclastic sand material in crossbedded arenaceous layers, thin-bedded to parting 

(very thin) argillaceous layers, and carbonaceous 

shale beds and partings. The lower 350 feet consists 

mostly of 1-3-foot-thick shale partings and shaly 

limestone intervals in dense platy medium-bedded 

limestone and arenaceous limestone that locally are 

cherty and very fossiliferous. The beds in the upper 

1,387 feet contain more-massive detrital cliff-form-
A12 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

ing limestone and interformational conglomerate 

with interbedded cherty, argillaceous, bioclastic 

limestone and calcareous sandstone and sparsely 

fossiliferous limestone beds (figs. 7, 8). A typical 

sedimentary cycle consists of a lower predominantly 

shaly or argillaceous limestone unit that is succeeded 

by a dominantly clastic calcareous (often bioclastic) 

sandstone, a calcitic arenaceous limestone, a crossbedded wispy quartz and calcitic arenaceous limestone, and a cherty limestone. The cycle is generally 

completed by a bedded chert layer.

TYPE SECTION OP LAKE POINT LIMESTONE (see fig. 4, section 8)

Southwest ridge of hill where altitude is 6£31 feet, from 

5,200-ft altitude to about the 6,160-ft altitude in NEV^ sec 6, 

T. 2 S., R. 3 W., and SW% sec. 31, T. 1 S., R. 3 W. 

Garfield quadrangle, Utah

[Measured by E. W. Tooker and R. J. Roberts]

Oquirrh Group:

Erda Formation. 

Conformable contact. 

Lake Point Limestone:

12. Arenaceous limestone, dark-gray; weathers 

light gray; thin to medium bedded; 

interlayers of thin argillaceous limestone, 

black nodular cherty limestone, and bioThicTcness 

(ft)

Thickness

(ft)

clastic limestone; sparse brachiopod 

fauna __________________ 71

11. Argillaceous and arenaceous limestone and 

interbedded shale; dark gray; weather 

medium gray; thin to medium bedded; 

local bioclastic limestone and carbonaceous shale partings and lenses; nodular 

black chert layers; shale layers produce 

mostly covered slope (USGS colln. 

23855-PC) __________________ 79

10. Calcareous sandstone, medium-gray; weathers reddish brown to buff; medium 

bedded; crossbedded; light-tan chert 

nodules ______ _ _ 6

9. Limestone, argillaceous limestone, arenaceous limestone, and cherty limestone, interbedded; medium gray to dark gray; 

weather tan to light gray; medium bedded; subordinate lenses and thin beds of 

carbonaceous shale, and banded and 

crossbedded calcareous sandstone and 

bioclastic limestone; black chert nodules 

and lenses. Unit locally forms cliffs; locally is fossiliferous (USGS colln. 23854- 

PC) _______________________ S99

8. Chert and interbedded argillaceous limestone partings and layers; medium gray; 

weather yellowish brown ________ 3

FIGURE 7. Typical exposures of Rogers Canyon sequence. View eastward between Rogers and Big Canyons, west side of 

the north end of the Oquirrh Mountains. Included are the basal Green Ravine Formation and the Oquirrh Group, 

consisting of the Lake Point Limestone and Erda and Kessler Canyon Formations. Also indicated are the Bonneville 

and Provo shore levels of Lake Bonneville, the Kessler anticline, the Lake Point thrust fault underlain by Erda 

Formation strata, and points a, b, and c shown in figure 8.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A13

7. Limestone, arenaceous limestone, and argillaceous limestone, interbedded; medium to dark gray; weather light gray to 

tan and yellowish brown; thin to medium 

bedded; locally massive; fossiliferous 

limestone and carbonaceous shale partings; locally thin crossbedded bioclastic 

limestone; black chert nodules in layers 

and lenses; abundant, brachiopods, 

corals, and bryozoans (USGS colln. 

17150-PC, 17148-PC, 17149-PC, and 

16324-PC) __________________ 426

6. Arenaceous limestone, light-gray; weathers 

brown to tan; medium bedded; medium 

grained ____________________ 11

5. Limestone, dark-gray; weathers light gray; 

medium bedded; interlayered thin bedded 

argillaceous limestone, carbonaceous 

shale, and crossbedded bioclastic limeFIGURE 8. General features of the lithology of the lowermost 

part of the Lake Point Limestone. View northeast up ridge 

between Green Ravine and Rogers Canyon. General location 

of reference points a, b, and c is shown in figure 7.

Thickness

(It)

stone; irregular layers of nodular black 

chert in limestone; abundant, brachiopods, corals, and bryozoans (USGS colln. 

16323-PC, 17147-PC, 16322-PC, and 

16319-PC) ___________________ 154

4. Fossiliferous limestone, dark-gray; limestone weathers medium gray, corals 

weather brown; medium bedded; Orygmophyllum! (colonial coral) (USGS 

colln. 16318-PC, 17146-PC, and 20259- 

PC) ____________________ 5

3. Limestone, variegated medium- and darkgray; weathers light gray and tan; fine 

grained; thin to medium bedded; arenaceous limestone and shale layers and 

partings; brachiopods abundant (USGS 

colln. 21140-PC) _______________ 48

2. Limestone, medium-gray; weathers yellowish tan to light gray, locally irregularly 

variegated light gray and medium gray; 

medium bedded to massive; cliff former; 

contains shale partings. Thin greenweathering chert layers at top contain 

Rhipidomella nevadensis (USGS colln. 

21139-PC and 21141-PC) ________ 98

1. Limestone, argillaceous limestone, and arenaceous limestone, interbedded; medium 

gray; limestone and argillaceous limestone weather light to medium gray, and 

arenaceous limestone weathers tan; thin 

to medium bedded; locally crossbedded. 

Upper 85 ft of unit contains mediumbedded limestone intraformational conglomerate that consists of medium-darkgray limestone clasts in tannish-gray 

limestone matrix; forms cliffs above a in 

figure 8. Lower beds of unit contain the 

first appearance of brown-weathered 

quartz grains set in light-gray carbonate 

matrix (characteristic of arenaceous 

limestones above the Green Ravine Formation). Local chert nodules and shale 

layers and partings occur throughout 

unit. Brachiopods locally abundant 

(USGS colln. 16340-PC, 17145-PC, 

21134-PC, 21135-PC, 17031-PC, 21139- 

PC, 21138-PC, and 21137-PC) ______ 437

Total thickness measured _______ 1,737 

Conformable contact. 

Green Ravine Formation.

The Lake Point Limestone locally contains an 

abundant, generally well-preserved silicified brachiopod, coral, and bryozoan assemblage. The positions of the collections are shown in the stratigraphic section and in table 2. In their detailed discussions, Gordon and Duncan have delineated two 

faunal zones, the Rhipidomella nevadensis Zone in
A14 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

the lower part of Late Mississippian (late Chester) 

age, and the Rugoclostus Zone in the upper twothirds of Early Pennsylvanian (Morrow) age. An 

intermediate, poorly fossilized shaly limestone zone 

within the Rhipidomella, nevadensis Zone contains 

specimens of Archimedes, which resemble those in 

the Manning Canyon Shale of the Bingham sequence. 

Thus Gordon and Duncan correlate the lower part 

with Upper Mississippian rocks and the upper part 

with Lower Pennsylvanian strata, the actual boundary lying within unit 3 of the type section.

The faunas indicate, therefore, that the lower 540 

feet of the Lake Point Limestone is of Late Mississippian age and that it is equivalent in age to parts 

of the Manning Canyon Shale in the Bingham and 

Timpanogos sequences and to the upper part of the 

Doughnut Formation in the Mount Raymond 

sequence (Tooker and Roberts, 1963, p. E35). The 

uppermost 1,200 feet is of Early Pennsylvanian age 

and is believed to be correlative with the lower part 

of the Oquirrh Group in the Bingham sequence and 

with the Round Valley Limestone in the Mount 

Raymond sequence. No break in the pattern of sedimentation between Mississippian and Pennsylvanian 

time has been recognized in the Rogers Canyon 

sequence. This Lake Point Limestone section is a 

continuous series that includes rocks of both Mississippian and Pennsylvanian age.

ERDA FORMATION

The Erda Formation of the Oquirrh Group is 

here named for the Erda siding on the Union Pacific 

Railroad; this siding is west of the mouth of Bates 

Canyon and immediately southwest of the prominent cliff exposures of these rocks on the west sides 

of Kessler, Coon, and Nelson Peaks in the Mills 

Junction and Garfield quadrangles, Utah (fig. 4, 

section 8). These rocks had previously been included 

in the middle member of the Oquirrh Formation 

(fig. 6). The .formation is well exposed along the 

north and west sides of the range and is lithologically similar to altered rocks exposed on the pediment 2 miles west of the range at Adobe Rock near 

Mills Junction (Tooker and Roberts, 1961, pi. 6). 

Erda Formation strata are also exposed in the 

structurally discordant lower plates of the Lake 

Point thrust fault at the range front (fig. 7) north 

of Green Ravine (Roberts and Tooker, 1961, p. 45). 

The rocks dip steeply northward and are locally 

overturned to the south on the north side of the 

range (Roberts and Tooker, 1961, p. 39); south of 

Lake Point, on the western side of the range, the 

strata are exposed in the Mills Junction syncline,

the Kessler anticline, and the Coyote and Bates synclines. The exposures extend southward in a sinuous line as far as Bates Canyon, where they end 

against the North Oquirrh thrust fault. The Erda 

Formation is cut off east of the crest of the range 

by the Garfield fault.

The type section of the Erda Formation is on the 

west side of Kessler Peak and extends from the hill 

that is 6,231 feet in altitude northward across the 

center of sec. 31, T. 1 S., R. 3 W., Garfield quadrangle, Utah, crossing Rogers Canyon, up toward 

the ridge point that is 7,521 feet in altitude on Lake 

Point Ridge as far as the 6,800-foot contour. Here 

the formation is 3,606 feet thick and is conformably 

overlain by the Kessler Canyon Formation. The 

upper contact of the Erda is at the base of the first 

thick tan-brown-weathering, cliff-forming quartzite 

unit (fig. 6; Tooker and Roberts, 1961, p. 30) below 

the interbedded calcareous quartzite, orthoquartzite, 

and ferruginous sandstone beds that characterize 

the Kessler Canyon Formation.

The Erda Formation is characterized by cyclically 

repeated layers of medium-gray limestone and medium-dark-gray ledge-forming argillaceous limestone 

and light-brown slope-forming carbonaceous shale, 

cinnamon-brown to tan calcareous quartzite, and 

variegated tan and light-brown crossbedded calcareous sandstone (fig. 9). These rocks stand in marked 

contrast to the predominantly grayish limestone 

beds below and massive red-brown-weathered quartzite layers above. The quartzite and limestone beds 

crop out as prominent ribs along gentle slopes or as 

cliffs on steep slopes. The shale and argillaceous 

limestone form intervening covered slopes. Cyclically repeated thin beds that are as much as 1 foot 

thick occur in the lower part of the section (Tooker, 

1962, p. 357), whereas these beds are medium to 

thick (2-4 ft) in the middle and upper parts of the 

section. However, in individual beds within each 

major cycle, minor repetitions are observed. For 

example, a limestone bed 2 feet thick is often composed of thin repetitive layers of sandy limestone 

(containing detrital quartz, clastic limestone, and 

fossil-fragment sands), cherty limestone, and argillaceous limestone. A comparable shale bed commonly contains thin dense arenaceous limestone, 

bedded chert, and calcareous quartzite layers and 

lenses; and a similar quartzite bed commonly contains limestone and shale partings separating individual quartz laminae. A complete major cycle may 

be 60-100 feet thick.

Silica-cemented quartzite (quartzose sandstone or 

orthoquartzite) is not abundant and commonly
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A15

FIGURE 9. Upper two-thirds of the Erda Formation and the basal part of the Kessler Canyon Formation. Views nortb 

of Rogers Canyon; point X is common to both photographs. The cyclic lithology of the Erda Formation can be seen. 

The massive quartzite beds (dark gray) at the base of the Kessler Canyon Formation are exposed at the top of the 

ridge. Z indicates three-layer limestone marker unit 4. Point Y locates unit 25, light-gray crinoid marker bed at the 

top of prominent cliff-forming cherty limestone.
A16 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

grades into calcareous sandstone. This calcareous 

sandstone contains detrital limestone and calcite 

grains in addition to quartz and feldspar and is 

cemented by calcite and silica cement. The rock is 

hard and fractures conchoidally. It effervesces in 

weak acid and weathers to a sandy, locally punklike 

surface as much as half an inch thick.

Limestone ranges from a dense fine-grained apparently precipitated rock to a crossbedded, coarsegrained, clastic rock. Irregular layers and lenses of 

chert nodules are common, and shale partings are 

abundant. Most of the interbedded shale is carbonaceous and generally grades vertically into argillaceous limestone.

Argillaceous and cherty limestones in the Erda 

Formation are abundantly fossiliferous; the fossils 

consist of brachiopods, bryozoans, corals, fusulinids, 

gastropods, and crinoids. In general fossils are less 

abundant and less well silicified in the Erda Formation than they were in the Lake Point Limestone.

TYPE SECTION OF ERDA FORMATION (see fig. 4, Section 8)

Traverse south to north across the center of sec. 31, T.I S., 

R. 3 W., Garfield quadrangle, Utah

[Measured by K. W. Tooker and R. J. Roberts]

Thickness 

(ft)

Oquirrh Group:

Kessler Canyon Formation.

Conformable contact.

Erda Formation.

35. Cherty limestone, dark-gray; weathers medium gray; thin to medium bedded in 

lower part, medium to thick bedded in 

upper part; black chert nodules and 

lenses; carbonaceous shale partings. 

Middle part of unit is medium-gray platy 

argillaceous limestone ___________ 147

34. Calcareous quartzite, quartzose sandstone, 

and limestone, interbedded; gray brown 

and medium gray; weather brownish tan 

and light gray; banded; medium bedded 

to massive; locally crossbedded. Quartzite and sandstone contain thin argillaceous limestone and carbonaceous shale 

layers and partings _____________ 267

33. Cherty limestone, dark-brownish-gray; 

weathers light gray to tan ; thin to medium bedded; black chert nodules and layers. Middle part of unit contains argillaceous platy limestone 2-6 in. thick _ 93

32. Calcareous quartzite, light-brownish-gray; 

weathers light grayish brown; medium 

bedded to massive _____________ 48

31. Argillaceous limestone, dark-gray; weathers light grayish brown and tan; thin to 

medium bedded; in many places, platy _ 39

Thickness 

(ft)

30. Calcareous sandstone, brown-gray; weathers medium grayish tan to red brown; 

occurs as massive beds __________ 82

29. Limestone and argillaceous limestone, interbedded; light to dark gray; weather 

to tan- and gray-striped beds; thin bedded to massive; locally black chert nodules ; chert, fissile shale, and quartz sandstone partings ________________ 122

28. Calcareous quartzite, light-grayish-brown; 

weathers tan brown; medium bedded. 

Unit contains a thin-bedded 4-ft gray 

limestone at 16 ft _____________ 111

27. Limestone and cherty limestone, interbedded; dark gray; weather medium light 

gray; medium to thick bedded; locally 

black chert nodules in the upper limestone layers; locally fossiliferous (USGS 

colln. 20232-PC, 20235-PC, 20236-PC, 

and f22568) _________________ 160

26. Calcareous sandstone, brownish-gray; 

weathers tan to rusty brown; thick bedded; well jointed; sparsely crossbedded^

25. Crinoidal limestone, medium-light-gray; 

weathers light gray; thin bedded; interlaminated thin sandstone and chert layers and lenses; bryozoans at base (USGS 

colln. 16328-PC) _____________________

24. Cherty limestone and limestone, interbedded; dark gray; weather medium light 

gray; thin to medium bedded; interlayers 

of bioclastic limestone and shale; locally fossilif erous (USGS colln. f 22570)

18

38

23. Cherty limestone, limestone, arenaceous 

limestone, and argillaceous limestone, interbedded; medium gray; weather medium light gray; thin to medium bedded; 

abundant thin shale partings; local bioclastic limestone layers; bryozoan and 

fusulinid fauna in upper part ____ _ .________ 140

22. Argillaceous limestone, arenaceous limestone, and limestone, interbedded; medium gray to brownish gray; weather to 

light brown gray and gray on fluted 

crossbedded surfaces; bioclastic limestone and shale layers and partings; 

sparse black chert nodules at base, increase upward in section _________ 90

21. Carbonaceous shale and argillaceous limestone, interbedded; medium gray ; weather dark brownish gray; thin bedded to 

platy. Unit is poorly exposed on covered 

slope ______________________ 13

20. Calcareous quartzite, light-brown; weathers tan to rusty brown; crossbedded __ 12

19. Cherty limestone, arenaceous limestone, 

limestone, argillaceous limestone, and 

fine-grained limestone, in sequence up-
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A17

Thickness

(ft)

ward; medium gray; weather brownish 

gray, slate-gray to light-gray and tan 

bands; thin to medium bedded; local 

layers of gnarly black chert nodules; 

local bioclastic limestone and shale partings; Prismopora (bryozoan), corals, 

brachiopods, and fusulinids abundant 

(USGS colln. 17165-PC and 17166-PC)_ 85

18. Calcareous quartzite, light-gray; weathers 

tan to reddish brown; medium to thick 

bedded; thin crossbedded calcareous 

sandstone parting layers; buff and black 

chert pods 1-6 in. thick _________ 74

17. Limestone, dark-gray; weathers to grayand tan-striped plates; argillaceous at 

base, more arenaceous and cherty in upper part ____________________ 145

16. Calcareous quartzite, light-brown-gray; 

weathers light brown; thin bedded to 

laminar; limestone partings; local chert 

pods _____________________ 43

15. Cherty limestone and shale, interbeddcd; 

dark gray; weather medium light gray 

and tan; thin bedded; calcareous sandstone and carbonaceous shale partings in 

limestone; local chert nodule layers; fossiliferous; productid brachiopod zone __ 136

14. Limestone, shale, and calcareous sandstone, 

interbedded; dark gray; weather to tan, 

light-gray, and dark-gray bands; thin to 

medium bedded; thin layers of gnarly 

black chert nodules and layers; argillaceous limestone layers and shale partings locally; spiriferid brachiopods in 

upper part (USGS colln. 16327-PC) __ 46

13. Limestone, cherty limestone, and carbonaceous limestone, interbedded; dark 

dark gray and black; weather light to 

medium bedded; upper 40 ft mainly arthin to medium-bedded limestone and 

finely laminated platy shale; black irregular chert nodule layers and lenses. Shale 

part of unit forms covered slopes. Fossils occur locally throughout limestone 

parts, zone of Desmoinesia muricatina 

(USGS colln. 17164-PC, 16325-PC, and 

16326-PC) __________________ 303

12. Calcareous quartzite, tan; weathers tan to 

brown; thin to medium bedded; interbed thin argillaceous limestone _____ 71

11. Argillaceous limestone, limestone, and arenaceous limestone, interbedded; dark 

gray and gray to brown gray; weather 

light grayish tan and brown; thin to 

medium bedded; upper 40 ft mainly argillaceous; thin layers and lenses of calcareous sandstone and carbonaceous 

shale partings spaced irregularly 

throughout unit; black chert nodules and

Thickness 

(ft)

lenses occur throughout unit; rocks are 

locally fossiliferous (USGS colln. 

17163-PC) __________________ 112

10. Limestone, black cherty limestone, and arenaceous limestone, interbedded; medium 

dark gray; weather light gray and tan; 

banded; medium to thick bedded; fossiliferous (USGS colln. 17159-PC, and 

17161-PC) __________________ 140

9. Calcareous quartzite, light-brown-gray; 

weathers brown to tan; medium bedded at 

base, massive in upper part; interbedded 

calcareous sandstone and arenaceous 

limestone; locally crossbedded; black 

chert nodules in basal layers ______ 56

8. Limestone, medium-dark-gray; weathers 

medium light gray; medium to thick bedded; locally platy and argillaceous; 

carbonaceous shale partings; sparse 

black chert nodule layers; fossiliferous 

(USGS colln. 17158-PC) _________ 90

7. Bedded black chert; limestone partings __ 6

6. Limestone, dark-gray; weathers light gray; 

thin bedded at base and medium to thick 

bedded in upper part; black chert nodules; arenaceous and argillaceous limestone layers and partings; sparse fossils 

(USGS colln. 17157-PC) _________ 193

5. Calcareous quartzite, tan; weathers tan to 

buff and brown; banded; crossbedded; 

interlayered thin limestone and chert in 

lower one-third of unit __________ 71

4. Fossiliferous limestone, arenaceous limestone, cherty limestone, argillaceous limestone, and calcareous quartzite, interbedded; olive gray and medium gray to 

brownish gray; weather light gray and 

brown; thin to medium bedded. Unit 

forms prominent three-layer light-grayweathering marker unit. Clastic limestone and quartzite are commonly crossbedded. Carbonaceous shale, thin chert, 

and bioclastic limestone form parting 

layers within beds. Unit is locally fossiliferous; large horn corals, brachiopods, and crinoids abundant in the top 

22 ft and in the middle part (USGS 

colln. 17155-PC and 17156-PC) _____ 119

3. Limestone, arenaceous limestone, argillaceous limestone, and calcareous sandstone, 

interbedded; light olive gray and medium dark gray; weather to variegated 

grayish orange and tan and light gray; 

thin to medium bedded; thin crossbedded 

sand layers and shale partings. Thin- to 

medium-bedded interformational conglomerate in middle part of unit. Fossiliferous at top; fauna includes Profustdinella (USGS colln. 17154-PC and 

f20486) ____________________ 131
A18 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Thickness

(ft)

2. Fossiliferous limestone, argillaceous limestone, and cherty limestone, interbedded; 

tan and olive gray to dark gray; weather yellowish gray to light gray; thin to 

medium bedded; crossbedded arenaceous 

limestone, thin carbonaceous shale, black 

chert, and calcareous sandstone parting 

layers and lenses. Fossils include spiriferid and productid brachiopods, bryozoans, and corals ___________ 57

1. Quartzite and calcareous quartzite, interbedded; light tan to light gray; weather 

grayish brown to reddish brown; thin 

(1-2 in. thick) to medium bedded; locally 

crossbedded bioclastic limestone layers 

and argillaceous limestone partings. Unit 

locally forms cliffs and contains interbedded limestone, black nodular cherty 

limestone, and arenaceous limestone, 

which are medium gray to light brown, 

weather light gray to brown, are thin to 

medium bedded, and are locally massive 

(up to 5 ft thick). Fossils locally abundant, include brachiopods and Chaetetes 

(USGS colln. 16334-PC, 17151-PC, 

17152-PC, and 17153-PC) __________ 344

Total thickness measured ________ 3,606 

Conformable contact. 

Oquirrh Group, Lake Point Limestone.

Fossil faunas from the Erda Formation, which 

are listed in table 3 and are described in detail by 

Gordon and Duncan, consist of several faunal assemblages that include brachiopods, corals, bryozoans, and fusulinids of Middle Pennsylvanian age. 

These strata, therefore, are approximate age equivalents of the lower and middle parts of the Oquirrh 

Group in the thick Bingham and Timpanogos 

sequences in the Oquirrh and Wasatch Mountains 

and of the thin Weber Quartzite in the Mount Raymond sequence in the Wasatch Mountains (Tooker 

and Roberts, 1963 >.

KESSLER CANYON FORMATION

The Kessler Canyon Formation of the Oquirrh 

Group is here named for the most prominent northflowing stream at the north end of the Oquirrh 

Mountains in the Garfield quadrangle. These rocks 

previously were designated informal units and subsequently were included in the upper member of the 

Oquirrh Formation (fig. 6). The formation is exposed on both sides of the Garfield fault (Tooker 

and Roberts, 1961, pi. 6). West of the fault, the 

lower part of the formation crops out on northfacing dip slopes on the north flank of the Kessler

anticline and as south-dipping beds on the ridge 

east of the Garfield smelter at the north end of the 

range. On the upper slopes of Coon Peak in the 

Coyote and Bates synclines, the lower and ruddle 

parts of the Kessler Canyon Formation are exposed. 

The upper part of the formation is exposed throughout the area east of the Garfield fault and noHh of 

the North Oquirrh thrust, where it forms symmetrical low-amplitude folds. Because of interruptions in exposures, the type section is in two parts 

(fig. 4, sections 9a and 9b). The lower l,03f feet, 

section 9a, (Tooker and Roberts, 1961, p. 30) was 

measured on the west side of Black Rock Canyon 

in a traverse from the NE^4 SE^i sec. 30, T. 1 S., 

R. 3 W., northwest to the ridge at the south edge of 

NE^4 sec. 30. The upper 3,436 feet, section 9b, 

(Tooker and Roberts, 1961, p. 30) was measured in 

Kessler Canyon southeast from the center SE*4 sec27, T. 1 S., R. 3 W., at an altitude of 5,400 feet, 

across the hill whose altitude is 5,984 feet and 

across the tributary to Little Valley Wash to the 

hilltop west of the hill whose altitude is 5,341 feet 

in the center of the west side NE*4 sec. 35, T. 1 N., 

R. 3 W. The upper contact is at the base of a prominent light-gray-weathering abundantly fossiliferous 

limestone containing a well-preserved brachiopod, 

coral, bryozoan, and crinoid assemblage (Tooker 

and Roberts, 1961, p. 31).

The lower third of the Kessler Canyon Formation 

is predominantly interbedded massive orthotuartzite and cherty limestone, and the upper two-thirds 

is ferruginous and dolomitic sandstone, dolomite, 

and fusulinid-bearing chert. The orthoquarteite is 

light gray tan and weathers tan and light brown to 

orange brown; it is fine grained to sandy, medium 

bedded to massive, generally well jointed, locally 

well banded, commonly crossbedded, and often contains interbedded calcareous, ferruginous, or dolomitic sandstone and shale partings. Thin (1 ft or 

less) chert layers and lenses occur locally in the 

section. The cherty limestone is light gray, thin 

bedded, and contains either black or tan chert 

nodules.

The upper part of the formation is poorly exposed; the beds are thin- to medium-bedded interbedded orthoquartzite, calcareous, ferruginous and 

dolomitic sandstone and dolomite, in contrast to 

thick silica-cemented orthoquartzite and cherty 

limestone in the lower part of the formation. Some 

dolomite beds are now sedimentary breccia. Worm 

trails are common in the ferruginous sandstorm, and 

poorly preserved fusulinids occur both in ck^omite 

and in bedded chert layers.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A19

The true thickness of the formation is uncertain 

because the upper part of the measured section 

crosses the Arthur fault (Roberts and Tooker, 1961, 

p. 44). Although the relative displacement on the 

fault initially did not appear to be large, subsequent 

geologic mapping suggests that as much as 1,500 

feet of section may be cut out at this point. Thus the 

total thickness of the Kessler Canyon Formation is 

probably in excess of 4,300 feet.

TYPE SECTION OF KESSLER CANYON FORMATION

(see fig. 4, section 9b)

Center SE^A sec. 27, T. 1 S., R. 3 W., southeast to center west 

side NEK sec. 35, T. 1 S., R. 3 W., Garfield quadrangle, Utah

[Measured by B. W. Tooker and R. J. Roberts]

Thickness 

(ft)

Park City Formation:

Grandeur Member. 

Conformable contact. 

Oquirrh Group:

Kessler Canyon Formation (upper part) :

37. Dolomitic limestone and interbedded sandstone, calcareous quartzite, and shale; 

light gray and tan; weather dark brown 

and orange; thin to medium bedded; 

limestone brecciatcd locally. Unit is poorly exposed. Fusulinids collected in sandstone from the same unit nearby (USGS 

colln. f21018) ________________ 260

36. Calcareous quartzite and ferruginous sandstone, interbedded; tan and medium 

brown; weather brown and dark brown; 

medium bedded; locally crossbedded; 

sparse bedded chert; worm trails in sandstone; locally chert contains poorly preserved fusulinids) _____________ 250

35. Calcareous sandstone and calcareous 

quartzite, dolomitic limestone and ferruginous sandstone, interbedded. Unit is 

covered slope _______________ 270

34. Calcareous quartzite, arenaceous dolomitic 

limestone, and ferruginous sandstone, 

interbedded; tan to buff and gray; 

weather light to dark brown and light 

gray; medium bedded; dolomitic limestone is locally brecciated; worm trails 

occur in sandstone; brachiopods in thin 

dolomitic limestone layers. Unit is mostly 

covered. Normal fault of unknown displacement at 565 ft may cut out as much 

as 1,500 ft of section ____________ 568

33. Fusulinid chert; interbedded dolomitic

limestone and calcareous sandstone __ 12

32. Calcareous quartzite, tan; weathers olive

brown. Unit is covered slope ______ 29

31. Fusulinid chert, poorly exposed ______ 10

Thickness 

(ft)

30. Dolomitic sandstone, light-gray, platy to 

thin-bedded; interbedded calcareous 

quartzite; sparse, poorly preserved fusulinids; exposures poor __ 36

29. Fusulinid chert, light-gray; weathers light 

to dark brown; weathered surface is 

pitted; fusulinids collected from unit 1 

mile north (USGS colln. f20479) ____ 13

28. Calcareous quartzite, dolomite, arenaceous 

dolomite, dolomite breccia, interbedded; 

tan gray and light gray; weather tan to 

buff and light brown; locally variegated 

pink to gray green; thin bedded. Weathered quartzite is pitted and punky at the 

rock surface; black chert nodules and 

lenses occur in arenaceous dolomite. Unit 

is poorly exposed on covered slopes _ 253

27. Arenaceous dolomitic limestone, dolomite 

breccia, ferruginous sandstone, and calcareous quartzite, interbedded; very 

poorly exposed ____ __ 94

26. Ferruginous sandstone and brecciated arenaceous dolomitic limestone, interbedded; 

tan and light gray; weather light brown 

and buff; locally cherty; pitted weathered surface on thin interbedded calcareous quartzite; poorly preserved bryozoans and brachiopods in limestone, and 

worm trails in sandstone. Unit is poorly 

exposed ______-____ 63

25. Calcareous quartzite, tan to buff; weathers 

dark red brown; thin to medium bedded; 

interbedded thin ferruginous sandstone 

and fusulinid chert layers. Section 

crosses small normal fault at base with 

unknown but small displacement ____ 74

24. Arenaceous dolomitic limestone, light-tan; 

weathers light gray to buff; medium 

bedded; contains coarse crinoidal sand 

stringers. Unit contains medial layer of 

thick calcareous quartzite. Cherty fusulinid layers occur near the base _ _ 48

23. Ferruginous sandstone, yellow-brown; 

weathers to medium dark brown with 

soft punky surface; interbedded thin 

hard ribs of orthoquartzite. Unit is 

poorly exposed on slopes _ - 69

22. Limestone, light-gray; weathers buff; thin

bedded; poorly preserved fusulinids ____ 3

21. Calcareous quartzite, ferruginous sandstone, dolomitic sandstone, and orthoquartzite, interbedded; tan and light 

gray; weather buff and limonite brown; 

thin to medium bedded; often platy; 

quartzite is pitted, and sandstone is 

punky on weathered surfaces. Locally, 

there are7 bedded chert layers. At 92 ft 

unit contains poorly preserved fusulinids. 

Unit is most covered (USGS colln. 

f22588) ________________-_ 288
A20 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Thickness 

(ft)

20. Fusulinid chert with crinoid steins; white;

pitted; fusulinid molds only ______ 1

19. Calcareous quartzite, calcareous and ferruginous sandstone, and cherty dolomite, 

interbedded; light gray and tan to light 

brown; weather light gray to tan, locally reddish brown. Beds are thin to 

medium bedded and are locally color 

banded. Locally, weathered surfaces of 

quartzite are pitted and form a thick 

punky surface rind. Dolomite breccia 

beds 1-6 ft thick are interspersed 

throughout the unit, and two thin fusulinid chert beds occur in the top 40 ft. 

Unit is poorly exposed and mostly covered _________________________________ 395

18. Orthoquartzite, calcareous quartzite, and 

calcareous sandstone, interbedded; light 

gray; weather banded light gray and 

buff; locally consist of coarse sand; 

pitted weathered surfaces. Unit poorly 

exposed ______________________________

17. Orthoquartzite and calcareous quartzite, 

interbedded; light gray to tan; weather 

light to medium brown and dark brown 

in prominent alternating bands; pitted 

weathered surface that locally appears 

to have ropy contortions; thin bedded 

and platy; contain ferruginous and calcareous sandstone and cherty limestone 

interlayers and partings; worm trails in 

ferruginous sandstone near top of unit. 

Lower half of unit is covered slope ___

61

639

Total thickness measured _____ __ 3,436 

Oquirrh Group, Kessler Canyon Formation (lower part) .

TYPE SECTION OF KESSLER CANYON FORMATION

(see fig. 4, section 9a)

sec. 30, T. 1 S., R. 3 W., to center south 

sec. 30, Gar field quadrangle, Utah

Thickness 

(ft)

[Measured by E. W. Tooker and R. J. Roberts]

Fault.

Oquirrh Group:

Kessler Canyon Formation: 

Upper part:

17. Calcareous quartzite and Orthoquartzite, 

interbedded; medium brown gray to 

tan; locally banded; weather brown on 

pitted surfaces; thin to medium bedded; thin calcareous and ferruginous 

sandstone layers and partings ______ 224

Total of upper part _________ 224

Thickness 

(ft)

Lower part:

16. Limestone, argillaceous limestone, anc1 

arenaceous limestone, interbedded; tar 

gray; weather yellow brown; thin bedded; jointed; locally, chert nodule layers at base 33

15. Cherty limestone and interbedded arenaceous limestone ___ 22

14. Calcareous quartzite, Orthoquartzite, ferruginous sandstone, and cherty lime-- 

stone, interbedded; light gray to gray 

brown; weather dark brown, gray tar 

to yellowish and reddish brown; thir 

to medium bedded; pitted weathered 

surfaces; cherty limestone containsdense sandstone partings in the middle 

part of the unit _____________ 212

13. Dolomitic sandstone, light-gray; weathers tan to buff; medium bedded ____ 3

12. Dolomitic limestone, light-tan; weathersbuff; thin bedded; medium grained; 

minor chert lenses. Unit contains medial dark-tan arenaceous dolomite 

marker bed __ _ - 21

11. Calcareous quartzite and ferruginous 

sandstone, interbedded; gray brown; 

weather tan brown and reddish brown; 

banded; medium bedded; quartzite ir 

well jointed and contains sandstone 

partings ___ __ 33

10. Fossiliferous limestone, light-browngray; weathers tan to buff; thin to 

medium bedded; local bioclastic limestone layers; sparse black chert nodules; abundant gastropod, brachiopod, 

bryozoan, and crinoid stem assemblage 

(USGS colln. 18486-PC and 18893- 

PC) ____ ____-________- 34

9. Cherty limestone, medium-gray; weathers medium light gray; thin bedded, 

locally laminar; small black chertnodules and lenses ____ _ 92

8. Ferruginous sandstone and calcareour 

quartzite, interbedded; orange tan an<? 

light gray; weather dark brown and 

tan to light gray; medium bedded; 

crossbedded; worm trails in upper 

sandstone beds __ 41

7. Cherty limestone, medium-dark-gray; 

weathers light gray; thin to medium 

bedded; interbedded arenaceous and 

cherty limestones. Black chert nodulef 

weather brownish with rought sanded 

surfaces in the upper part, are black 

and smooth in the lower part. Arenaceous and cherty limestones are sparsely fossiliferous ____ _ 125
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A21

Thickness

(ft)

6. Calcareous quartzite, tan; weathers dark 

brown; medium bedded; contorted 

warped "ropy" layers with tan- and 

brown-banded layers and pitted weathered surface _________________ 75

5. Calcareous quartzite, quartose sandstone, 

and orthoquartzite, interbedded; tan; 

weather tan to dark brown and yellowish brown; medium to thick bedded; 

well jointed; form cliffs and blocky 

talus slopes; shale partings within 

the quartzite ________________ 97

4. Cherty limestone, medium-dark-gray; 

weathers medium gray; thin bedded; 

black chert nodules. Unit is mostly 

covered slope _______________ 28

3. Calcareous quartzite, tan; weathers tan 

to reddish brown; thin to medium bedded; crossbedded, well jointed; interbedded thin calcareous sandstone __ 151

2. Ferruginous sandstone, orange-graybrown; weathers brown; medium bedded; argillaceous limestone partings; 

carinoid corals, brachiopod fragments^ 8

1. Orthoquartzite, light-gray-brown; weathers tan to light brown; medium bedded; well jointed; locally crossbedded; 

black chert layer at base in thin calcareous quartzite layer ________ 58

Total measured thickness of lower 

part __________________ 1,033

Conformable contact.

Oquirrh Group, Erda Formation.

Fossils are sparse and generally poorly preserved 

in the Kessler Canyon Formation; only one collection (USGS colln. 18486-PC) represents the formation. A 35-foot-thick bed, unit 10, in the lower 

part (section 9a) contains an unusually fine assemblage of abundant, large, well-preserved specimens of gastropods, brachiopods, bryozoans and 

long, nearly intact sections of crinoid stems. Most 

of the upper two-thirds of the section, however, 

contains only sparse, poorly preserved, silicified 

fusulinids and occasional crinoid fragments in thin 

beds of dolomitic limestone and bedded chert.

The lower part of the formation has not provided 

identifiable fossils, but J. E. Welsh (oral commun., 

1961) reported fusulinids of Missouri (Late Pennsylvanian) age from the lower Kessler Canyon Formation in the Coon Canyon syncline south of Coon 

Peak. Fossils in the middle part are of probable 

Virgil age according to Gordon and Duncan. The 

poorly preserved chertified fusulinids found in the

upper parts also are of probable Virgil (Late Pennsylvanian) age (section on biostratigraphy and correlation, p. A49). Missouri age strata, so abundant 

in the Bingham sequence, were not found by us, and, 

if present, are extraordinarily thinned or were 

eroded prior to deposition of Virgil strata. Gordon 

and Duncan suggest that the lack of Missouri age 

rocks has regional significance and compare it to 

Steele's (1961) "Regional Middle Pennsylvanian 

unconformity." This suggests that sediments of the 

Rogers Canyon sequence have a closer affinity with 

those in the Confusion Range and eastern Nevada 

than those of the Timpanogos and Bingham 

sequences.

Wolfcamp sediments are also missing in this 

sequence, and the Early Permian Park City strata 

rest without angular unconformity on Virgil (?) 

beds of the Kessler Canyon Formation. Similarly 

these rocks are absent in the Wasatch Mountains in 

the Mount Raymond sequence (Baker and others, 

1949).

Gordon and Duncan suggest that this absence 

may indicate a period of nondeposition and erosion, 

a factor that gains some credence in our observation 

locally of highly altered iron-stained zones in upper 

Kessler Canyon sediments as at the mouth of Coon 

Canyon perhaps evidence of weathering surfr°.es. 

The apparently conformable relation between the 

Kessler Canyon Formation and Grandeur Member 

of the Park City Formation strata suggests that the 

area was not undergoing uplift and erosion. It may 

have been awash, parts of the area emergent at 

times to permit weathering action.

PARK CITY FORMATION

Rocks equivalent in lithology and age to thos^ in 

the basal part of the Park City Formation in the 

Wasatch Mountains, named originally by Boutwell 

(1907), were recognized in the Oquirrh Mountains 

by Tooker and Roberts (1961, p. 32) and by Welsh 

and James (1961, p. 4). These rocks, origirally 

assigned to an informally named unit by Tooker and 

Roberts (fig. 6), correspond to the Grandeur Member as it was defined in the Wasatch Mountains by 

Cheney, Swanson, Sheldon, and McKelvey (1959, 

P. 12).

GRANDEUR MEMBER

The Grandeur Member is exposed in Little Valley 

syncline in Little Valley at the northeast end of the 

Oquirrh Mountains and also in the Coon Canyon 

area (fig. 2). The unit is exposed discontinueusly 

southward along the eastern range front and is cut
A22 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

off by the North Oquirrh thrust fault (Tooker and 

Roberts, 1961, pi. 6). No outcrops are found west of 

the Garfield fault. The Grandeur Member appears 

to lie conformably on the Kessler Canyon Formation of the Oquirrh Group; overlying strata have 

been eroded. The member is locally unconformably 

overlain by Tertiary conglomerate and volcanic 

rocks (for descriptions see Tooker and Roberts, 

1961, p. 32-34) .

The Grandeur consists of thin- to medium-bedded 

fine- to coarse-grained arenaceous limestone, dolomite, and dolomitic limestone interspersed with thin 

shale and argillaceous limestone, phosphorite, chert, 

orthoquartzite, and calcareous sandstone partings, 

lenses, and layers. The exposed thickness of the 

member in section 10 (fig. 4) is about 760 feet. The 

member can be divided into three parts : a lower 

limestone 215 feet thick ; medial quartzite, dolomite, 

sandstone, shale, chert, and phosphorite 284 feet 

thick; and an upper dolomite and quartzite 261 feet 

thick. These are lithologically comparable to the 

three parts in the type locality of the Grandeur 

Member in the Wasatch Range.

REFERENCE SECTION OF GRANDEUR MEMBER OF PARK CITY

FORMATION (see fig. 4, section 10)

East of fork in Coon Canyon, north side in

sec. 14, T. 2 S., R. 3 W., Garfield quadrangle, Utah

[Measured by E. W. Tooker]

Thickness

(ft) 

Unnamed conglomerate.

Unconformable contact, erosion interval. 

Park City Formation: 

Grandeur Member:

25. Dolomitic limestone, light-grayish-tan; 

weathers light tan to buff; medium bedded; tan chert nodules near base __ . _ 41

24. Calcareous and ferruginous sandstone, interbedded; reddish gray; weather brown 

to reddish brown; medium bedded; locally, chert nodules. Unit is mostly covered- 55

23. Dolomitic limestone, light-grayish tan; 

weathers light gray; medium bedded. 

Unit is mostly covered _ ________ __ 7

22. Orthoquartzite and limestone, interbedded; 

tan to light brown and light gray ; weather tan; medium bedded; lacy chert laminae in limestone _____________ _ 73

21. Calcareous quartzite, calcareous sandstone, 

and arenaceous dolomitic limestone, interbedded. Unit is mostly covered __ _ 45

20. Dolomite and dolomitic and ferruginous 

sandstones, interbedded; reddish brown; 

weather tan; thin to medium bedded; 

sanded weathered surfaces ________ 24

Thickness

(ft)

19. Dolomitic limestone, mottled gray; weathers light grayish-tan; thin to medium 

bedded; brachiopods abundant _____ 10

18. Dolomite, tannish-gray; weathers light buF 

gray; thin to medium bedded; banded 

chert layers and lenses ___________ 6

17. Orthoquartzite and bedded chert, interbedded; reddish brown; weather hematite red and mottled reddish gray; thin 

bedded; irregular layers; conspicuous 

shale partings ______________ 59

16. Shale and calcareous quartzite, interbedded. Unit is mostly covered. Dark-gray 

phosporite nodules in light-brown thin 

sandstone layers throughout unit ___ 81

15. Phosphatic chert and shale, interbedded; 

black and dark gray; weather bluish 

white to gray as surface coating on chert 1

14. Dolomite and shale, interbedded; medium 

gray; weather light gray tan; medium 

and thin bedded; brachiopods abundant 8

13. Shale, calcareous quartzite, and calcareous 

sandstone, interbedded; light grayish 

brown and dark gray; weather tan to 

light brown and medium gray; thin bedded, ribbon banded appearance _____ 14

12. Calcareous quartzite and sandstone, interbedded; medium brownish gray; weather 

tan to brown; thin to medium bedded; 

local phosphorite nodule zones; lacy tan 

chert; Orbiculoidea brachiopods. Unit i« 

mostly covered _________________ 66

11. Orthoquartzite, medium-dark-gray; weathers tan; medium bedded; brownish-blac1*" 

chert nodules common ___________ 7

10. Quartzose siltstone, reddish-gray; weathers tan; thin to medium bedded. Unit is 

mostly covered _______________ 30

9. Dolomite medium-light-gray; weathers 

light tan; medium bedded. Unit is mostly 

covered slope _________________ 18

8. Limestone and arenaceous limestone, irterbedded; light tan to brown; weather 

tan; thin bedded; productid brachiopods. 

Unit is mostly covered __________ 13

7. Cherty limestone, reddish-gray to brown; 

weathers light grayish brown; medium 

bedded; dark reddish-gray chert nodules 

and lenses; brachiopods abundant. Unit 

poorly exposed; mostly covered ____._ 24

6. Limestone and arenaceous limestone, interbedded; brownish gray; weather tan; locally black chert nodules and lenses; bioclastic limestone lenses common ____ 39

5. Limestone and arenaceous (bioclastic) 

limestone; light brown gray; weather
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A23

Thickness

(ft)

tan gray; medium bedded; gastropods, 

brachiopods, and crinoids abundant __ 8

4. Limestone and cherty limestone, interbedded; gray; weather medium light gray; 

thin to medium bedded; abundant chert 

nodules and lenses up to 4 inches thick_ 11

3. Fossiliferous limestone, medium-darkgray; weathers light gray; thin to medium bedded; local lacy tan chert beds; 

brachiopods, gastropods, and crinoid 

stems abundant _______________ 12

2. Argillaceous limestone and silty limestone, 

interbedded; dark gray; weather medium 

dark gray; thin to medium bedded; 

brachiopods locally abundant ______ 78

1. Limestone, light-gray; weathers light 

gray; medium bedded; tan lacy chert 

bands; bioclastic in part; brachiopods, 

bryozoans, and gastropods very abundant (USGS colln. 20240-PC, 20241-PC 

and 20242-PC in reference area and 

19949-PC, 19948-PC, 22848-PC, 20238- 

PC, from unit in Little Valley) _____ 30

Total thickness measured _. 

Conformable contact. 

Oquirrh Group, Kessler Canyon Formation.

760

Fossils are abundant and well preserved in the 

lower limestone unit. The fauna in table 4 includes 

bryozoans, crinoids, brachiopods, and gastropods of 

probable late Leonard (Early Permian) age; Gordon and Duncan in the section on biostratigraphy 

and correlation describe the several collections, their 

biostratigraphic relation, and correlation. They conclude that an unconformity occurs at the base of the 

Grandeur Member that accounts for the absence of 

Wolfcamp and part of the Leonard rocks in the 

Rogers Canyon sequence.

BINGHAM SEQUENCE

The Bingham sequence, named for the Bingham 

mining district in the central part of the Oquirrh 

Mountains where the most complete upper part of 

the Paleozoic stratigraphic section occurs, is the 

folded upper plate of the Midas thrust fault. The 

lower part of the sequence is exposed only in a 

small area in the Ophir mining district in the southern part of the range. The rocks consist of lower 

Paleozoic formations ranging from Cambrian 

through Mississippian in age; they were described 

by Gilluly (1932) and will not be discussed further 

here. The upper thick series of sediments, the 

Oquirrh Formation, which Gilluly did not subdivide, 

was raised to group status and subdivided by Welsh 

and James (1961). Their formational assignments 

are here modified and revised (fig. 5).

OQUIRRH GROUP

The Oquirrh Group rests conformably on the 

Manning Canyon Shale of Mississippian and Pennsylvanian age and is divided into the West Canyon 

Limestone, the Butterfield Peaks Formation, and 

the Bingham Mine Formation (fig. 3). The Bingham 

Mine Formation is divided into the Clipper Ridge 

Member and the overlying Markham Peak Member. 

These rocks are of Pennsylvanian age.

WEST CANYON LIMESTONE

Nygreen (1958, p. 13-14) originally applied the 

name West Canyon Limestone Member to the basal 

clastic cyclic limestone unit of the Oquirrh Formation in the Fourmile Canyon tributary of West Canyon on the east side of the Oquirrh Mountains in 

the Fairfield quadrangle. We have raised this unit to 

formational status as the West Canyon Limestone. 

James Gilluly (oral commun., 1967) agrees that 

these strata constitute a valid recognizable formational unit in the Stockton and Fairfield quadrangles. 

The formation is exposed on the east limb of the 

Ophir anticline in Manning, Ophir, and Soldier Canyons on the west side of the Oquirrh Mountains as 

well as on the flanks of Long Ridge anticline in 

West Canyon (Gilluly, 1932, pi. 12). In addition to 

the type section shown by Nygreen (1958, p. 13) in 

the El/2 sec. 23 and Wy2 sec. 24, T. 5 S., R. 3 W., 

Fairfield quadrangle (fig. 4, section 4) and by Welsh 

and James (1961, pi. 5), three nearly comparable 

reference sections by Roberts and Tooker in the 

southern Oquirrh Mountains, in West Canyon, Soldier Canyon, and at Lewiston Peak (fig. 4, section 

5; ridge west of Lewiston Peak, sec. 29, 30, T. 5 S., 

R. 3 W., Fairfield 15-minute quadrangle) indicate a 

wide areal extent for the West Canyon Limestone 

of the Bingham sequence. The West Canyon and 

Soldier Canyon reference sections are included to 

afford a direct comparison of lithologies; the fauna 

in Soldier Canyon are more abundant and better 

exposed (fig. 10) and preserved than those in West 

Canyon.

Contacts of the West Canyon Limestone with the 

underlying Manning Canyon Shale and the overlying Butterfield Peaks Formation are poorly exposed. Gilluly (1932, p. 32) stated that the Soldier 

Creek section of the Manning Canyon Shale, which 

he believed probably was most representative 

because it was least deformed by folding, apparently was conformable with, and transitional lithologically into, limestones of the Oquirrh Formation. 

In each of the areas where the section was measured, the base of the West Canyon Limestone is at
A24 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Butterfield Peaks Formation 

._«£ ' x/ ^r banning Canyon Shale

: * fi.";i. '^ , m*.

FIGURE 10.' Typical exposures of reference section of the West Canyon Limestone and the basal portion 

of the Butterfield Peaks Formation in Soldier Canyon. View is westward toward spur on north side of 

the canyon along the east boundary of sec. 34, T. 4 S., R. 4 W., Stockton 15-minute quadrangle.

the base of the continuous predominantly limestone 

section that overlies a generally concealed shale 

unit. The formation is also conformable with and 

transitional into the cyclic shale, limestone, and calcareous quartzite of the Butterfield Peaks Formation. In each section, the upper contact is mapped 

at the base of a continuous, though variable in 

thickness, crossbedded, silica- and carbonatecemented orthoquartzite and calcareous sandstone 

separating two less resistant limestone and argillaceous limestone units.

The West Canyon Limestone is 1,450 feet thick in 

the type section (Nygreen, 1958, p. 14, 39) and is 

1,436 feet thick in the reference locality in West 

Canyon (section 6a). Comparable rocks are 1,180 

feet thick at Lewiston Peak, and 1,060 feet thick in 

the Soldier Canyon reference sections.

The West Canyon rocks are principally cyclical 

clastic arenaceous limestone composed of quartz 

and calcite grains and fossil fragments and interbedded thin cherty argillaceous dense crystalline 

limestone beds as much as 1 or 2 feet thick. Thin 

calcareous quartzite beds or partially silica-cemented 

calcareous sandstone, generally banded or crossbedded, separate much thicker limestone strata. The 

limestone generally is medium dark gray; it weathers light and medium gray if pure or brownish gray 

if arenaceous and contains tan and black chert nodules and lenses. The rocks are medium grained, containing coarse angular to subrounded sands, and are 

thin to medium bedded, ranging from less than 1 

foot to 3 feet in thickness. The calcareous quartzite 

is medium gray to tan; the sandy-weathered surface 

rind is of variable thickness and is tan to light gray 

brown. The quartzite is composed of detrital quartz 

and calcareous sand grains cemented by silica and 

calcite. Evidence of small-scale rhythmic sedimentation may be seen in these rocks, although the environment favored the formation of limestone. 

Toward the upper contact of the formation, the cal-
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A25

careous quartzite beds become thicker and more 

abundant.

FIRST REFERENCE SECTION OF WEST CANYON LIMESTONE

(see fig. 4, section 6a)

Ridge on north side of West Canyon, opposite Maple Canyon, 

sec. 27, T. 4 S., R. 3 W., Fairfield 

quadrangle, Utah

[Measured by E. W. Tooker and R. J. Roberts]

Thickness 

(ft)

Oquirrh Group:

Butterfield Peaks Formation.

Conformable contact.

West Canyon Limestone:

14. Limestone, cherty limestone, and arenaceous limestone, interbedded; medium to 

gray; weather medium to light gray; 

thin to medium bedded; black chert nodules ; shale partings ; local bioclastic limestone; sparse brachiopods ________ 201

13. Calcareous quartzite and limestone, interbedded; brownish gray; weather tan to 

rusty brown; quartzite is medium bedded and crossbedded; limestone is thin 

bedded, fine grained, and locally bioclastic _____________________ 15

12. Arenaceous limestone, cherty limestone, argillaceous limestone, and limestone, inbedded; medium gray; weather light 

gray; thin to medium bedded; local crossbedding; black cherty lenses and nodules; local shale partings and bioclastic 

limestone beds; abundant brachiopods 

(USGS colln. 20331-PC) _________ 87

11. Calcareous quartzite, tan; weathers rusty 

brown; medium bedded; crossbedded and 

thinly laminated; well jointed ______ 11

10. Cherty limestone, arenaceous limestone, argillaceous limestone, and limestone, interbedded; medium gray; weather medium light gray; thin to medium bedded; 

fine-grained dense silty limestone and 

platy shale partings ; black chert nodules 

and thin irregularly layered brownweathering white chert; local bioclastic 

limestone layers; brachiopods abundant 347

9. Calcareous quartzite and calcareous sandstone, interbedded; medium grayish tan; 

weather medium light gray; medium bedded; crossbedded and laminar bands; inlayered limestone and shale partings __ 29

8. Arenaceous limestone and argillaceous 

limestone, interbedded; medium gray; 

weather medium light gray; thin bedded; irregular thin bioclastic limestone 

layers ______________________________

7. Calcareous sandstone, medium-gray; 

weathers brown; fluted weathered surface; medium bedded; crossbedded __

32

13

Thickness 

(ft)

6. Arenaceous limestone, cherty limestone, 

and argillaceous limestone, interbedded; 

medium gray; weather light gray; thin 

to medium bedded; black chert layers 

and lenses; shale partings; local bioclastic limestone layers 43

5. Argillaceous limestone, arenaceous limestone, and dense limestone, interlayered; 

medium gray; weather light gray with 

brown streaks in coarser sand layers; thin 

to medium bedded; local cherty limestone 

and carbonaceous shale partings; crossbedded bioclastic limestone layers; 

abundant brachiopods (USGS colln. 

20330-PC and 21157-PC) ________ 231

4. Limestone, medium-gray; weathers light 

gray; thin to medium bedded; coarse 

sandstone laminae irregularly distributed 

through the limestone; fossiliferous 

(USGS colln. 21156-PC) _________ 80

3. Calcareous sandstone, brown-gray; weathers light brown; medium bedded _ 3

2. Limestone, arenaceous limestone, and argillaceous limestone, interbedded; medium gray to brownish gray; weather light 

to medium gray and tan; thin to medium 

bedded; crossbedded sandstone and carbonaceous shale lenses and partings; 

abundant bioclastic limestone; abundant 

brachiopods, bryozoan, crinoid, and Antiquatonia coloradoensis assemblage 

(USGS colln. 20329-PC, 21154-PC, 

21155-PC) __________________ 262

1. Limestone and argillaceous limestone, interbedded; medium dark gray; weather 

brownish gray and medium gray; thin 

to medium bedded; interlayered arenaceous and bioclastic limestone, cherty limestone, and carbonaceous shale; abundant 

fossils in cherty limestone. Unit is poorly 

exposed, mostly covered __________ 82

Total thickness measured ________ 1,436 

Conformable contact. 

Manning Canyon Shale.

SECOND REFERENCE SECTION OF WEST CANYON LIMESTONE

(see fig. 4, section 11)

Begin at base of ridge on north side Soldier Creek lat 40° 25' 

45", long 112° 16' 30", traverse N. 6° E. to ridgetop, then 

N. 40° E. to ridgetop west of peak 9075, sees. 26, 27, and 

34, T. 4 S., R. 4 W., Stockton quadrangle, Utah

[Measured by E. W. Tooker, Mackenzie Gordon, Jr., and R. J. Roberts]

Thickness 

(ft)

Oquirrh Group:

Butterfield Peaks Formation. 

Conformable contact.
A26 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

West Canyon Limestone:

Thickness

. _ (ft) 

14. Limestone, arenaceous limestone, argillaceous limestone, interbedded; light gray 

to dark gray and brownish gray; weather light gray to tan; thin to medium bedded; locally interbedded black chert nodule layers, thin calcareous sandstone 

beds, and shale partings; locally platy; 

locally fossiliferous (USGS colln. 17170- 

PC) _______________________ 121

13. Calcareous sandstone, dark-brownish-gray; 

weathers grayish brown; medium bedded; black chert nodules in the upper 

1.6 ft ______________________ 4

12. Limestone, dark-brownish-gray and medium-gray ; weathers medium gray to medium light gray; thin to medium bedded; 

nodular chert layers and dark-brown bioclastic sandy streaks in upper 4 ft; lower part contains interbedded bioclastic 

limestone and argillaceous limestone layers and shale partings; lower 81 ft along 

line of section concealed due to faulting; 

Tertiary monzonite porphyry sill 28 ft 

thick underlies top 4 ft of unit _____ 153

11. Calcareous quartzite, light-brownish-gray;

weathers tan; thick bedded; well jointed 12

10. Limestone, medium-dark-gray; weathers 

medium gray; medium to thin bedded; 

lenticular nodules of black chert 2 in. 

thick and 6 in long; locally grades into 

thin bioclastic and shaley interlayers in 

the upper part ________________ 98

9. Limestone, argillaceous limestone, and 

shale, interbedded; medium dark gray 

to brownish gray and dark gray; weather light gray to grayish tan; thin to 

medium bedded; well jointed; calcareous sandstone in lower 3 ft; 1-2-ft 

shale layers near the top are mostly covered _______________________ 48

8. Limestone, dark-gray; weathers light gray; 

medium bedded; in part, silty; in part, 

arenaceous and bioclastic; locally sparse 

black chert nodules; locally, thin finegrained dolomite lenses; abundantly fossiliferous locally; silicified bryozoans and 

brachiopods __________________ 86

7. Arenaceous limestone, gray to brownishgray; weathers light gray with brownish sandy streaks; medium bedded; locally poorly sorted sand particles; chert 

nodules in middle part; fossiliferous, 

derbyid and spiriferid brachiopods 

(USGS colln. 17169-PC) _________ 33

6. Limestone, medium-dark-gray; weathers 

light olive gray; thin bedded; argillaceous limestone interlayers; sparse black 

chert nodules in upper part _______ 59

Thickness

(ft)

5. Limestone, argillaceous limestone, and 

shale, interbedded; light olive gray and 

dark gray; weather light gray; medium 

to thin bedded; shale partings and interbedded argillaceous limestone; sparse 

black chert nodular limestone; locally, 

thin bioclastic limestone layers. Upper 

30 ft is predominantly shale and mostly 

covered __________-__ _ 80

4. Argillaceous limestone, medium to darkgray; weathers dark brownish gray; 

thin bedded and platy; interbedded black 

nodular chert and calcareous sandstone 

layers at base; fossiliferous, brachiopods 

and bryozoans (USGS colln. 17168-PC)_ 5

3. Limestone, medium-olive-gray; weathers 

light olive gray; medium bedded; in part, 

platy and well-join ted blocky float; forms 

cliffs along section line ___ 25

2. Limestone, arenaceous limestone, argillaceous limestone, carbonaceous shale, cherty 

limestone, and calcareous quartzite interbedded with cyclic repetition; light 

olive gray, light gray to dark gray; 

weather medium gray to brownish gray 

and buff; thin to medium bedded; locally 

crossbedded; bioclastic limestone and 

calcareous quartzite; thin shale layers 

and partings; locally at base of unit interbedded argillaceous limestone and 

shale are fossiliferous; brachiopods 

(USGS colln. 17167-PC). The unit is 

mostly covered in lower 100 ft _____ 288

1. Argillaceous limestone, arenaceous limestone, and calcareous quartzite, interbedded ; olive gray to light tan; thin bedded; irregularly interbedded ferruginous 

shale and arenaceous limestone; locally 

crossbedded and banded. The unit is 

mostly covered _______ _ 41

Total thickness measured ________ 1,053 

Conformable contact. 

Manning Canyon Shale.

Fossils are locally abundant and similar to those 

found in the upper part of the Lake Point Limestone of the Rogers Canyon sequence, but are often 

fragmented in the argillaceous and flaggy limestone. 

The collections are located in the reference sections 

and in table 5; a detailed description of the fauna 

and its correlation is given by Gordon and Duncan 

in the section on biostratigraphy and correlation. 

Brachiopods typical of the Rugoclostus zone are 

most abundant, bryozoans are fairly common, corals 

are very rare, mollusks are limited to a few scattered pelecypods, and trilobites are present as rare 

fragments. Nygreen (1958) reported finding the
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A27

fusulinid Millerella in the upper part. A Morrow 

age is suggested for the West Canyon Limestone. 

The Mississippian-Pennsylvanian boundary lies in 

the upper part of the underlying Manning Canyon 

Shale.

BUTTERFIELD PEAKS FORMATION

The Butterfield Peaks Formation is here named 

for Butterfield Peaks, 3 miles south of Bingham in 

the Fairfield quadrangle. The formation, which 

rests conformably on the West Canyon Limestone, 

includes the medial cyclic series of rocks of the 

Oquirrh Group in the Bingham sequence. These 

rocks formerly were believed to represent the upper 

part of the Maple Formation and all of the "White 

Pine" and Butterfield Formations of Welsh and 

James (1961) (fig. 5). The rocks crop out along the 

Long Ridge anticline northwest of West Canyon and 

along the Pole Canyon syncline (fig. 2). The type 

section of the Butterfield Peaks Formation, however, was measured up the ridge at the head of West 

Canyon, westward along the ridge separating the 

Middle and Settlement Canyons (fig. 11), and then 

northward across Middle Canyon west of the mouth 

of Left Hand Fork (fig. 4, section 7a). Here the 

formation is 9,072 feet thick. The upper contact is 

at the base of a banded quartzite layer underlying 

the Jordan marker unit (fig. 12). A reference section of the lower part of the formation, which continues the West Canyon Limestone reference section 

and which also was the type section of the Butterfield and White Pine Formations of Welsh and 

James (1961, pi. 5), is on the north side of West 

Canyon, opposite Maple Canyon, in the north center 

part of sec. 27 and the south center part of sec. 22, 

T. 4 S., R. 3 W., Fairfield quadrangle. A second reference section of the lower part (3,900 feet) of the 

Butterfield Peaks Formation measured in Soldier 

Canyon, a continuation of the West Canyon LimeFIGURE 11. Typical exposures of the middle part of the Butterfield Peaks Formation as exposed in part of its 

type section along the skyline at the head of White Pine Canyon tributary of Middle Canyon. Cyclically 

repeated beds measured along the skyline ridge appear as prominent bands; light-colored beds are mostly 

calcareous sandstone and arenaceous and cherty limestone, darker beds are covered argillaceous limestone zones.
A28 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

FIGURE 12. Typical exposures of the Jordan (limestone) 

marker bed (a thick cherty limestone) within the base of 

the Clipper Ridge Member of the Bingham Mine Formation 

at the type locality of the member in Middle Canyon. View 

looking west toward W% cor. NE 1^ sec. C, T. 4 S., R. 3 W. 

Bingham Canyon 7%-min. quadrangle. Light-colored rocks 

at the base and top are calcareous quartzite.

stone reference section, contains several important 

fossil collections.

The rocks are predominantly calcareous quartzite 

and silica-cemented orthoquartzite, calcareous sandstone, and arenaceous, cherty, argillaceous, and finegrained dense limestones. The calcareous quartzite is 

brown gray, fine to medium grained, medium to massive bedded, and locally may contain argillaceous 

limestone laminations. In places the quartzite is 

crossbedded and ripplemarked on bedding surfaces. 

It weathers tan to light brown to red brown. The 

silica-cemented orthoquartzite beds stand in prominent relief and have a hard vitreous weathered surface; the carbonate-cemented calcareous quartzite 

beds weather, forming a soft outer surface rind of 

variable thickness up to one-third inch thick. These

units grade into one another and locally weather in 

the form of ribs outlining crossbeds in the orthoquartzite or parallel bands in the calcareous quartzite. Limestones typically are medium dark gray, 

fine crystalline to medium sandy, and thin to medium 

bedded; they weather light gray. Thin black chert 

nodules and lenses locally band the rocks; thin 

coarse arenaceous layers, some of which are bioclastic and many of which are crossbedded, and interlaminated shale and argillaceous limestone beds 

occur in the strata. Limestones in the lower part 

of the formation are very fossiliferous.

TYPE SECTION OP BUTTERPIELD PEAKS FORMATION

(see fig. 4, section 7a)

Ridge along the divide beginning at the head of West Canyon 

and between Settlement and Middle Canyons to point 8944 

thence northeast to base of Middle Canyon, sees. 6, 7, 18, 

19, 20, and 21, T. 4 S., R. 3 W., and sec. 12, T. 4 S., R. 4 W., 

Fairfield, Stockton, and Bingham Canyon quadrangles, Utah

[Measured by E. W. looker and R. J. Roberts]

Thickness

(ft) 

Oquirrh Group:

Bingham Mine Formation: 

Clipper Ridge Member. 

Conformable contact. 

Butterfield Peaks Formation:

50. Calcareous quartzite, orthoquartzite, and 

calcareous sandstone, interbedded; tan 

to light orange gray; weather light 

brown; medium bedded to massive; interlayered thin- to medium-bedded arenaceous limestone and silty limestone; 

fossil fragments in limestone. Unit is 

poorly exposed ________________ 215

49. Arenaceous limestone, olive-gray; weathers 

light gray; thin to medium bedded; interlayered argillaceous and silty limestone; fossil fragments __________ 11

48. Calcareous quartzite and arenaceous limestone, interbedded; pale grayish orange; 

weather light brown and olive gray; 

interstratified with banded medium-bedded orthoquartzite and thin-bedded argillaceous limestone. Unit is partly covered _______________________ 473

47. Orthoquartzite and calcareous quartzite, 

interbedded; pale grayish orange; medium bedded to massive; crossbedded and 

banded _____________________ 9

46. Calcareous quartzite and calcareous sandstone, interbedded; medium grayish tan; 

weather tan; medium bedded; banded; 

locally crossbedded; interlayered thin 

fossiliferous and bioclastic limestones. 

Unit is partly covered __________ 196
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A29

Thickness

(ft)

45. Arenaceous limestone, olive-gray; weathers pale yellowish brown; thin bedded; 

poorly preserved fusulinids __________ 1

44. Calcareous quartzite, calcareous sandstone, 

arenaceous limestone, and argillaceous 

limestone, interbedded; quartzite is banded and crossbedded. Unit is poorly exposed on slope ___________-_-__ 231

43. Cherty limestone, medium-dark-gray; 

weathers medium gray; thin bedded; 

small black chert nodules and layers; 

grades downward into platy silty limestone without chert __________ _ 7

42. Arenaceous limestone, brownish-gray; 

weathers yellowish gray; thin bedded; 

platy float __________________ 51

41. Orthoquartzite and calcareous quartzite, 

interlayered; light grayish orange and 

brownish gray; weather pale yellowish 

brown and yellowish gray; medium bedded to massive; well jointed ______ 222

40. Calcareous quartzite and arenaceous limestone, interbedded; locally crossbedded; 

fossil fragments in sandy layers in limestone ______________________ 182

39. Arenaceous limestone; contains bioclastic 

limestone layers and poorly preserved 

fusulinds; poorly exposed ________ 6

38. Calcareous quartzite and limestone, interbedded. Unit is poorly exposed ______ 232

37. Limestone, silty limestone, and arenaceous 

limestone, interbedded; medium dark 

gray; weather light olive gray; thin to 

medium bedded; banded layers contain 

abundant brachiopods and bryozoans _ 140

36. Cherty limestone, medium-dark-gray; 

weathers dark yellowish brown; thin 

bedded to laminar; interlayered arenaceous and argillaceous limestone; black 

chert layers and nodules up to 6 in. thick. 

Lower 20 ft grades into arenaceous limestone ___________________ 101

35. Orthoquartzite, light-grayish-tan, mediumbedded ______________________ 23

34. Arenaceous limestone, calcareous quartzite, 

calcareous sandstone, Orthoquartzite, and 

platy silty limestone, interbedded with 

cyclic repetition; medium dark gray and 

light grayish tan; weather medium light 

gray and olive gray; thin bedded to 

thick bedded. Unit contains thin bioclastic limestone layers. Unit is poorly exposed ______________________ 213

33. Orthoquartzite and calcareous quartzite, 

interbedded; light grayish tan to light 

olive gray; weather tan to yellowish 

brown; medium bedded to massive; pitted 

and mottled on weathered surfaces; inThickness 

(ft)

terlayered thin-bedded arenaceous and 

cherty limestone, calcareous sandstone, 

and silty and argillaceous limestone; 

USGS colln. f22576 from bioclastic sand. 

Unit is mostly covered __________ 392

32. Argillaceous and cherty limestone, interbedded; medium gray; weather tan and 

light gray; thin bedded; platy. Cherty 

limestone contains both black and tan 

chert nodule layers ____________- 236

31. Arenaceous limestone, medium-gray; 

weathers light grayish brown; thin to 

medium bedded; local bioclastic limestone layers and shale partings; abundant fusulinids found locally in lowe^ 

half (USGS coll. f22583 and f22584) __ 95

30. Calcareovis quartzite and Orthoquartzite, 

interbedded; tan; weather tan to buff; 

medium bedded; banded; locally crossbedded; interlayered thin beds of calcareous sandstone ________________ 222

29. Cherty limestone and calcareous sandstone, interbedded; medium gray and 

light brownish gray; weather brownish 

gray and tan; medium bedded; contain 

black chert nodule layers; interlayered 

thin platy argillaceous limestone in upper part; abundant bryozoans, spiriferid 

brachiopods, and crinoids in upper part _ 79

28. Calcareous quartzite, light-grayish-tan; 

weathers tan; platy to massive bedded; 

interlayered Orthoquartzite and argillaceous limestone ______________ 107

27. Shale and argillaceous limestone, interbedded; dark gray; weather tan; thin bedded; platy; contain sparse chert nodules; 

thin interlayers of arenaceous and silty 

limestone ____________________ 66

26. Cherty limestone, medium-gray; weathers 

light gray; thin to medium bedded; interlayered bioclastic limestone and argillaceous limestone; black chert nodules 

and irregular chert lenses; basal platy 

limestone; abundant shale partings; 

crinoids, bryozoans, corals, and fusulinids (USGS colln. 20308-PC, f22580, 

f22581, and f22582) ____________ 308

25. Arenaceous limestone, calcareous quartzite, 

and Orthoquartzite, interbedded; gray, 

dark gray, and grayish tan; weather tan 

to grayish tan; thin to medium bedded; 

locally laminar ________________ 41

24. Orthoquartzite, light-grayish-tan; weathers white to light gray; medium bedded 

to massive; locally laminated with thin 

calcareous limestone layers _______ 104

23. Argillaceous limestone, shale, and limestone, interbedded; dark gray; weather 

medium gray. Thin-bedded chert band
A30 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Thickness

(ft)

in shale in upper part of unit. Dolomite 

breccia in middle part of unit. Unit is 

poorly exposed __________ 68

22. Orthoquartzite and calcareous sandstone, 

interbedded; grayish brown and medium 

gray; weather grayish tan and brownish 

gray; interlayered argillaceous limestone 

and cherty limestone parting layers __ 149

21. Limestone and shale, interbedded; dark 

gray; weather medium gray; thin bedded; locally contain bioclastic limestone 

lenses _____________________ 85

20. Limestone, dark-gray; weathers light 

gray; thin to medium bedded; locally 

abundant black chert nodules in irregular lenses and layers; thin bioclastic 

limestone layers. Thick-bedded chert zone 

in middle part of unit. Bryozoans locally 

abundant in upper part (USGS colln. 

20307-PC) __________________ 479

19. Calcareous quartzite, argillaceous limestone, calcareous sandstone, and limestone, interbedded with cyclic repetition; 

brownish gray and dark gray; weather 

grayish tan and medium gray; thin 

bedded to massive _____________ 133

18. Arenaceous limestone and limestone, interbedded; dark gray; weather brownish 

gray; medium bedded; interlayered argillaceous limestone. 1-ft fault breccia at 

base of unit. Fault displacement unknown, but it does not appear to be very 

great. Brachiopods and prismoporoid 

bryozoans are present (USGS colln. 

20306-PC) __________________ 73

17. Calcareous quartzite, gray-brown; weathers tan; medium bedded to massive; locally banded and crossbedded; interlayered laminar calcareous sandstone __ 90

16. Cherty limestone and argillaceous limestone, interbedded; medium to dark gray; 

weather brownish gray; thin to medium 

bedded; prismoporoid bryozoans and 

spiriferid brachiopods -_ _ _ __ 60

15. Calcareous quartzite, brownish-gray; 

weathers tan; medium bedded to massive; thin argillaceous limestone and orthoquartzite parting layers _______ 115

14. Cherty limestone, arenaceous limestone, 

and argillaceous limestone, interbedded; 

dark gray; weather brownish gray and 

light gray; thin to medium bedded; black 

chert nodules and layers throughout 

unit; abundant brachiopods (USGS 

colln. 20305-PC) ______________ 364

13. Orthoquartzite and calcareous quartzite, 

interbedded; brownish gray; weather 

tan; medium bedded to massive _ _ _ _ 66

Thickness 

(ft)

12. Limestone, dark-gray; weathers medium 

gray; medium bedded; interlayered argillaceous limestone in middle part; 

spiriferid brachiopods at base ________ 43

11. Orthoquartzite and calcareous quartzite, 

interbedded; brownish gray; weather 

tan; locally laminar; in part medixun 

bedded to massive ______________ 115

10. Limestone, dark-gray; weathers medixtm

light gray; thin bedded to platy _____ 82

9. Orthoquartzite and calcareous quartzite, 

interbedded; brownish gray; weather 

tan; medium bedded ____________ 39

8. Limestone, arenaceous limestone, and 

cherty limestone, interbedded; arenaceous limestone and cherty limestone rre 

brownish gray, limestone is mottled 

medium dark gray and dark gra.y; 

weather medium gray to grayish tan; 

thin to medium bedded; locally platy; 

sparse brachiopods in lower half of unit_ 109

7. Calcareous quartzite, calcareous sandstone, 

silty limestone, arenaceous limestone, 

cherty limestone, and argillaceous limestone, interbedded with cyclic repetition. 

Calcareous quartzite and calcareous 

sandstone are grayish tan to brownish 

gray, weather sandy brown and tan (in 

many places in variegated bands) are 

locally crossbedded, and are thin to 

medium bedded. Silty limestone, arena^eous limestone, cherty limestone, and argillaceous limestone are dark gray and 

medium gray, weather medium gr-T.y, 

and are thin to medium bedded. Brachiopods are locally abundant (USGS colln. 

20303-PC) ______-___________ 612

6. Calcareous quartzite, Orthoquartzite, g-.nd 

calcareous sandstone, interbedded; 

brownish gray; weather sandy brown to 

tan; banded laminae; crossbedded in upper part; locally platy and blocky float. 

Unit is poorly exposed _______ 121

5. Limestone, calcareous quartzite, arenaceous limestone, argillaceous limestone, 

cherty limestone, and calcareous sandstone, interbedded with cyclic repetition. 

Limestone, arenaceous limestone, argillaceous limestone, and cherty limestone 

are dark gray and medium dark gray, 

weather medium gray, and are thin to 

medium bedded; limestone contains shale 

and sand partings. Calcareous quartzite 

and calcareous sandstone are grayish 

brown, weather brownish tan and medium 

grayish tan, and are thin to medium bedded; sandstone is locally crossbedded. 

Bioclastic limestone layers are present 

locally in the unit. Unit is locally fos-
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A31

Thickness

(ft)

siliferous (USGS colln. £22578 and 

20302-PC) ___________________ 780

Porphyry dike 7 ft thick.

4. Limestone, calcareous quartzite, arenaceous limestone, argillaceous limestone, 

and cherty limestone, interbedded with 

cyclic repetition; medium dark gray; 

weather light gray; thin to medium bedded; crossbedded bioclastic limestone 

and shale parting layers locally; horn 

corals and fusulinids present (USGS 

colln. £22577 and 20299-PC) ______ 630

3. Calcareous sandstone, limestone, calcareous quartzite, arenaceous limestone, and 

argillaceous limestone, interbedded. Calcareous sandstone and calcareous quartzite are brownish gray, weather yellowish tan and tan, and are thin to medium 

bedded; sandstone is locally crossbedded. 

Limestone, arenaceous limestone, and 

argillaceous limestone are dark gray, 

weather medium gray, and are thin to 

medium bedded; limestone locally contains black chert nodules. Unit contains 

shale partings and thin interlayers of 

bioclastic limestone. Chaetetes is found 

in limestone at 150 ft in nearby reference section (6a) (USGS colln. 20332- 

PC and 20333-PC) ____________ 610

2. Arenaceous limestone and cherty limestone, 

interbedded; medium gray; weather medium dark gray; thin to medium bedded; 

interlayered argillaceous limestone and 

bioclastic limestone. Lower part of unit 

covered ____________________ 279

1. Calcareous quartzite, brown-gray; weathers tan; locally crossbedded _______ 7

Total thickness measured _______ 9,072 

Conformable contact. 

Oquirrh Group, West Canyon Limestone.

REFERENCE SECTION OF LOWER PART OF BUTTERFIELD PEAKS

FORMATION (see fig. 4, section 11)

Begins approximately 7250 contour on traverse beginning at 

base of ridge on north, side Soldier Creek, opposite unnamed stream heading at the d in Bald Mountain, traverse 

N. 6° E. to ridge top, then N. 40° E. to ridge top west of 

peak 9075, sees. 26, 27, and 34, T. 4 S., R. 4 W., Stockton 

quadrangle, Utah

[Measured by E. W. Tooker, Mackenzie Gordon, Jr., and R. J. Roberts]

Thickness 

(ft)

Fault contact near ridge crest. 

Oquirrh Group:

Butterfield Peaks Formation (upper part). 

Butterfield Peaks Formation (lower part) :

15. Cherty limestone, medium gray; weathers 

medium light gray; thin bedded; black 

chert nodules _________^______ 66

Thickness 

(ft)

14. Orthoquartzite, medium brownish gray; 

weathers grayish tan; medium bedded; 

local thin interbedded bioclastic limestone ______________________ 129

13. Argillaceous limestone, arenaceous limestone, and limestone, interbedded; medium gray; weather medium light gray; 

thin to medium bedded; locally bioclastic 

limestone and cherty limestone in lower 

part of unit; argillaceous limestone and 

carbonaceous shale partings in limestone; argillaceous limestone at top of 

unit abundantly fossiliferous, Prismopora bryozoans, brachiopods, and crinoid 

stem fragments, locally fusulinids 

(USGS colln. 20324-PC and 20325-PC) 445

12. Orthoquartzite, medium brownish gray, 

weathers tan; medium bedded; in part 

crossbedded and banded __________ 59

11. Limestone, cherty limestone, argillaceous 

limestone, and calcareous quartzite and 

Orthoquartzite, interbedded with cyclic 

repetition. Limestone intervals 50-100 ft 

thick are medium dark gray, weather medium gray to medium light gray, are thin 

to medium bedded; locally arenaceous 

limestone is bioclastic; argillaceous limestone and shale form parting layers locally; sparse black chert nodules occur 

locally in the dense limestone layers. 

Unit is fossiliferous; bryozoans, crinoid 

stems and brachiopods (USGS colln. 

20322-PC and 20323-PC). Quartzite intervals 6-50 ft thick are medium brownish gray, weather grayish tan, are medium bedded, are locally crossbedded 

and banded; calcareous quartzite has 

characteristic sanded weathered surface _______________________ 670

10. Calcareous quartzite, medium-brownishgray to light-gray; weathers medium 

gray to brownish tan; medium bedded 

to massive; locally well jointed. Medial 

13-ft limestone is medium dark gray, 

weathers medium gray, is medium bedded, and is in part bioclastic. Unit is 

fossiliferous, spiriferid brachiopods 

(USGS colln. 20321-PC) ________ 1?6

9. Limestone, cherty limestone, arenaceous 

limestone, argillaceous limestone, and 

calcareous quartzite, interbedded with 

cyclic repetition; medium to dark gray 

and grayish tan; weather medium light 

gray, grayish tan to brownish gray; thin 

to medium bedded; locally arenaceous 

beds are crossbedded and banded, occasionally are bioclastic; thin carbonaceous shale partings, bedded chert, and 

quartzite lenses and layers occur 

throughout unit; limestone locally con-
A32 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Thickness

(ft)

tains abundant black chert nodules. 

Quartzite makes up less than one-fifth 

of unit, is crossbedded and banded, and 

locally has a thin-sanded weathered surface. Fossils are locally abundant in the 

limestone mostly productid brachiopods. A 22-ft Tertiary monzonite dike 

crops out at 343 ft _____________ 348

8. Orthoquartzite, calcareous quartzite, and 

limestone, interbedded; medium light 

gray and medium dark gray; weather 

medium light gray; thin to medium bedded. Quartzite intervals 50-150 ft thick 

predominate in the unit; however, quartzite units contain thin interbedded limestone layers and limestones contain thin 

interbedded quartzitic layers. Limestones 

are locally arenaceous, bioclastic, and argillaceous. Argillaceous limestones contain abundant fossils locally, spiriferid 

brachiopods, crinoids, and corals _ -- 358

7. Calcareous quartzite, limestone, arenaceous limestone, and argillaceous limestone, interbedded with cyclic repetition; medium gray to medium light 

grayish tan; weather light gray and tan; 

thin to medium bedded. Quartzite intervals predominate and average 10-30 

ft thick; half as many limestone intervals average about 20 ft thick. Quartzite 

is poorly exposed. Limestone locally contains black chert nodular zones, shale 

parting layers and bioclastic limestone 

beds; locally abundantly fossiliferous 

(USGS colln. 20320-PC) __________ 309

6. Limestone, arenaceous limestone, argillaceous limestone, and calcareous quartzite, 

interbedded with cyclic repetition; medium dark gray to gray; weather medium 

light gray to light gray grayish tan; thin 

to medium bedded; shale partings; locally medium bedded bioclastic limestone 

and cherty limestone interlayers. Quartzite has brownish sand streaks along 

crossbeds and layer bands that weather 

in fluted relief. Unit topped by a 2-ft 

light-tan chert with interstitial limestone; weathers light tan to white; locally fossiliferous (USGS colln. 20319- 

PC). Tertiary monzonite sill 3 ft thick 

30 ft above base of unit __________ 271

5. Limestone, arenaceous limestone, and calcareous quartzite, interbedded; medium 

gray to medium dark gray; weather medium light gray and brownish gray; 

thin to medium bedded; thin fissile shale 

and argillaceous limestone and bioclastic 

limestone interlayers. Quartzite intervals make up a minor part of the unit, 

range from 2 to 15 ft thick, and are 

poorly exposed. Argillaceous limestone is

Thickness 

(ft)

fossiliferous, containing abundant horn 

corals, bryozoans, and spiriferid bra.chiopods (USGS colln. 20318-PC). A Tertiary monzonite sill with characteristic 

greenish weathered surface is 7 ft thick, 

occurs 2 ft above the base of the unit _ 146

4. Calcareous quartzite, orthoquartzite, limestone, arenaceous limestone, and argillaceous limestone, interbedded, Quartzite 

beds are color banded in medium gray and 

brownish medium gray, are weathered 

medium light brownish gray to dark 

brownish gray, are medium bedded to 

massive, occur in intervals ranging from 

10 to 55 ft thick at the base, middle, and 

upper parts of the unit; crossbedd: ng 

prominent locally. Unit characteristically forms cliffs in outcrop. The werthered surface of orthoquartzite is characteristically smooth; a thin sanded rind 

occurs on calcareous quartzite. Limestones are medium gray to medium dark 

gray, weather medium light gray to 

grayish tan with brownish rust streaks 

along coarse sand zones, are fine to medium bedded, are locally crossbedc"ed, 

have occasional bioclastic limestone layers and shale partings, have local black 

chert nodule limestone beds, and are 

fossiliferous, containing productoid 

brachiopods and bryozoans (USGS colln. 

20317-PC) __________________ 141

3. Limestone, arenaceous limestone, argillaceous limestone, and calcareous quartzite, 

interbedded with cyclic repetition. Limestones are medium gray to medium d"rk 

gray, weather medium gray to li<rht 

gray, are thin to medium bedded, have 

interbedded thin bioclastic limestone, 

argillaceous limestone, and shale partings, contain sparse chert nodules locally, contain interlayers of thin quartzite 

locally; locally abundantly fossiliferous 

containing spiriferid and derbyid brachiopods, brachiopods, corals, bryozorns, 

and crinoids (USGS colln. 20316-PC and 

20315-PC). Limestone intervals range 

from 10 to 15 ft thick and make up more 

than three-fourths of the unit. Quartzite 

intervals range from 2 to 10 ft thick, 

are medium brownish gray to grayish 

tan, weather grayish tan and tan, and 

are medium bedded. Quartzite locally 

forms cliffs in outcrop. Locally crossbedded and banded thicker limestone intervals generally contain calcareous 

sandstone and limestone interbeds ____ 441

2. Limestone, argillaceous limestone, arenaceous limestone, cherty limestone, orthoquartzite, and calcareous quartzite, interbedded with cyclic repetition. Li^ne-
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A33

Thickness 

(ft)

stones are medium gray to medium dark 

gray, weather medium to light gray to 

tan, are thin to medium bedded, contain 

thin fissile chert, shale, and bioclastic 

limestone interlayers, and commonly contain crossbedded brown quartz sand partings. Limestones are fossiliferous locally, containing brachiopods, crinoids 

and fusulinids fragments. A white chert 

layer 1 ft thick is a marker unit at 137 

ft. Quartzites are gray to grayish tan 

and medium brownish gray, weather buff 

to tan, are medium bedded to massive, 

are commonly crossbedded, are locally 

banded, locally contain limestone, chert, 

and shale parting layers. Limestones 

make up three-quarters of the unit in 

intervals ranging from 2 to 15 ft thick; 

quartzite intervals range from 2 to 5 ft 

thick. A Tertiary monzonite porphyry 

sill 12 ft thick occurs at 92 ft above base 

of unit _____________________ 279 

1. Calcareous quartzite, light-gray-brown; 

weathers reddish to brownish tan; thick 

bedded; blocky ________________ 5

Total measured thickness _______ 3,863 

Conformable contact. 

Oquirrh Group, West Canyon Limestone.

The limestone beds in the Butterfield Peaks Formation contain an abundant fauna of brachiopods, 

bryozoans, corals, and fusulinids, as noted by Welsh 

and James (1961, p. 8-11). The positions of fossil 

collections are shown in the stratigraphic sections 

and in table 6; a detailed discussion of the faunas 

and their correlation is given by Gordon and Duncan in the section on biostratigraphy and correlation. In general the fauna resemble those of the 

Erda Formation in the Rogers Canyon sequence. 

The age is Des Moines (Middle Pennsylvanian) 

although the lower few hundred feet may be Atoka.

BINGHAM MINE FORMATION

The Bingham Mine Formation was named by 

Welsh and James (1961, p. 8-9) for limestone and 

quartzitic sandstone in the Bingham mining district. It was originally defined as the predominantly 

calcareous quartzite strata of Pennsylvanian age 

above the base of the Jordan marker bed. Their type 

section was specified to be on South Mountain in 

sees. 20, 21, and 22, T. 4 S., R. 5 W., Stockton quadrangle.

The Bingham Mine Formation is 7,311 feet thick 

and is divided into two members. The Clipper Ridge 

Member, 2,985 feet thick, is composed predominantly of cyclically interbedded orthoquartzite and

calcareous quartzite. The overlying Markham Peak 

Member, 4,327 feet thick, is composed predominantly of calcareous quartzite and ferruginous sandstones.

CLIPPER RIDGE MEMBER

The Clipper Ridge Member, here named for the 

area of excellent exposure on the south side of Clipper Ridge in Middle Canyon on the west side of the 

Oquirrh Mountains, is about 3,000 feet thick and is 

the lower member of the Bingham Mine Formation 

(fig. 5). The type section is in Ni/2 sec. 6, T. 4 S., 

R. 3 W., and Si/2 sec. 31, T. 3 S., R. 3 W., Bing'ham 

Canyon quadrangle (fig. 4, section 7a). The lower 

contact of the member is at the base of the 10 -foot 

quartzite that underlies the prominent and distinctive cliff outcrops of the 360-foot thick laminar 

cherty limestone Jordan marker bed (unit 2). The 

Jordan can be traced from the range front south of 

the mouth of Middle Canyon, eastward across the 

Long Ridge anticline to the south edge of the F:ngham porphyry intrusive mass. The upper contact is 

immediately above a fossiliferous sandy limestone 

marker unit, which contains an abundant wellpreserved assemblage of fusulinids, Caninia and 

Syringopora corals, and bryozoans; the contact is 

beneath a quartzite and sandstone unit, which contains the first prominent ferruginous sandstone in a 

predominantly calcareous sandstone and quartzite 

unit.

The Clipper Ridge Member consists mostly of 

orthoquartzite, calcareous quartzite, and calcareous 

and quartzose sandstone, but also contains several 

limestone layers more than 100 feet thick. The 

quartzite commonly is medium to thick bedded and 

is fine to medium grained. Some beds are finely 

banded and locally crossbedded. In the mining district the limestone units include conspicuous mappable beds such as the Parnell, York-Phoenix, Jordan, and Commercial marker beds. Interbedded 

cherty, arenaceous, and argillaceous limestones and 

shale are as much as 270 feet thick in the lower 

part of the member. In the upper part of the member, limestones are thinner, ranging from less than 

10 feet to 70 feet in thickness, and are interbedded 

with quartzite units, ranging from 150 feet to 300 

feet in thickness.

TYPE SECTION OF CLIPPER RIDGE MEMBER (see fig. 4, section 7a)

Ridge southwest from hill 8745, north side of Middle Canyon,

sec. 6, T. 4 S., R. 3 W. and SV2 sec. 31, T. 3 S., 

R. 3 W., Bingham Canyon quadrangle, Utah

[Measured by E. W. Tooker and R. J. Roberts] 

Oquirrh Group:

Bingham Mine Formation:
A34 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Thickness 

(ft)

Markham Peak Member. 

Conformable contact. 

Clipper Ridge Member:

20. Limestone, dark-gray; weathers light 

bluish gray; thin to medium bedded; 

interlayered thin arenaceous limestone; locally black chert nodules; 

abundant well-preserved bryozoans, 

brachiopods, syringoporoid corals, 

and fusulinids (USGS colln. f 22604) 5

19. Calcareous quartzite, light-tan; weathers light brownish tan; medium 

bedded; interlayered thin silty limestone and calcareous sandstone; 

fusulinids abundant _________ 18

18. Arenaceous limestone, medium-gray; 

weathers medium grayish brown; 

banded; abundant fusulinids and 

syringoporoid corals (USGS colln. 

f22603, f22572, and 23890-PC) _ 10

17. Orthoquartzite and calcareous quartzite, interbedded; light grayish tan to 

brown; weather light brownish tan; 

medium bedded to massive; banded_ 160

16. Silty limestone, arenaceous limestone, 

and calcareous quartzite, intarbedded; medium gray and buff tan; 

weather medium light gray and tan; 

thin to medium bedded; brown sandstone partings in limestone; fusulinids (USGS colln. f22601 and 

f22602) _________________ 23

15. Calcareous quartzite and orthoquartzite, interbedded; light grayish tan; 

weather light brown and gray; medium bedded; locally banded; interlayered thin arenaceous limestone; cherty limestone, and silty limestone; 

fusulinids, caninoid corals, and 

productid brachiopods occur in limestone (USGS colln. 20295-PC and 

f22574) _________________ 142

14. Arenaceous limestone and calcareous 

quartzite, interbedded; medium 

gray and grayish tan; weather light 

reddish brown and light gray; medium bedded _______________ 26

13. Calcareous quartzite, arenaceous limestone, and calcareous sandstone, interbedded; grayish tan and medium 

gray; weather reddish brown to 

light brown and light gray; platy 

to medium bedded __________ 65

12. Limestone, medium-gray; weathers 

mottled grayish brown and light 

brown; thin to medium bedded; interlayered thin arenaceous and arT"iickness 

(ft)

gillaceous limestones; worm trails 

shale partings ____________- 10

11. Calcareous quartzite, arenaceous limestone, orthoquartzite, and cherty 

limestone, interbedded; quartzite is 

tan to light gray, limestone is dark 

gray; quartzite weathers to light 

brown and tan, limestone weathers 

mottled gray and light brown; thin 

to medium bedded; locally banded, 

crossbedded, and ripple marked; interlayered bioclastic limestone beds 

and shale partings; some black chert 

nodules and lenses along bedding; 

fusulinids and bryozoans locally 

abundant (USGS colln. f22600) __ 456

10. Limestone, arenaceous limestone, and 

cherty limestone, interbedded; medium light gray; thin to medium 

bedded; locally black chert nodules 

along bedding; abundant fusulinids, 

productid and spiriferid brachiopods, crinoids, bryozoans, and caninoid and syringoporoid corals ___.. 10

9. Calcareous quartzite, tan; weathers 

brownish tan and medium gray; 

medium bedded; locally crossbedded; 

interlayered thin arenaceous limestone and orthoquartzite; fusulinids 

in limestone (USGS colln. f22599) - 95

8. Silty and arenaceous limestone, interbedded; medium gray; weather medium light gray and brownish tan; 

medium bedded; locally crossbedded; 

interlayered thin dark-gray limestone; sparse crinoid and bryozoan 

fossils _____ _____-___ 15

7. Calcareous quartzite, calcareous sandstone, and arenaceous limestone, interbedded; grayish tan; weather 

brownish tan and light gray; medium bedded to massive; banded and 

crossbedded, and locally ripple 

marked; locally interlayered orthoquartzite, which has a hard weathered surface in contrast to the pitted 

thick punky weathered surface on 

calcareous quartzite; worm trails in 

sandstone; brachiopods and bryozoans in limestone __________ 659

6. Limestone, medium-dark-gray; weathers light gray; thin bedded; interlayered thin arenaceous limestone, 

partings; fusulinids (USGS colln. 

f22598) _________________ 14

5. Calcareous quartzite, arenaceous limestone, and orthoquartzite, interbedded; grayish tan; weather
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A35

Thickness

(ft)

brownish tan; medium bedded to 

massive; crossbedding, channel scour 

and fill, and local ripple marks; 

sparse fossils in thin limestone 

layers ___________________ 626

4. Cherty limestone and arenaceous limestone, interbedded; dark gray; 

weather medium dark gray and 

brownish gray; thin laminar to medium bedded; abundant large individual black chert nodules parallel 

to bedding, many of which are zonally altered; abundant brachiopods 

and bryozoans locally. This is the 

Commercial limestone marker bed _ 136

3. Calcareous quartzite, arenaceous limestone, and calcareous sandstone, interbedded; tan; weather brownish 

tan; medium bedded; crossbedded; 

well jointed; punky ferruginous 

weathered rind in sandstone and 

hard weathered surface on quartzite _____________________ 144

2. Arenaceous limestone, cherty limestone, silty limestone, and calcareous 

sandstone, interbedded; dark gray 

to medium gray; weather medium 

gray, and locally near base, mottled 

light gray and tan; thin to medium 

bedded; sandstone locally banded 

and crossbedded. Abundant chert in 

thin nodule layers in the lower part 

unit; nodules along layers in the 

upper part. Sheared altered zone 6 

in. thick at base of unit. Bryozoans, 

abundant spiriferid and productid 

brachiopods, and corals occur 

in the middle part, and fusulinids, brachiopods, and bryozoans 

at the base (USGS colln. f22597 and 

22486-PC). This is the Jordan limestone marker bed ____________ 361

1. Orthoquartzite tan; weathers brownish tan; massive bedded; dense; 

banded __________________ 10

Total thickness measured __ 2,985 

Conformable contact. 

Oquirrh Group, Butterfield Peaks Formation.

Megafossils, mostly corals, are sparse and poorly 

preserved except in arenaceous limestone or calcareous sandstone; fusulinids are the most useful 

for geoehronology. Positions of selected collections 

are shown in the stratigraphic section and are discussed by Gordon and Duncan in the section on biostratigraphy and correlation. Triticites is the most 

common fusulinid, and the forms are believed to be

of probable Missouri age. The megafauna are not 

sufficiently diagnostic to confirm this age designation, but Syringoporoid corals, which are fairly common in the upper part of the member, may represent a Missouri fauna. On the basis of these data 

we consider the Clipper Ridge Member to be of Missouri age.

MARKHAM PEAK MEMBER

The Markham Peak Member of the Bingham Mine 

Formation is here named for the quartzite and sandstone beds of the upper part of the Oquirrh Group; 

these beds are exposed on and near Markham Peak 

in the central part of the Oquirrh Mountains (fig. 

4, section 7b). In addition to rocks of the upper part 

of the Bingham Mine Formation of Welsh and 

James (1961), the Markham Peak Member also includes about 1,200 feet of rocks on Markham Peak 

assigned to the lower portion of the Curry Formation by Welsh and James (1961, p. 6-7).

The lower contact with the Clipper Ridge Member is conformable, the upper part of the member 

has been eroded at Markham Peak, and north of the 

peak the sequence is cut oif by the Midas thr ist 

fault; therefore, the total thickness of the meml^r 

is unknown. However, more than 4,300 feet hr.ve 

been measured in the type section on the ridge between Spring and Dry Canyons west of the Occidental fault (sees. 30 and 31, T. 3 S., R. 3 W., Bingham Canyon quad.), and on Markham Peak east of 

the Occidental fault (sees. 21 and 22, T. 3 S., R. 3 

W., Bingham Canyon quad.) (fig. 4, sections 7a, 

7b).

Orthoquartzite and calcareous quartzite, calcareous sandstone, calcareous silt, and all possible intergradations of these lithologies constitute the Markham Peak Member. A few thin 1-3-foot fusulinidbearing arenaceous limestone beds provide marker 

horizons. Layers and lenses of chert pebble congkmerate occur on Markham Peak in the upper part of the 

section. Welsh and James (1961, p. 12) believed 

that this conglomerate represented an unconformity 

at the Pennsylvanian-Permian boundary. The orthoquartzite is buif to tan, weathers tan to light brovn, 

is medium grained, detrital, silica-cemented, medium 

bedded to massive, locally banded, crossbedded, ripplemarked, and locally shows channel scour and fill. 

Calcareous quartzite is light tan gray, weathers 

yellow gray to yellow orange, is sandy, and is carbonate cemented; locally pitting and a soft sardy 

rind develops on weathered surfaces.

Thin beds of arenaceous medium-dark-gray limestone, which weather olive gray, are common in the
A36 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

lower most part of the member; in many places they 

contain coarse fossil fragments as well as quartz 

grains. Brachiopods, corals, bryozoans, and fusulinids occur at these horizons. Arenaceous limestone 

and calcareous sandstone grade into each other.

TYPE SECTION OP MARKHAM PEAK MEMBER

(see fig. 4, section 7b)

East-trending ridge from Markham Peak through the middle 

of sees. 21 and 22, T. 3 S., R. 3 W., Bingham Canyon 

quadrangle, Utah

[Measured by E. W. Tooker and W. .T. Moore]

Thickness 

(ft)

Erosion unconformity at Markham Peak. 

Oquirrh Group:

Bingham Mine Formation.

Markham Peak Member (upper part) :

26. Calcareous sandstone, medium-darkgray; weathers light reddish brown; 

interlayered ferruginous sandstone; 

thick punky weathered surface rind 192

25. Calcareous quartzite, orthoquartzite, 

and ferruginous sandstone, interbedded; local small breccia zones 

along bedding. Unit is poorly exposed __________________ 148

24. Calcareous sandstone, dark-gray; 

weathers light gray; thin to medium 

bedded; platy; sparse black chert 

nodules irregularly scattered 

throughout unit ___________ 5

23. Ferruginous sandstone and calcareous 

quartzite, interbedded; dark brown 

and grayish tan; thin to medium 

bedded; interlayered thin silty limestone and calcareous sandstones that 

contain chert nodules _________ 189

22. Calcareous quartzite, calcareous sandstone, orthoquartzite, and ferruginous sandstone, interbedded; thin 

bedded to massive; local thin breccia 

zones. Unit is mostly covered ____ 111

21. Orthoquartzite, dark-tan; weathers 

brownish tan; medium, bedded to 

massive; jointed; nonbanded; 1-ft 

breccia at 136 ft ____________ 182

20. Calcareous quartzite and basal 4-ft 

ferruginous sandstone. Unit is mostly covered _____________ 148

19. Calcareous sandstone, olive-gray; 

weathers light grayish orange; medium to thick bedded; thin hard 

weathered surface rind _______ 111

17-18. Orthoquartzite, calcareous quartzite, 

and sandstone, interbedded; light 

grayish tan; weather light reddish 

brown and tan; medium bedded; orThickness

(ft)

thoquartzite banded; interlayered 

thin ferruginous sandstone and thin 

conglomerate lenses. Unit poorly exposed ____________ _- 280

16b. Orthoquartzite and calcareous quartzite, interbedded; light grayish tan; 

medium bedded; thinly banded; well 

jointed; locally crossbedded in uppe^ 

half of unit ______________ - 267

15-16a. Orthoquartzite, tan, medium- to thickbedded; nonbanded; well jointed; 

interlayered 3- to 4-ft ferruginous 

sandstone beds ____ 144 

14d. Calcareous quartzite, ferruginous sandstone, orthoquartzite, arenaceous 

limestone, and silty limestone, interbedded. Dark-yellowish-brown 

medial sandstone; dark-gray upper 

and lower limestones. All are medimr 

bedded. Upper 40 ft of unit is 

mostly covered _____ 198

14c. Orthoquartzite, tan; weathers light 

tan; finely banded; well jointed; 

smooth weathered surface; interlayered calcareous quartzite. Upper 

part of unit is mostly covered _ 534 

14b. Silty limestone, dark-gray; weathers 

medium gray; thin bedded; Lithostrotion colonial coral ____ 37 

14a. Covered zone; brown iron-stained gossan and line of prospect pits; possible concealed fault of unknown displacement ________- 4

13. Calcareous quartzite, light-grayishtan; weathers tan; medium bedded; 

occasional interlayered silty limestone and calcareous sandstone; fusulinid fragments found in sandstone; worm trails present in limestone (USGS colln. f23432 and 

f23433) _________________ 292

12. Calcareous siltstone and sandstone, 

interbedded; light gray; weather tan 

and olive gray; thin bedded; locally 

banded; thin hard rind on weathered 

surface of sandstone; worm trails in 

punky siltstone; fusulinid molds ir 

sandstone _________ _ 323

11. Calcareous sandstone; light tan to 

medium gray; weathers olive gray 

(hard weathered surface) and 

orange brown (soft and punky 

weathered surface); medium bedded; 

locally crossbedded; well jointed; 

interlayered silty and platy limestone; fusulinids found in sandy 

limestone unit 1 mile south alonfr 

ridge (USGS colln. f23431) ; mostly 

covered above 20 ft _________ 202

Total thickness measured ___ 3,367
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A37

Conformable contact.

Oquirrh Group, Bingham Mine Formation, 

Markham Peak Member (lower part).

TYPE SECTION OF MARKHAM PEAK MEMBER (see fig. 4, section 7a)

Ridge between Spring and Dry Canyons, south of Tooele 

Smelter in sees. 30 and 31, T. 3 S., R. 3 W., Bingham 

Canyon quadrangle, Utah

[Measured by E. W. Tookor and R. J. Roberts]

Thickness 

(ft)

Alluvium, covered, faulted, conformable contact 

at offset in section across the Occidental fault. 

Oquirrh Group:

Bingham Mine Formation:

Markham Peak Member (lower part) :

18. Orthoquartzite, medium-bedded, jointed. Unit is covered slope ______- 116 

17. Orthoquartzite, pale-yellowish-brown; 

weathers medium yellowish brown; 

medium bedded to massive; fine 

banding; well jointed; ripple 

mark flutes on weathered bedding 

surfaces; partly covered __ _ 254

16. Orthoquartzite, calcareous quartzite, 

and ferruginous-calcareous sandstone, interbedded; pale yellowish 

brown and brown; weather reddish 

brown; thin to medium bedded; local 

2-in. chert bands; thick weathered 

surface rind on sandstone ____ 315

15. Arenaceous limestone, medium-darkgray; weathers pale yellowish 

brown; medium bedded. Medial 4-ft 

calcareous sandstone. Fusulinids and 

Caninia corals (USGS colln. f23111) 

abundant ____________ 22

14. Orthoquartzite, calcareous quartzite, 

and calcareous and ferruginous 

sandstones, interbedded; pale yellowish brown; weather reddish brown 

to medium yellowish brown; thin to 

medium bedded; banded; interlayered thin fossiliferous limestone, bioclastic limestone, and cherty limestone; fusulinids near middle part 

of unit __________________ 765

13. Calcareous quartzite and ferruginous 

sandstone, interbedded; light grayish tan and pale yellowish brown; 

weather dark yellowish brown and 

brown; medium bedded; interlayered 

thin Orthoquartzite and limestone 

beds; sandstone weathers to thick 

soft punky surface, locally brecciated. Sandstone locally contains 

worm trails; arenaceous limestone 

contains fusulinids (USGS colln. 

f23108 and f23109) _________ 306

Thicknis 

(ft)

12. Calcareous sandstone and calcareous 

quartzite, interbedded; buff to tan; 

weather yellow; interlayered thin 

silty light-gray limestone and bioclastic limestone; sandstone weathers to thick soft (punky) surface. 

Unit is mostly covered slope ___ 12-T

11. Calcareous quartzite and ferruginouscalcareous sandstone, interbedded; 

light olive gray; weather brownish 

yellow to yellowish orange; medium 

bedded; interlayered thin gray arenaceous and silty limestones; fusulinids (USGS colln. f23105, f23106, 

and f23107) ; locally abundant worm 

trails; several 1-ft breccia zones, in 

lower 30 ft of unit. Unit is mostly 

covered _________________ 450

10. Silty limestone, medium-light-gray; 

weathers light olive gray and brownish gray; thin bedded; locally platy; 

fusulinid (USGS colln. f23112) ___ 4

9. Calcareous quartzite and ferruginous 

sandstone, interbedded; interlayered 

arenaceous and bioclastic limestone 

and siltstone; caninoid and syringoporoid corals, and brachiopods. Unit 

is mostly covered _________ 67

8. Silty limestone, medium-light-gray; 

weathers light gray and light olive 

gray; thin bedded; platy; poorly 

preserved fusulinids ________ 2

7. Calcareous quartzite and arenaceous 

limestone, interbedded; light olive 

gray; weather dark yellow orange 

to pale yellowish gray; medium 

bedded to massive; locally pitted 

weathered surface; sparse coral and 

bryozoan fauna. Unit is poorly exposed _______________________

6. Arenaceous limestone, calcareous 

quartzite, and ferruginous sandstone, interbedded; light olive gray 

to light grayish tan; weather dark 

yellowish orange, grayish orange, 

and pale yellowish brown; medium 

bedded to massive; well jointed; locally platy; interlayered orthoquartzite and silty limestone; worm 

trails in ferruginous sandstone ____

86

65

5. Orthoquartzite and calcareous quartzite, 

interbedded; buff to tan and light 

gray; weather tan to light brown; 

medium bedded to massive; well 

jointed; banded layers; local crossbedding, ripple marked in upper 

part; interlayered thin brownishgray arenaceous limestone; worm 

trails in limestone __________ 257
A38 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Thickness

(ft)

4. Orthoquartzite, buff to tan; weathers 

light brown; medium bedded; 

jointed; banded; ripple marked; 

channel scour and fill; interlayered 

thin calcareous quartzite ______ 259

3. Orthoquartzite, buff to tan; weathers 

tan and brown; medium bedded; 

banded ________________.

2. Orthoquartzite and calcareous quartzite, interbedded; buff; weather tan to 

light brown; medium bedded to massive; banded; crossbedded; ripple 

marked. Unit is partly covered __

1. Arenaceous limestone, medium-gray; 

weathers light grayish tan; medium 

bedded; caninoid corals up to 6 in. 

long, productid brachiopods, bryozoans, crinoids, and fusulinids __

91

32

24

Total measured thickness _____ 3,240 

Conformable contact.

Oquirrh Group, Bingham Mine Formation, 

Clipper Ridge Member.

Fossils in the Markham Peak Member are sparse 

and poorly preserved; the position of representative 

collections is shown in the measured sections and in 

table 7 and are discussed by Gordon and Duncan 

in the section on biostratigraphy and correlation. 

Welsh (in Welsh and James, 1961, p. 8-9) also has 

identified comparable fusulinid collections independently. The age assignment of the Markham Peak 

Member to the Missouri and Virgil is based on these 

sparse and poorly preserved fusulinid collections in 

the Oquirrh Mountains. Welsh reported that the 

upper 1,200-1,500 feet of the Bingham Mine Formation, below a chert pebble conglomerate that he 

regards as the Pennsylvanian-Permian boundary, 

contains a fauna of Virgil age and that the fossils 

above are of Wolfcamp age. However, this age relation was based largely on faunas identified in the 

type section of the Bingham Mine Formation at 

South Mountain (see fig. 4, section 6b). Subsequent 

studies by R. C. Douglass (written commun., March 

13, 1966) indicates that probable Missouri fusulinids, Triticites sp., persist well up into the Markham Peak section. Collection f23431, on a ridge 

northeast of Clipper Peak near the crossing of an 

abandoned tramway line, contains Upper Pennsylvanian Triticites sp. Collection f23432 from the east 

ridge of Markham Peak at about the 8,000-foot contour contains Triticites'! sp. and Pseudofusulinella 

sp. In collection f23433 from the same ridge at the 

8,080-foot contour "the fusulinids are recrystallized,

obliterating almost all structure. They appear to represent a large Triticites suggestive of Virgil age." 

Comparable Upper Pennsylvanian rocks occur in 

the downfaulted block east of Stockton, and south 

of Settlement Canyon. We find no well-identified 

well-preserved fossils of Wolfcamp age in the uppermost strata of the Markham Peak Member in the 

Bingham sequence. Gordon and Duncan describe 

(p. A54) an unusually large fossil collection near 

Lark that they believe is of Virgil age and which 

probably correlates (in age) with a similar assemblage in the lower part of the Kessler Canyon Formation in the Rogers Canyon sequence.

While the absence of a Wolfcamp fauna in the 

Rogers Canyon sequence may well indicate a period 

of nondeposition or erosion during that time, we do 

not believe that the absence of these fauna in the 

Bingham sequence is a strictly comparable phenomenon. Indeed recognition of the presence of what we 

consider to be Oquirrh Group strata of Wolfcamp 

age on South Mountain by Welsh and James (1961, 

p. 6), in a sequence lithologically related to the 

Bingham sequence, and confirmed in our South 

Mountain collections by R. C. Douglass (written 

commun., 1962), and recognition in the snthern 

East Tintic Mountains in the Bingham sequence of 

the fusulinids Schwagerina and Pseudoschwagerina 

Douglass (written commun., 1959) in uppermost 

Oquirrh sediments underlying the Diamond Creek 

Sandstone, suggests to us that sediments of Wolfcamp age were deposited in the Bingham sequence 

rocks wherever they were accumulated before thrusting. These rocks have since been eroded in the 

Oquirrh Mountains, following the uplift of the 

range during late Tertiary time. Gordon and Duncan discuss some of the broader regional correlations of the Bingham Mine Formation.

BIOSTRATIGRAPHY AND CORRELATION

OF THE OQUIRRH GROUP AND RELATED

ROCKS IN THE OQUIRRH MOUNTAINS, UTAH

BY MACKENZIE GORDON, JR., and HELEN M. DUNCAN

The Carboniferous and Early Permian rocks of 

the Oquirrh Mountains are very fossiliferous locally. 

The fossils provide a reasonably accurate bssis for 

dating these rocks. They also provide a faunal or 

biostratigraphic framework for correlating the formations of the Rogers Canyon and Bingham 

sequences, which on a lithologic basis alone would 

probably have been correlated somewhat differently. 

It was in part the discovery of Mississippian fossils 

in the Green Ravine-Rogers Canyon measured 

section through a considerable thickness of rocks
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH AS 9

that resemble those of the Pennsylvanian Oquirrh 

Group in Soldier Canyon that ultimately led to the 

concept proposed by Tooker and Roberts of two 

different rock sequences separated by thrust faults.

Because these sections are of considerable interest 

and import and because the fossil faunas have 

played a prominent part in setting forth the geologic story, the biostratigraphy is being presented 

in this separate discussion. We are indebted to the 

authors of the main part of this paper for the 

opportunity to record our fossil determinations and 

biostratigraphic interpretations. We also are indebted to them for their continuous interest in 

these aspects of the problem and for having been 

indefatigable fossil collectors during the course of 

their fieldwork.

Most of the fossils upon which this report is 

based were collected by Tooker and Roberts between 

the years 1956 and 1966. Some of the largest collections were made by them in company with the 

writers. Brief visits were payed to the area by 

Gordon in 1957, 1962, and 1969 and by Duncan in 

1961 and 1962 at which times extensive collections 

were made.

The megafossil collections used in preparing this 

report, 119 in all, are confined with few exceptions 

to the type and reference sections of the formations 

in both sequences. The collections are shown on six 

tables, which list the fossils identified in each formation. Five of the tables are arranged in stratigraphic sequence and record the distance in feet 

above the base of the formation of the bottom of the 

unit from which the collection was taken, as well as 

the number of the unit in which it was made. On 

the sixth, which records collections from a relatively narrow stratigraphic interval, such an arrangement was not feasible. The fossils in these 

lists were identified by several paleontologists. Most 

of the corals and bryozoans were identified by H. M. 

Duncan; several Late Mississippian colonial corals 

were studied and reported upon by W. J. Sando, 

and two sponges were examined by R. M. Finks. 

Gastropods were identified by E. L. Yochelson. The 

rest of the fauna, principally brachiopods and pelecypods, were identified by M. Gordon, Jr. The fossils were classified principally as to genus because 

many of the species appear to be new.

Fusulinids are abundant in some beds, particularly in the upper part of the Oquirrh Group. These 

were studied by R. C. Douglass, who also made collecting trips into the Oquirrh Mountains in 1958 

and 1962. The forams in 36 collections identified by 

Douglass are listed in the register of late Paleozoic

f usulinid collecting localities given later in this report 

His age determinations are included here in the discussion that follows. These results constitute only a 

minor part of Douglass' study as most of his collections were from areas outside of the type sections. Other microfossils, such as ostracodes and 

conodonts, were not studied.

In the fossil tables the letter symbols opposite 

each species give an indication of relative abundance as follows:

R = rare,

X = fairly common,

C = common,

A = abundant.

These were determined in most collections by th«j 

following criteria: rare=less than 5 specimens; 

fairly common=5 to 25 specimens; common=26 to 

100 specimens; abundant^more than 100 specimens. 

In small collections and where large colonial forirs 

were involved, an augmentative factor was applied 

more or less subjectively in order to give a mor*? 

realistic estimate.

Most of the fossils in the formations of both 

sequences are silicified, or at least partly silicified. 

This includes the fusulinids, many of which appear 

to have been reworked. Limestone beds in the formations below the Grandeur Member of the Park 

City Formation generally contain a considerate 

content of silt. The silt component interferes with 

the process of etching out the fossils in dilute hydrochloric acid and forms an interlocking matrix that 

must be removed manually by scraping the surface 

of the fossils with a needle or dental tool. Many of 

the fossils have been distorted by structural disturbances that have taken place since their deposition. Nevertheless, it is possible to secure reasonably 

well preserved examples by working carefully ard 

by selecting from fairly large samples.

ROGERS CANYON SEQUENCE

About two-thirds of our collections, 83 in all, 

came from the Rogers Canyon sequence. The five 

late Paleozoic formations that make up this sequence 

are in ascending order: the Green Ravine Formation of Mississippian age, the Lake Point Limestone 

of Mississippian and Pennsylvanian age,4 the Erda 

Formation of Pennsylvanian age, the Kessler Can-

* Since the preparation of this report, it has been determined tt at 

paleontologic evidence shows a slight difference in the boundary of the 

Lower and Middle Pennsylvania Series as used in the midcontinent 

when correlated with the type Pennsylvanian in the Appalachian 

region. Indications are that part of the Morrow is Middle Pennsylvanian in age.
A40 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

yon Formation of Pennsylvanian and Permian (?) 

age, and the Grandeur Member of the Park City 

Formation of Permian age. Collecting localities in 

these formations are listed at the end of this report.

GREEN RAVINE FORMATION

The Green Ravine Formation can be separated 

into three parts biostratigraphically: a -pre-Caninia

Zone part containing a predominantly bryozoanbrachiopod fauna and locally a number of small 

mollusks; the Caninia Zone with corals and chaetetiform bryozoans predominant; and a post-Cawm'a 

Zone part populated mainly by brachiopods. The 

fossils in 25 collections from the type section of 

this formation are listed in table 1.

TABLE 1. Megafanna of the Green Ravine Formation in its type section 

[Symbols explained in text]

Unit

Distance, in feet, above base of formation _ __ __ ___ _ _

USGS colln. No.

Corals : 

AmpJejcizaphrentis sp

Caninia cf. C. excentrica (Meek)

Horn coral, gen. & sp. indet

Lithostrotion stelcki Nelson

Multithccopornt n. sp

Aitlopora sp

Favositid, small form, gen. & sp. indet

Bryozoans : 

Fistuliporoid, encrusting form

ramose form

RamiporaJia sp

Trepostome. encrusting form

ramose form

Stenoporoid, massive form

ramose form

Tabttlipora sp

RtenopliraqmirHiim! sp

Chaetetiform brvozoan, n. gen. A. sp. 1

Chaetetiform hrvozoan, n. gen. B. sp. 1

FeiiesteUa spp

PoJypora sp

Penniretepora sp

Iclithitoracliisl sp

Tlinmniscitsl sp

Rhomboporoid, gen. & sp. indet

Ciistoclictiia sp. A

sp. B

Bchinoderms : 

Crinoid coluninals

Crinoirt plates and spines

Pelmatozoan debris

Worms : 

Spfrorliis sp

Brachiopods : 

Sclii-ophoria sp

Leptaqottia sp

KrJiucltertelln sp

Ortltotetcx aff. O. ocfiilentnlis Lane

Ruqosochonetcs sp

Heteralosia sp

Promarqinifera n. sp

In flat in sp

Fle.raria sp

Bitj'tnnin sp

Echinoconcli/is rorleocntsix Hernmi. var

fHapJirngmiiH aff, I), rcxtriciinin (Worthen)

Antiqiiatotiia aff. A. penioftomi Easton 

Gratia sp. A

sp. B

Produetoid, gen. & sp. indet

LeiorJiiincJiiix far'boniferum GirtvV

PsiJocHinaral sp

Spirifer brazeriaitux Girtv

Aiitlirai-ospirifer sp

Spiriferoid. gen. & sp. indet

Pitnctospirifer tramtrerxiix (Mc< 1 liesne\ )

ReticuJarihia campeHtrin ( White I

Hustcdia sp

Cniritlniris sp

Alartininl sp

('leiotfiiii'irtina up A

S

&

CC

Cl

TH 

TH

X

X

R

X

O5

* ,

s

X

6

§

^

-t

o

X

X

R

C

R

X

X

R

X

C

c

c

R

X

C

A

c

R

R

R

X

X

c

X

R 

R

R

R

p

R

X

R

A

Cl

OS

O

PH

c:

TH 

TH

,

X

R

X

R

ft

f-t

X

R

 >

R

X

C

tcs

O 

I

 t 

ti

R

R

 )

R

X

R

R

R

R

R

C

R

C

X

X

R

^

R

R

R

X

H

R

X

10

C5

o:

O

1

1C

X

?

OS

c

O

ti

cc

cc

c

X

R

cc 

c

PH

e-i

X

X

X

X

R

X

R

R 

R

OS

or 

C

o

PH

OS

c

C

R

X

R

R

X

X

X

R

''.

K

If

K

ts

c

£

20248

c 

c

O

PH

OS

cc

X

X

X

TH

CT 

O

O

PH

s

X

X

R

R

R

R

R

R

X

R

es 

c

O 

P,

c

X

-t 

tc

O

PH

C

or

X

X

X

X

?

R

R

11

-t

o

O

PH

TH

OC

TH 

TH

R

R

?

X

X

X

R

R

X

R

X

C

R 

R

R

R

C

TH

g

1C

b

R

X

R

es

TH

o

TH

CC 

OC

C

C

X

ifl

TH

o

PH

c:

TH

O

10

o

X

X

«*- 

O

1C

o

X

X

R

X

R

X

R

R

R

X

R

X

C1"

0

PH

1Ctl

o

R

X

X

X

c

R

1

H

X

X

R

R

«*- 

O

PH

TH

1C 

O

Cl 

GO 

f

ft

1C

o

1?,

o

0101

0

PH

THl-r-l

R

R

X

R

C

K

K 

R

R

R

R

 >

X

X

R

o

O5

O

PH

COr-i r-i

X

(1

R

X

X

li

1

1

CO 

CO

r-l

H

X

X

li

X

u
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A41

TABLE 1. Megafaima of the Green Ravine Formation in its type section Continued

[Symbols explained in text]

Unit

Distance, in feet, above base of formation _ __

USGS colln. No

Brachiopods Continued

Pelecypods :

Gastropods :

Cephalopods :

Fish:

10i 

U

H

COei

TH

TH

R

IN

05

u&

CO *

CI

R

M

OS

U

H

so *

?1

o

X

?

R

R

R

R

X

R

R

R,

R

R

R

R

R

R

R

R

R

IN

05

U

&

O5 

?>

TH 

TH

IO5

u&

I- *

M

O

R

10

O5 

05 

Iu&

IO 

CO 

CO

so

O5 

IN

O

u&

M

CO 

COto

1-1

CO

o

u

111

1

CO 

IK 

n

O5 

CO

e

g

O5 * 

IN

O

R

o to 

o

U

111

-tn 

(N

O

O

so 

o

U

H

05 

IN

CCto

THto

O

U 

'V

O 

CO

TH 

TH

05to

0

U*v

10

w

o

 * 

to

u

111 i

cc

COto

11

3

U 

^i-i

CO

TH

R

 *

o

U 

'V

i-10

(M

O

X

OS 

M

8

TH

CO

CO 

SO

O5 

M

u

Hi

CO *

THt05 

SO

U

Hi

si

10 

M

O

X

u

Hi

o 10

M

O

X

R

R

U

Hi

N

1O 

IN

O

R

U

Hi

TH

10 

M

O

05 

CC 

M

i-l

U

Hi

«*

10 

IN

O

X

o o>

IN

iH

u

Hi

"JH 

 * 

1-1 

ITH

 \?,

o

05 

IN

TH

0

Hi

M

CO 1-1 

1-1 

N

05 

05 

01

i-l

uHi

CO

CO 

CO

so

TH

The lowest of these faunas occurs in unit 6 of the 

type section. Five collections through the lower 30- 

35 feet of this unit have yielded some 65 species of 

megafossils. The principal coral in these beds is 

Amplexizaphrentis sp., and locally Aulopora sp. is 

common; however in general corals are not nearly 

as abundant as in the upper middle part of the formation. A few caninoid corals occur in loose slabs on 

the slopes but probably have come from higher in 

the section.

Bryozoans are present in profusion. Among the 

common forms are species of Fenestella, Polypora, 

Penniretepora, and Cystodictya of the group of C. 

lineata Ulrich. A narrower species of Cystodictya is 

even more abundant. The most common brachiopods 

include the tiny productoid Promarginifera n. sp., 

Reticulariina campestris (White), and a small species of Cleiothyridina. In one collection, 18 molluscan species were identified, most of them small 

gastropods.

The Caninia Zone occupies units 10 and 11 of the 

type section. The top of unit 11 coincides with the 

type of this zone. The stratigraphic position of the 

base of this zone is as yet undetermined but may 

lie within unit 9. The Caninia Zone exceeds 400 feet 

in thickness and may be more than 500 feet thick. 

Sixteen collections from this zone have been examined, all but one of them from unit 11. The dominant fossils of this zone are the large solitary corals 

Caninia cf. C. excentrica (Meek) and the less common form referred with some question to Caninia 

nevadensis (Meek).

Two species of syringoporoid corals in this rxme 

were examined by W. J. Sando (oral commun., 

1969) who found them identical to new specie? of 

syringoporoids he is describing from the Caninia 

Zone in the Amsden Formation in western Wyoming. One of them, having closely packed corallites, 

represents a new genus and the other is referred 

with question to Multithecopora. Lithostrotion 

stelcki Nelson, a colonial coral that is widely distributed in the late Chester equivalents in western 

Canada and Alaska, occurs locally.

Chaetetiform bryozoans in colonies up to nearly 

1 foot across also are common. Many of these colonies, particularly the smaller ones, started by growing on bellerophontid gastropod shells, at least some 

of them during the life of the snail. Continued 

growth of the colonies probably robbed the snail of 

its ability of locomotion and brought the unfortunate 

animal to an untimely end. Also present in the 

Caninia Zone are Tabulipora and other stenoporoid 

bryozoans and Fenestella.

Among the brachiopods, a species of Antiquatonia 

related to A. pernodosa Easton is commonly formd 

in limestone beds that alternate with the coral-
A42 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

bearing limestones. Other characteristic brachiopods 

include Flexaria sp., a form related to Diaphragmus 

cestriensis (Worthen), Spirifer brazerianus Girty, 

Reticulariina campestris (White), and Cleiothyridina sp., which attest to the Chester age of the beds.

The vost-Caninia Zone part of the formation is 

limited to unit 12 of the type section. Its fauna is 

distinguished by the absence of the corals so abundant in the underlying rocks, the continued survival 

of most of the brachiopod species of the Caninia 

Zone, and the appearance of several new forms. 

Relatively common in unit 12 are species of Schuchertella, Rugosochonetes, Inflatia, Diaphragmus, 

Antiquatonia, Reticulariina, and Cleiothyridina. One 

of the four collections consists of a single bellerophontid gastropod.

Correlation and age. The Caninia Zone is distributed widely in Late Mississippian rocks of the 

western United States. This is the K Zone recorded 

by Dutro and Sando (1963, p. 1974) in the Monroe 

Canyon Limestone of the Chesterfield Range, Idaho. 

This zone occurs also in the lower part of the Amsden Formation in the Salt River Range, Wyoming 

(Sando, 1968, p. D34). It has been recognized also 

in the Doughnut Formation in the northern part of 

the Wasatch Range and is present also within the 

upper part of the Chainman Shale in the Confusion 

Range and at Granite Mountain, Utah.

In the southern part of the Wasatch Range and in 

the Bingham sequence in the southern part of the 

Oquirrh Mountains, the Caninia Zone lies within the 

Great Blue Limestone. In the Bingham sequence it 

occupies an intermediate position between the Long 

Trail Shale Member and the top of the formation. 

The age of this zone is principally middle Chester, 

but it is probably in part late Chester in age.

The shaly fossiliferous beds of the lower part of 

the formation contain fossils such as Spirifer brazerianus Girty and Reticulariina campestris (White) 

that in association indicate Chester age. A precise 

correlation with the Upper Mississippian Chester 

type section is not possible at present. Lithologically, 

according to stratigraphic position, and in part 

faunally, these beds are correlated with the Long 

Trail Shale Member of the Great Blue Limestone in 

the Bingham sequence of the Oquirrh Mountains and 

to the Paymaster Member of the same formation 

in the East Tintic Range. Some of the common and 

characteristic Long Trail and Paymaster species are 

absent. This is believed to be a facies, rather than 

an age difference, suggesting a somewhat restricted

distribution and a more remote point of origin for 

the Green Ravine assemblage than its present geographical location in relatively close proxinity to 

the Bingham sequence indicates.

LAKE POINT LIMESTONE

Two faunal zones, widely distributed in Carboniferous rocks in the Great Basin, are recognized in 

the Lake Point Limestone. The Rhipidomella nevadensis Zone in the lower part of the formation is 

Late Mississippian (late Chester) in age. VHiat is 

yet informally called the Rugoclostus zone, in the 

upper two-thirds of the formation, is Early Pennsylvanian (Morrow) in age. The productoid brachiopod genus Rugoclostus Easton is widely distributed 

in the Great Basin and Rocky Mountain regions and, 

so far as we have been able to determine, is restricted to west American rocks of Morrow ajre. The 

stratigraphic distribution of these two zones, represented by 23 fossil collections, is shown in table 2.

The lowest occurrence of Rhipidomella nevadensis 

(Meek) was recorded 143 feet above the base of the 

formation. This species continues in some abundance through the next 30-35 feet of beds upward, 

but in rocks still higher it seems to be absent. The 

same brachiopod is common in a 54-foot cliff-forming limestone (unit 2 of the type section), the top 

of which lies roughly 390 feet stratigraphically 

above the lowest occurrence of R. nevadensis and 48 

feet stratigraphically below the base of a 5-foot 

limestone bed crowded with phaceloid colonies of 

the coral Orygmophylluml (unit 4 of the type section) .

In between the two intervals with abundant R. 

nevadensis the rocks are not highly fossiliferous, 

but several thin shaly limestone beds are crowded 

with frondescent Archimedes. Two such beds occur 

in unit 1 at 192 and 208 feet, respectively, below the 

top of the cliff-forming limestone (unit 2). The 

Archimedes resemble those that occur in the type 

section of the Manning Canyon Shale, 405-415 feet 

above its base, in the Bingham sequence.

In the cliff-forming limestone (unit 2), besides 

the relatively abundant R. nevadensis, the following 

faunal elements indicate Mississippian age: Inflatia 

sp. A and B, Flexaria sp. A, Carlinia phillipsi (Norwood and Pratten), C. diabolica Gordon, Ovc-tia sp. 

A, and Spirifer brazerianus Girty, var. All of these 

species are fairly common in very late Mississippian 

beds in other parts of the Great Basin, and none of 

them is known in beds of Pennsylvanian rge. In 

some areas, for example at Conger Mountain in the 

Confusion Range,. Utah, R. nevadensis is alsc found
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A43

TABLE 2. Megafauna of the Lake Point Limestone in its type section

[Symbols explained in text]

Unit _ _ _

USGS colln. No _ _ _

RHIPIDOMELLA NEVADBNSIS ASSEMBLAGE

Corals :

Bryozoans : 

Fistuliporoid, encrusting form

Fistuliporoid, massive form _ _ _

Trepostomatous bryozoan, gen. & sp. indet _ _

Polypora sp

Archimedes _

Rhomboporoid, gen. & sp. indet

Echinoderms : 

Crinoid columnals _ _

Pelmatozoan debris

Echinoid ( ?) spines _ _ _

Brachiopods : 

Schizophoria cf. 8. texana Girtv _

cf. 8. resupinoides (Cox)

RhipidomeUa, nevadensis (Meek)

ScfiucherteUa sp. A _

Orthotetes sp _____

Riigosochonetes aff. R. pseudoUratus (Easton)

Inflatia sp. A

sp. B _

Scoloconcha sp

Marginiferid, gen. & sp. indet

Flexaria sp. A

Carlinia phillipsi (Norwood & Pratten)

dia'bolica Gordon _ _ _

O vat ia sp. A

sp. B

Spirifer brazerianus Girty, var

Antfiracospirifer sp _ _ _ _ _

Crurithyris sp _.

Cleiothyridhia of. C. sublanifUosa (Hall) _ _

Composita sp _

Beeclteria sp

Pelecypods : 

Sulcatopinna sp

Scaphopods : 

LaevidentaUuml sp. indet _ _

Gastropods : 

Belleropfton ? sp. indet

KnightHes (Retispira) sp. indet

JEuphemiles sp. indet

Gen. indet. cf. Clolpites sp _

Rhineoderma! sp. indet

Trepospira (Trepospira) sp _

Baj/lea ? sp. indet _

Pleurotomariacean, gen. & sp. indet _ _ _

StropJiostyliis'i sp. indet _

Naticopsis sp

Stegocoelia sp _ _ _

Eotrochusl sp. indet

Paleostylus"! sp. indet _ _

Strobeus sp

Meekospira sp _

Cephalopods : 

Reticycloceras sp

Trilobites : 

Paladin sp _ _

Fish: 

Fish dentition _ _

RUGOCLOSTDS SEMISTRIATUS ASSEMBLAGE

Corals : 

AmplexizapJirentis"! sp

LopJiophi/Uidium sp _

OrygmophyUuml sp

Ganinia sp

Bryozoans : 

Fistuliporoid. encrusting form

Eridopora"! sp

Tabulipora'i sp

Stenoporoid, encrusting form

ramose form

Fenestella spp

Poltiporella sp

Poylpora sp

EnaJlopora"! sp

Rhomboporoid, gen. & sp. indet

Echinoderms : 

Crinoid columnals

Pelmatozoan debris

Echinoid spines

Brachiopods : 

Schisophoria sp

Orthotetesl sp

Riigoclostus semistriatus (Meek)

!

o

1

R

C

R

PH 

 *

X

X

X

R.

X

R

A

R

R

R

C

R

R

R

R

R

R

X

R

R

R

R

R

R.

X

X

R

R

?

IO

X

1

P^

tR

R

X

X

R

R

X

R

X

R

R

R

36-PC '.

rt

R

X

(i

R

O

C

0

R

 >

p

p

CL, 

i>

TH

X

X

p

R

39-PC 5

rt

R.

R.

X

R

X

R

R

R

R

X

R

X

X

X

R

?1

O

«V 

1-1

1-1

X

X

R

X

R

R

3

?

,H

O 

P 

O

CO

P

R

4

^r

o:

0

f-i

46-PC

tr

19-PC

tO

R

R

?

IN

CO

R

R.

R

r»

i.

tR

X

X

X

R

00

3

CO 

<N

CO

R

fl.

X

CD

? * 

<N

CO 

CO

R

R

«

48-PC

tR

R

R

X

X

X

X

X

R.

R.

^

©

3A *

lX

R

R

?

X

X

S

50-PC <

t9

K

a

S

riir

oc

er

X

X

11

CO 

CO

F-T

O

 V

10 ift

00

CO

R.

X
A44 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

TABLE 2. Megajauna of the Lake Point Limestone in its type section Continued

[Symbols explained in text]

Unit

Distance, in feet, above base of formation ___ __ __ _ ___ __ 

USGS colln. No. _

Brachiopods Continued 

Rugoclostus Continued

aff. A. rocki/montanus (Marcou) _ _

Oleiothi/ridina of. C. or'bicvlaris (McChesnev)

Composita sp

Reecheria cf. B. Itoridens (Morton)

Dielasmoid, gen. & sp. indet

Gastropods :

Trilobites : 

Paladin sp _

CO-tl

rH

0

k

10

rn

t-

"tl 

rH

£ 

-tl

ei

-ti

10

rH

O

OH

1-5

CO

M

1

COtrH

O

A

JH

O

1O-x. 

tl

o

A

CO

Cl

tCl

CO

O 

PH

GO

N

(35 

CO 

05

O 

A

i~

Cl

rH 

r-t

O

O

A

i

M

 >

O 

rH 

1O

0

A

rH-h

Cl

a

Cl

CO 

1O

O

A

o

CJ

C

R

C

X

R

CO 

GO 

10

O 

A

oo

CO

R

4

COyj

10

0

A

(35 

10

O

CO 

00 

1O

O

 V

CD

trH

R

Cl 

Cl

CO

O

A

JL

CO 

rH

X

X

00 

Cl

CD

OA

Cl

co

rH

R

R

R

R

5

CO-*

CD

0

PH

ttrH

r

R

X

X

X

R

X

X

X

?

GO 

COtO

A

CO

CD 

iH

R

K

CD 

CD 

t0

5

CD 

rH

X

R

R

R

COt- tO

A

at

rH

c

R

X

R

X

X

X

R

C

X

R

7

o t00

g

JL

trH

X

R

X

R

X

X

X

X

R

X

X

C

X

X

R

R

00 

O 

0

o p-l

o

trH

R

r

R

9

t-

(35 

rH

iH

O>t

-tl

COci

R

?

R

R

R

11

CD 

CO 

CD

r-T

O>t

10 

10

COCl

X

R

R

R

l)

X

sparingly in beds of undoubted Pennsylvanian age, 

but our observations have shown that where this species is common to abundant, other associated faunal 

elements indicate Mississippian, rather than Pennsylvanian age. In the Oquirrh Mountains R. nevadensis was not found in the Pennsylvanian.

Between the top of unit 2 and the base of the next 

fossiliferous bed, which is Pennsylvanian in age, is 

24 feet of beds without megafossils. For all practical 

purposes the top of unit 2 can be regarded as the 

top of the Mississippian in this section. Nevertheless, 

the actual Mississippian-Pennsylvanian boundary 

probably lies within unit 3 of the type section. A 

detailed breakdown of this unit, measured by Gordon, is as follows:

Unit 4: 

Unit 3:

Orygmophylluml bed.

Thickness

(ft)

j. Limestone, medium-dark-gray, silty, interbedded with some gray limestone; poorly fossiliferous _______________ 23

i. Silty limestone, like bed below but crowded 

with silicified productoids (USGS colln. 

21140-PC) ___________________ 1

h. Silty limestone, medium-dark-gray (weathers brownish gray) ; some gray limestone 6

g. Limestone, gray (weathers light bluish

gray), rather fine grained ________ 5

/. Covered ______________________ 2

Thickness

(ft)

e. Sandy limestone, medium-dark-brownishgray, fine-grained, in two slabby layers _ 1 

d. Limestone, gray (weathers bluish gray), 

medium to fine-grained; some vertical 

calcite veinlets up to V% in. wide ____ 2.5

c. Covered __-_____________ 3

b. Brecciated limestone, gray, containing 

light-brown siliceous boxwork surrounding limestone fragments up to 1 in. 

across, particularly well developed ir 

upper 6 in. __________________ 1.5

a. Shale, buff, silty, and nodular limestone

(weather brownish gray) ___ 3

Total ________. 

Unit 2: Cliff-forming limestone.

48

At our present state of knowledge of Great Basin 

Carboniferous stratigraphy we are inclined to place 

bed a of unit 3 in the Mississippian and refer the 

rest of the unit to the Pennsylvanian. This reasoning is based upon the fact that beds of Htl N ology 

similar to bed a occur in the Confusion Range abovebeds containing Carlinia (Gordon, 1970) and carry 

Mississippian fossils including R. nevadensis 

(Meek), Inflatia n. sp., Diaphragmus n. sp., and 

locally Pentremites n. sp. (of Mississippian affinities). These Mississippian beds in western Utah 

were included by Hose and Repenning (19-^9, p. 

2173) in the lower part of the Ely Limestone.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A45

The brecciated limestone, bed b of unit 3, is regarded as marking the base of the Pennsylvanian 

and delimiting a minor hiatus wherein these latest 

Mississippian beds, generally thicker in sections 

near the western limits of Utah, may have been 

partly removed by erosion.

The lowest fossils of undoubted Pennsylvanian 

age occur in bed i of unit 3. This bed is crowded 

with shells of the productoid Rugoclostus aff. R. 

semistriatus (Meek) associated with Anthracospirifer occidmis (Sadlick). The Rngoclostus fauna is 

distributed through at least 1,075 feet of section in 

the Lake Point Limestone, from the middle of unit 

3 to the upper part of unit 11. It is typically an 

assemblage of large productoid brachiopods of the 

genera Rugoclostus, Flexaria, Echinoconchus, Antiquatonia, and Linoproductus. Commonly associated 

with them are Anthracospirifer occiduus (Sadlick), 

Neospirifer cf. N. cameratus (Morton), Composita 

sp. Punctospirifer transversus (McCheshney), and 

Reticulariina campestris (White), the last two continuing upward from beds of Late Mississippian 

(Chester) age.

The 5-foot limestone bed with Orygmophyllum'! 

(unit 4) occurs in the type section of the Lake Point 

Limestone only 24 feet above the base of the Rugoclostus zone. Most of the corals in this bed are concentrated in a 2-foot zone in the middle of it. Another 

area where Orygmophylluml occurs in countless 

numbers in a single bed is the Confusion Range. The 

corals are in a 5-foot calcareous shale about 550 feet 

above the base of the Ely Limestone. This coral was 

identified as Barb our ia sp. in Hose and Repenning 

(1959, p. 2171). They (p. 2173) as well as the writers regard the lower 40-60 feet of the Ely Limestone 

in that area as Mississippian in age. Because the 

Orygmophylluml bed occurs there high in the Rugoclostus zone, some 500 feet above the base of the 

Pennsylvanian, scant likelihood exists that its deposition was contemporaneous with the one in the 

Lake Point Limestone.

Typical silicified brachiopods of the Rugoclostus 

zone are abundant in the lower 200 feet of the zone. 

Above this the fossiliferous beds are fewer and more 

widely spaced. In some beds Anthracospirifer is 

present to the exclusion of almost all other species. 

In several of these the spirifers are not silicified. 

Silicified Rugoclostus and Antiquatonia were observed well up in unit 9 of the type section, but were 

not collected. Flexaria was recognized in a calcareous 

sandstone bed a few feet below collection 23855-PC. 

No collections were made in the upper 100 feet of the 

formation in the type section. i

One other collection, from the upper part of the 

formation but not from the type section, should be 

mentioned. This is from a bed on the north s: de of 

Big Canyon, the first canyon south of Green Ravine 

(USGS colln. 16337-PC), which contained the following species:

Hederella sp _--__ - _____ X 

Fistuliporoid bryozoan, incrusting form R 

Stenoporoid bryozoan, incrusting form R 

Derbyial sp. indet _ - R 

Flexaria sp - R 

Linoproductus nodosus (Newberry) C 

Anthracospirifer opimus (Hall)? '-- X 

Cleiothyridina cf. C. orUcularis (McChesney) __ R 

Composita sp ___-_-_-__ -- ----- C

The presence of numerous shells of Linoproductus nodosus in this bed is noteworthy because of 

similar occurrences of the same species near the top 

of the West Canyon Limestone of the Oquirrh Group 

in the Soldier Canyon section of the Bingham 

sequence and at approximately the same stratigraphic level in Provo Canyon in the Timpanogos 

sequence in the Wasatch Range.

Correlation and age. As interpreted in the foregoing discussion the type section of the Lake Point 

Limestone measured by Tooker and Roberts includes 

538 feet of beds of Late Mississippian (late Chester) 

age and 1,199 feet of beds of Early Pennsylvanian 

(Morrow) age. The zone of uncertainty (without 

megafossils) as to the precise level of the Mississippian-Pennsylvanian boundary is actually 24 feet 

thick.

Some of the fossils of the Rhipidomella nevadensis Zone are present also in the type section of the 

Manning Canyon Shale, about 15 miles to the south 

of the Lake Point Limestone type section, in the 

same range. The topmost 100 feet of the Marning 

Canyon, which is gradational into the overling 

Oquirrh Group at Soldier Canyon, contains fossils 

typical of the Rugoclostus zone. The top of the Manning Canyon corresponds to an undetermined level 

in the Lake Point Limestone, probably a few tens 

of feet above the Orygmophyllum'! bed (unit 4). 

Orygmophyllum'!, however, has not been fourd in 

the Manning Canyon Shale. The entire thickness of 

;he Manning Canyon is believed to be represented 

by little more than the lower 600 feet of the Lake 

Point Limestone.

The upper part of the Lake Point Limestone is

.tratigraphically equivalent to the West Canyon

jimestone of the Oquirrh Group. The upper contact

of both units is believed, on faunal as well as lithoogic grounds, to lie at approximately the same

stratigraphic level.
A46 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

The significance of the bed (or beds) with abundant Linoproductus nodosus near the top of the Lake 

Point Limestone as well as the West Canyon Limestone of the Oquirrh Group is an indication of late 

Morrow age. In the Appalachian region, in eastern 

Kentucky, L. nodosus is abundant in the Kendrick 

Shale Member of the Breathitt Formation, formerly 

thought to be of Atoka age but now regarded as 

Morrow. This species is replaced by a different 

Linoproductus in the slightly higher Magoffin Beds 

of Morse (1931). The ammonoids of the Kendrick 

(Furnish and Knapp, 1966) belong to the same zone 

that occurs in the Trace Creek Shale Member of the 

Bloyd Formation in the type section of the Morrow

Series in northwest Arkansas. L. nodosus is not 

known in the Atoka Formation of Arkansas and 

Oklahoma. For these reasons L. nodosus is presently 

regarded as a late Morrow species with a geographically extensive peak zone.

ERDA FORMATION

The Erda Formation contains several faunal assemblages which indicate that this formation is 

Middle Pennsylvanian in age. Twenty collections 

from the type section and two from recognizable 

horizons in nearby sections were studied; the fossils 

ara listed in table 3. Microfossils in four collections 

determined by Douglass are listed in the lithologic

TABLE 3. Megafauna of the Erda Formation type section

[Symbols explained in text]

Unit

USGS colln. No

MULTITHECOPORA-KOZLOWSKIA ASSEMBLAGES

Corals : 

Caninia sp

sp. indet _ _

MttltitJiecopora sp. A

Multithecopora'! sp. B

Bryozoans :

Ancopora sp. A _ _

FenesteUa cf. F. xerratula var. of Condra & Elias __

Echinoderms :

Brachiopods :

Desmoinesia ingrata (Girtv)?

Rugoclostus'i sp _ _ _____

Linoproductus sp. indet

occiditus (Sadlick) ?

Cleiottiyridina cf. C. orbicularis (McChesney)

Composita ovata Mather _ _ _ _ _____

ANTIQUATONIA-HYSTRICULINA ASSEMBLAGE

Corals :

Stereostylus sp

Auloporoid, gen. & sp. indet

Bryozoans : 

Ascopora sp. B

TabuJipora sp. A _

sp. B

Stenoporoid, ramose form _ _ _

Diploporaria sp

RhombocJadia sp

Worms : 

Spirorbis sp _

Brachiopods : 

Derbi/ia cf. D. crassn (Meek & Hayden)

Meekella striatocostata (Cox)

Chonetinella cf. C. alata (Dunbar & Condra)

Hystricullna sp

O

^

"*

M

R

1

t10

0

hM

10

X

R

R

?

fi

00

0

^

in

R

R

R

O 

^

10

R

3

to

Cl

0

hM 

1

IO

R

X

 *

o

O

&

10

R

of

X

X

R

R

R

R

t

o t

0 

PH

10

X

fi

011ft

O

hM

i

10

Q

R

R

R

X

X 

X

R

R

R

R

R

R

X

R

X

S

rH 

0\

0 

^

10

R

X

R

R

X

R

C

R

R

 >

1

i^

a

-

O 

«

IO

R

X

X

R

X

R

R

R

R

R

X

R

R

C

0

I-

(N

0

°i

»

11

o

00

O

PH 

I

CO

R

X

?

R

X

X

X

X

R

?

R

O 

^

i-i

'

13

 ^

a

-

g

COi-i

r

t~

00

O 

^

CO

R

X

0

R

R

14

CO

o

O 

w

tl

Cl

X

R

R

1

COift

0

PH

CO

R

R

R

X

 >

9

 *

o

O

hM

CO

CO

X

R

R

X

X

R

R

R

25

IO

T-l

0

w

Cl

R

CO 

CO

O

hM 

1

CO

fl

X

R

X

X

R

 ?

9,7

O 

PH 

1

ec

<ri

R

R

R

R

R

O

PH

CO

CO

(M

R

R
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A47

TABLE 3. Megafauna of the Ercla Formation type section Continued

[Symbols explained in text]

Unit

USGS colln. No

Brachiopods Continued

Fie jf aria sp

Echinaria sp

Antiqiiatonia aff. A. coloradoensis (Girtv)

Khynchonelloid, gen. & sp. iiiclet

Anthracoxpirifer rocJcumontantis (Marcou)

Neospiriferl sp. indet

Grurithuris planiconvejea iShumard)

PhricodotJtyris perplexa (McChesney)

Gastropods : 

Eupltemites sp. indet _ _

Platyceran sp. indet

PRISMOPORA-DESMOINESIA ASSEMBLAGES

Corals : 

Caninoid, gen. & sp. indet

Bryozoans : 

Prismopora cf. P. triangulata (White)

sp

RhombotnipeUa'? sp. indet

Trepostomatous brvozoan fragments

Septopora sp

Pemiiretepora'/ sp

Acanthoeladiid, gen. & sp. indet

RJtabdomeson. sp

Rhombocladia sp

Rhombopora"? sp

Echinoderms :

Brachiopods :

Chonetinella cf. C. nlnta (Dunbar & Condra)

Inflatial sp _

Cancrinella '! sp

Desmoinesia muricatina (Dunbar & Condra)

Antiquntonia sp

Piitictospirifer Jientuclcensis (Shumard)

Cleiotliyridina sp. indet

Pelecypods : 

Parallelodon sp

AcantJiopecten sp

Myalina"! sp. indet

Trilobite :

O

^

-t*

CC

1

bO

O 

^

rH

L^

t'

Cl

00

O

Oi 

1 e-j

K5 

t^

O

Oi 1

CO10 

t0

CC 

C)

o

Oi

 +*

IO

 +*

O

"?

1Cin 

tt

O *

O

Oi

10

tR

R

?i

10

O 

Oi

t10

tS

T-l c-i

O 

Oi

10 

b1

bC6

^-

0

Oi

10 

tX'

R

R

C

R

X

R

c

X

c

0

t 

f)

o

Oi

CC 

b11

V.

a

Hi

co

of

X

R

R

a

Oii Cl

ce

X

1!

R

18

-V

03

0

Oi

CJ

ce

T{

R

boo

a

Hi

co 

bR

X

R

X

R

R

X

X

A

R

R

X

14

 £

O

M-( 

1

C-l

?

R

R

X

R

1

CO 

IO

O

 V

ce 

tX

X

R

r

R

9

 *

o

o

Oi

cc

R

0

R

R

35

0 r-l

O

Hi 

ot

<N

CO

0

R

X

R

P.

X

X

ce

00

O

Oi 

1

COC1

o

 >

R

X

27

O 

fc

CO 

Cl

o

R

 )

R

R

R

R

X

R

X

R

R ?

R

R

R

0

Hi

c-5

c

R

R

Ft

R

r

c 1

R

R

descriptions of the measured sections. With the possible exception of Anthracospirifer opimus (Hall) 

from an uncertain level near the base, no fossils 

were collected in the lower 157 feet of the formation, much of which is quartzite.

Multithecopora, a syringoporoid coral represented 

by two distinct species, ranges through 600 feet of 

beds in units 1 through 6 at levels from 157 to 757 

feet above the base of the formation. We have been 

referring to this interval informally as the Multithecopora zone. Chaetetes was collected 182 feet (in 

unit 1) and Profusulinella 502 feet (in unit 3) 

above the base of the formation. These occurrences 

probably do not, however, represent the Profusulinella-Chaetetes faunizone of Dott (1955, p. 2239). 

According to our observations in other parts of the 

Great Basin, the compound coral Chaetetes is commonly in or interbedded with limestone beds containing Fusulinella and locally ranges upward into 

beds of Des Moines age. Raymond Douglass (oral 

commun., 1969) informs us that his identification of 

Profusulinella' mentioned above is based upon fragmentary and presumably reworked specimens.

Interspersed with the coralliferous beds in the 

upper part of the Multithecopora zone and extending above them stratigraphically are brachiopodbearing beds in which Kozlowskia aff. K. haydenensis (Girty) and Neospirifer cf. N. coloradoensis Ste-
A48 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

vens are rather common. These two species were 

found associated in units 4 through 8, in beds 604- 

921 feet above the base of the formation.

The next highest brachiopod assemblage in the 

type section of the Erda Formation is dominated by 

productoids of the genera Hystriculina and Antiquatonia and introduces the genus Chonetinella. 

This assemblage was found in two beds, in units 10 

and 11, at levels 1,092 and 1,280 feet above the base 

of the formation. Crurithyris planiconvexa (Shumard) and the small gastropod Neilsonia are numerous in the lower bed. Among the bryozoans, Ascopora sp. B and two species of Tabulipora are present in the upper bed.

Desmoinesia muricatina (Dunbar and Condra) is 

the dominant species in unit 13, where it occurs with 

Punctospirifer kentuckensis (Shumard) and Composita subtilita (Hall) in beds of gray-black calcareous shale or shaly limestone. Silicified specimens 

of D. muricatina are abundant in these dark shaly 

beds, 1,494-1,690 feet above the base of the formation. This species was found only in unit 13.

In the higher beds of the formation bryozoans are 

locally dominant, including such distinctive genera 

as Prismopora, Ichthyorachis, and Rhabdomeson. 

Prismopora cf. P. triangulata (White) is common 

in unit 19, 2,204 feet above the base of the formation. Prismopora appears in the section 2,153 feet 

above the base of the Erda and is found intermittently in the rocks above for more than 500 feet. The 

highest specimens stratigraphically occur in unit 27 

associated with the brachiopods Mesolobus and Chonetinella. Douglass has identified Fusulina sp. 

(USGS colln. f22570) in unit 24 of the type section, 

2,488 feet above the base of the formation. He also 

has recognized in unit 27 but outside of the type 

section: Fusulina and W edekindeUina! in Black 

Rock Canyon and Fusulina in Big Canyon. No recognizable fossils were found in the upper 909 feet of 

the formation in the type section.

Correlation and age. The fossils of the Erda 

Formation indicate a definite Des Moines age for 

beds 10 through 27 of the type section, from 1,017 

to 2,697 teet above its base. The question as to how 

much of the section to assign an Atoka age is a perplexing one. We are inclined to regard the beds with 

Kozlowskia aff. K. haydenensis and Neospirifer cf. 

N. coloradoensis as of probable Des Moines age. In 

the Confusion Run^e, Mexolobu* and Dexnwhiesia 

occur in a similar association with them.

Fusulinid evidence to support or to refute these 

tentative assignments is still lacking. The fact that 

the one record of Profusulinella, in the type section

of the Erda Formation is based on material that 

appears to have been reworked suggests the possibility that beds of Atoka age, once present, were 

removed by erosion. Physical evidence has not been 

found, however, for unconformity in the lower part 

of the formation.

KESSLER CANYON FORMATION

The lower part of this formation has not provided 

identifiable fossils in the type section. The only reasonably good collections of megafossils came from 

unit 10 of the type section, a 35-foot cherty limestone 

the base of which lies 675 feet above the base of the 

formation. Two collections were made from this 

unit. Although these come from the same general 

locality, they have only two species in common, 

which are marked by an asterisk (*) in th0. list 

below. The composite fauna follows (USGS collns. 

18486-PC, 18893-PC).

Relative 

ab'indancc

Rhipidomella carbonaria (Owen) _________ X

Derbyial sp. indet ___________ __- R

Neochonetes cf. N. granulifer (Owen) ____ X

Retaria sp. indet ____________ _________ R

*Kochiproductus aff. K. peruvianus (d'Orbigny) __ R 

Chaoiella sp _________-___ _ ___ R

Linoproductus sp. indet ________________ R 

Crinoid columnals ____________ _ __- C

'fOmphalotrochus wolfcampensis Yochelson ____ X 

Trilobite, gen. and sp. indet ________ __- R

The Oniphalotrochiis wolfcampensis assemblage 

in this bed was assigned an Early Permian age by 

E. L. Yochelson (in Tooker and Roberts, 1961, p. 

30). However, in the Southern and Western United 

States, many of the megafossils normally considered 

to indicate Early Permian (Wolfcamp) age put in 

an appearance in rocks of Late Pennsylvanian (Virgil) age. According to G. A. Cooper (oral commun., 

1968), typical Permian genera such as Kochiproductus, Waagenoconcha, Omphalotrochus, and Peruvispira are already present in the Upper Pennsylvanian Uddenites Zone of Texas. It is, therefore, not 

possible to determine on the basis of the usual megafauna alone whether a rock is very late Pennsylvanian or Early Permian in age. Further evidence 

must be sought among specialized groups, particularly the fusulinids. But even these are not always 

definitive.

Fusulinids occur in several beds above unit 10. All 

of them are in chert beds and all of them are poorly 

preserved. The one genus that can be recognized in 

all of these beds is Triticites. According to R. C. 

Douglass (oral commun., 1969) the species of Triti-
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A49

cites that occurs in unit 21 of the type section, 2,221 

feet above the base of the formation appears to be 

a Late Pennsylvanian form, but because of the silicification of these fossils and their occurrence in an 

organic detrital bed, reworking cannot be ruled out. 

The Triticites from unit 29, 3,027 feet above the base 

of the formation is better preserved, but is of a type 

that could be either Late Pennsylvanian or Early 

Permian in age, according to Douglass. Triticites 

from unit 37, the uppermost unit in the formation, 

is very poorly preserved and, Douglass felt, should 

not be assigned a precise age.

In summary, the recognizable fossils in the Kessler Canyon Formation type section indicate Late 

Pennsylvanian age for much of the formation and 

either a very late Pennsylvanian or Early Permian 

age for the uppermost beds. We cannot tell at present therefore, whether the Pennsylvanian-Permian 

boundary is contained within the formation or conforms to the top of it.

The age of the lower part of the formation is not 

known. As bed 10 can be no older than late Virgil in 

age, the likelihood that the lower part of the Kessler 

Canyon includes some beds of earlier Virgil age 

seems reasonable. Between the top of unit 27 of the 

Erda Formation and the base of unit 10 of the 

Kessler Canyon lies 1,584 feet of strata that have 

not yielded fossils. Whether these barren beds include rocks of Missouri age, it is not possible at 

present to say. No physical evidence of an unconformity in this part of the section has been found. 

Nevertheless, the presence of more than 5,500 feet 

of rocks containing fusulinids of Missouri age in the 

Bingham sequence and the absence of Missouri fossils in the Rogers Canyon sequence strongly suggests 

that an unconformity might be present at or near the 

base of the Kessler Canyon Formation.

PARK CITY FORMATION, GRANDEUR MEMBER

Abundant and well preserved fossils, most of them 

brachiopods, occur in the lowermost limestone unit 

of the Grandeur Member of the Park City Formation. Eight collections from unit 1 of Tooker and 

Roberts' section of the Grandeur Member have been 

studied; the fossils are listed in table 4. As all of the 

collections have come from a single unit only 30 

feet thick, we have not attempted to list them in 

stratigraphic order.

The presence of the genera Timanodictya, Penniculauris, Megousia, Liosotella, and Babylonites indicate a definite post-Wolfcamp and probable Leonard 

(Early Permian) age for this unit. G. A. Cooper 

(oral commun., 1962) who was interested in the

TABLE 4. Megafauna of the Grandeur Member of the 

Park City Formation

[Symbols explained in text]

USGS eolln. No

Bryuzoans :

Trppostomatous bryozoans.

Brachiopods :

Di/oros sp

HetFraloxia sp

Krotovia aff.K. waUacinnd (Derby).

Kochiprodiictns aff. K. pcrurianus 

(d'Orbigny )

Penniculatiri* cf. P. bnxxi I McKee ) _ 

IHctyoclostid, gen. & sp. indet ____

RJijtnrJiopora cf. R. tai/lori Girty __

ReecJieria cf. R. boriflen* (Morton)_ 

Pflecypods :

PnraUeloflon cf. P. politus Girty ___

Astnrtelln cf. A. xubqunrirnta Girty_

Gastropods :

Pleurotomariacean, gen. & sp. indet_ 

Orthonema cf. O. socorroense Girty _

Echinoderms :

Arthropods :

O 

Hi

O5 -f

00

R

X

r

R

R

X

R

X

R

R

X

X

c

R

R

X

O

c^

-t

O5 

Oi

X

X

R

R

R

R

r

R

R

X

X

u*v

**

05

OJ

R 

X

R

r

X

o

<V

Me-1

o

c

r

R

R

r

R

0

&

i "* 

£!

X

C

R

R

r

X

R

R

0

tn

**

<M

o

R

R 

R

0

O 

OH

-H 

Cl

O

p

R

R

R

0

C^

10

rH 

rH

X

R

A

R

X

A

r

R

R

X

R

c

R

R

R

R

X

X

X

CJ

PH

00 

**<

c«

r

y

i-

 v

Tf

R

R

R

R

occurrence of Liosotella in our collections, suggested 

a late Leonard to early Word (Early Permian) age 

for this limestone. He pointed out that Liosotella 

in the west Texas section is particularly characteristic of the Road Canyon Formation, the fauna 

of which has much stronger ties to that of ths 

Leonard Series than to the overlying Word fauna. 

Independently, E. L. Yochelson (oral commur,, 

1969) suggested that the gastropod Babylonites in 

this unit resembles specimens found near the Leonard-Word boundary in Texas. Yochelson (in Tooker 

and Roberts, 1961, p. 32) has previously suggested 

a late Leonard age for this Utah fauna.

The bryozoan Timanodictya is also common in 

and characteristic of the Kaibab Limestone of southwest Utah and northern Arizona. In the Confusion 

Range in extreme western Utah Timanodictya w°s
A50 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

also collected by Hose and Repenning (1959, p. 

2177) in the upper part of the Arcturus Formation. 

It is regarded as a good indicator of Leonard age.

Unconformity at the base of the Park City Formation. Although the possibility cannot be eliminated that the uppermost beds of the Kessler Canyon Formation are Early Permian (Wolfcamp) in 

age, nevertheless, typical Wolfcamp and early Leonard faunal assemblages are unknown in the Rogers 

Canyon sequence. This is in contrast to the sequence 

on South Mountain, west of the Bingham block, 

where presumed pre-Grandeur rocks totaling nearly 

6,000 feet in thickness were found by Welsh and 

James (1961, p. 4-7) to contain Early Permian 

(Wolfcamp) fusulinids, at least in their middle part.

We conclude, therefore, that an unconformity at 

the base of the Grandeur Member of the Park City 

Formation in the Rogers Canyon sequence accounts 

for most, if not all, of Wolfcamp time and part of 

Leonard time.

BINGHAM SEQUENCE

The Paleozoic rocks of the Bingham sequence include formations of Cambrian to Late Pennsylvanian age. The pre-Oquirrh rocks have been described in some detail by Gilluly (1932) and are not 

the concern of this paper. The rocks of Gilluly's 

Oquirrh Formation were not subdivided; Welsh and 

James (1961) proposed the Oquirrh Group and 

subdivided it. These subdivisions are modified in 

Tooker and Robert's part of this report, where they 

have been divided in ascending order into the West 

Canyon Limestone, Butterfield Peaks Formation, 

and the Bingham Mine Formation, the last composed of the Clipper Ridge and Markham Peak 

Members.

Thirty-seven collections of megafossils from the 

Oquirrh Group have been studied. Most of these 

came from the type and reference sections of the 

formations enumerated above. In addition, some 30 

fusulinid collections were studied by R. C. Douglass.

WEST CANYON LIMESTONE

The fauna of the West Canyon Limestone is similar to that found in the upper part of the Lake Point 

Limestone of the Rogers Canyon sequence. Fossils 

identified in seven collections from the reference 

section in West Canyon (p. A51) and four collections from the reference section in Soldier Canyon 

(p. A51) are listed in table 5. Brachiopods are by 

far the most abundant constituents of the fauna; 

bryozoans are fairly common; corals are very rare;

mollusks are limited to a few scattered pelecypods; 

and rare fragments of trilobites complete the list. 

All are typical of the Rugoclostus zone, and many of 

them are found also in the Lake Point Limestone. 

Several differences with regards to abundance are 

apparent, however. Rugoclostus is relatively rare in 

the West Canyon Limestone, while Flexaria sp. A, 

not a very common species in the Lake Point, is 

locally abundant in the West Canyon.

A small coarse-ribbed marginiferid productoid referred to Elliottella in table 5 is absent in the Lake 

Point but found locally in the lower part of the West 

Canyon; it is particularly common at a level about 

165 feet above its base. This same species occurs in 

Provo Canyon in the Wasatch Range, where it is 

abundant in the top few feet of the Manning Canyon 

Shale. The difference in the stratigraphic level of 

the peak zone of this species at the two localities is 

paralleled by the base of the Rugoclostus zone. The 

first appearance of the fossils of this zone occurs 

roughly 100 feet below the top of the Manning Canyon Shale in Soldier Canyon (Oquirrh Mountains) 

and at the base of the medial limestone of the Manning Canyon Shale in the area just south of Provo 

Canyon (Wasatch Range). These two pairs of biostratigraphic tie points indicate an eastward transgression of the base of the Oquirrh Group from the 

Oquirrh Mountains to the Wasatch Range.

Microfossils were not collected in the Wert Canyon Limestone, but Nygren (1958, p. 14) reported 

that he found the fusulinid genus Millerella present 

890 feet above the base of the formation.

The bed crowded with Linoproductus nodosus 

(Newberry), mentioned earlier in the discussion of 

the Lake Point Limestone, occurs in the Soldier 

Canyon section, 90 feet below the top of the West 

Canyon Limestone. The abundance of this species at 

this level is believed to signal a late Morrow age for 

the upper part of the formation. The top of the West 

Canyon Limestone in the Bingham sequence approximates the top of the Lake Point Limestone of the 

Rogers Canyon sequence. A Morrow age is suggested 

for the entire West Canyon Limestone.

BUTTERFIELD PEAKS FORMATION

The fauna of the Butterfield Peaks Formation 

approximates that of the Erda Formation of the 

Rogers Canyon sequence. Nine collections from the 

type section (p. A52) and 11 collections from the 

reference section (p. A52) (measured from tl N e ridge 

north of Soldier Creek to peak 9075, sees. 26, 27, 

and 34, T. 4 S., R. 4 W. Stockton quadrangle) have
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A 51

TABLE 5. Megafaiina of the West Canyon Limestone in its reference sections

in West Canyon and Soldier Canyon.

[Symbols explained in text]

Unit

TJSGS colln. No

Corals :

Bryozoans :

Echinoderms :

Brachiopods :

EUiottella sp. A

Antiquatonia aff. A. coloradoensis (Girtv) _

Linoproductus sp. A _ "

Cleiothiiridina ct. (7. orbicularis (McChesney) _ _

Pelecypods : Mi/alina"! sp. indet

Willkingia ? sp. indet

Trilobites : 

Paladin! sp. indet

West Canyon 

reference 

section

2

»

CO

1-1

U

PM

» 

»

1-1 

TH

Ol

c

IN * 

i-l

0

^

-f 

IO

TH 

TH

O}

R

X 

X

R 

R

X

R

R 

X

?

X 

X

R 

R

R

« *

iH

0

 Vo>

N

CO

o 01

R 

X

R 

X 

X 

X 

R 

X 

R

7

X 

R 

R 

X 

X

R

4

CO *

IN

O

PH

CO

»

i-l

T-t

Ol

X

R

X 

X

R

R

R 

R 

X 

X

C

c

X

R

X 

X

R

00to *

u

^t-

»

iH 

iH 

M

X

R 

R

R 

R

5

00to *

o

PM

o to to

o

IN

X 

R 

?

X

12

to iiH

T-T

o

PM

i-l

to

CO

o

IN

C

Soldier 

Canyon 

reference 

section

2

CO10

o

FM

ti 

to ITH 

TH

R 

X 

X 

X

X 

X

C

X 

X

X

c

R

4

 *

10 

CO

0

FM

00

COt-1-1 1-1

R 

R

R 

X

R 

R

7

11769-PC 513

R 

X

X

R

14

Cl

CD 

O>

O

t

O

t- liH 

iH

R

X

R 

X

R 

X 

R

R 

?

C 

X

X

R

R

been studied. The fossils from these 20 collections are 

listed in table 6.

Chaetetes was found in the type section only, 436 

feet above the base of the formation. According to 

Welsh and James (1961, p. 11), Profusidinella occurs in the Chaetetes-beaicing limestone beds, but 

whether in place or reworked, as is the case in the 

Erda Formation, is not clear. They also reported 

Fusulinella from limestone beds higher in the section. The Multithecopora zone was recognized in the 

type section at levels 940 and 1,027 feet above the 

base; in the more intensely collected reference section, corals typical of this zone occur from 525 to 

1,470 feet above the base. As in the Erda Formation, Kozlowskia aff. K. haydenensis (Girty) and 

Neospirifer cf. N. coloradoensis Stevens range 

through much of this zone.

The occurrence of Fusulina sp., recognized by R.

C. Douglass (written commun., 1962) at a level 941 

feet above the base of the reference section indicates 

a Des Moines age for this part of the section, but 

does not indicate earliest Des Moines age.

Desmoinesia muricatina (Dunbar and Condra) 

was represented only by a single example in one 

collection, 920 feet above the base of the formation 

in the reference section, where it was associated 

with Kozlowskia and Neospirifer. The absence of 

beds with abundant Desmoinesia muricatina in the 

Butterfield Peaks Formation type section is a local 

facies condition. The gray-black shale beds in which 

this species is found in profusion in the Erda Formation are also present in other sections of the 

Butterfield Peaks Formation.

Beds crowded with bryozoans occur in the upp?.r 

part of the formation. A large collection from one 

of these beds was made in the reference section,
A52 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

TABLE 6. Megafauna of the Butterfield Peaks Formation at its type and reference sections

[Symbols explained in text]

Unit

USGS colln. No _ _____

MULTITHECOPORA-KOZLOWSKIA ASSEMBLAGES

Corals :

Bryozoans :

Fenestella spp

Brachiopods :

Koelowskia aff. K. haydenensis (Girty)

Desmoinesia muricatina (Dunbar & Condra) _ _

Flexarial sp. indet _ _ _

Linoproductus sp

Trilobite :

INTERMEDIATE & PRISMOPORA ASSEMBLAGES

Corals :

Bryozoans : 

Prismopora sp

Tabulipora sp

Matheropora sp

Rhabdotneson sp

Echinoderms :

Brachiopods :

Linoproductus prattenianus (Norwood & Pratten) _____ 

Cleiothyridina sp. indet

Gomposita subtilita (Hall)

West Canyon type 

and reference sections

3

tc

M *

O

PH

Cl

M 

M 

0

X

c *e*

O

OH

M 

M 

M 

0

X

4

t- ei

CO

r-T

O

fc

O5 

Ci 

CJ

R 

X

5

OS 

1H 

CO 

iH

O

OH

CJ

o

M 

0

X

X

R

7

CI

es

10

ci

O

^

CO

0

M 

0

C

14

iH

GO 

OS

0

OH

10 

0 CO

o

R

C 

R 

R

IS

|S0306-PC 4,131 

X

X

X

R

20

10 i~ 

w *"

O

^ i~

0 

CO

o

R

X

R 

R 

R

X

26

a>iH *

>o

O

P^

00

o

08

O

R

R 

R

X

Soldier Canyon 

reference section

3

>o

M

>O

0

OH

10 

r-l

CO

O

cf.

R 

X 

X

R

R

C 

X

R

10 10 w

O

^ 

w

2?

R 

X

R

R 

X

1

X

R

4

M 

00I0

OH

ti

CO 

0

R

R

R

1 

R

R

R 

R

X 

R 

R 

R 

R

5

o

IN

A

0

OH

CO 

iH 

M 

O

C

R 

R

X 

R

R

R 

R

R

6

 * 

o e-»

0

OH

O5 

iH

CO

O

R

7

w 

« *

lH 

U

fc

o MM 

O

R 

X

10

9> 

9>

M

e*

0

OH

iH 

fl

M 

O

Cf.

11

M 

iH 

00

e*

0 

^

M 

N

M 

O 

M

R

10

or-l

M

0

fc

M

ct

M 

O 

fl

R 

R

X

R 

X

R 

R

R

R 

R

R

IS

20324-PC 3,553

X

X 

X

 >.

R 

R

R

20325-PC 3,627

r 

c

-__, r

c

F

r

r

T

Y 

T 

T

T 

Y

r

3,627 feet above the base of the formation. Characteristic genera are Prismopora, Chainodictyon, 

Ichthyorachisl, Diploporaria, Matheropora, Rhabdomeson, and Rhombocladia. These were not recorded lower in the formation. The beds containing 

these forms are correlative with the Prismoporabearing beds in the upper-middle part of the Erda 

Formation and are regarded as late Des Moines in 

age.

Fusulinid evidence for Des Moines age was encountered by R. C. Douglass (written commun.,

1962) at several levels in the type section. F^sulina 

sp. occurs in association with textulariids and Wedekindellina sp. 1,327 feet above the base of the formation (unit 4), and in association with text\ilarii.ds 

5,429 feet above the base (unit 26) ; Fusulina is 

present without associated larger Foraminfera 5,- 

449 (unit 26) and 6,081 (unit 31) feet abnve the 

base. Fusulinella sp. was identified by Douglass at 

levels 2,301 (unit 6) and 6,048 (unit 31) feet above 

the base of the type section.

Only 235 feet of beds at the top of the reference
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A53

section have not as yet provided fossil evidence as 

to the age of the rocks. We regard the beds in the 

reference section, from the first appearance of Kozloivskia aff. K. haydensis to the final appearance of 

the Prismopora assemblage, as Des Moines in age. 

For practical purposes, we include all but the lower 

few hundred feet in the Des Moines Series. The 

lower beds are Atoka in age. The Butterfield Peaks 

Formation correlates directly with the Erda Formation of the Rogers Canyon sequence.

BINGHAM MINE FORMATION

Megafossils are scarce and poorly preserved in 

the Bingham Mine Formation, except at one locality 

of uncertain stratigraphic position, where a large 

and varied fauna was found. The fossils found most 

frequently and in greatest numbers are fusulinids, 

but many of these are silicified and show signs of 

having been reworked. Despite the uncertainties 

generated by structural complication, reworking, 

and poor preservation, fairly reliable deductions 

can be made concerning the age of this formation 

and of the two members into which it has been 

divided. In the following discussion, fossils of the 

type sections of both members are considered in 

ascending order, after which the large fauna collected west of Lark is recorded.

CLIPPER RIDGE MEMBER

The fusulinids in 11 collections from the type section were studied by R. C. Douglass (written 

commun., 1962). Most of them were referable to the 

genus Triticites. Foraminifera identified by Douglass are listed in the register of Late Paleozoic fusulinid collecting localities in this report. Three collections of megafossils from the type section were studied by the writers. Two of them contained corals 

unidentifiable as to genus. The third collection is 

listed below.

Fusulinid specimens that were scattered and that 

appeared worn, were collected from unit 2 of the 

type section, 10 feet above the base of the formation; they were identified by R. C. Douglass (written 

commun., 1962) as Triticites sp. of probable Missouri age. In the same unit, 114 feet above the base 

of the formation, the following megafossils were 

recognized (USGS colln. 22486-PC).

Relative 

abundance

Stenoporid bryozoan, massive form __________ X 

Trepostomatous bryozoan, ramose form ______ R 

Fenestella sp ______________________ X 

Polypora sp ________________________ R 

Penniretepora sp _____________________ X 

Rhombocladia sp ____________________ X

Relative 

abundance

Crinoid columnals _ X 

Chonetinella sp _____ B 

Antiquatonial sp. indet __ B 

Linoproductus sp. indet _ _ B

This megafauna is not sufficiently diagnostic to 

enable one to determine the relative age of these 

beds. The age assignment must necessarily depend 

upon the fusulinids, and it is clear that as the bf.sal 

beds of the Clipper Ridge Member contain Triticites 

of a type characteristic of the Missouri Series, even 

though they appear reworked, this member can be 

no older than Missouri in age.

Triticites occurs also at levels 1,284 (unit 6), 

1,967 (unit 9), 2,379 (unit 11), 2,627 (unit 15), 

2,772 (unit 16), 2,957 (unit 18), and 2,980 (unit 

20) feet above the base of the member (and formation). Other Foraminifera found with that genus 

lopally include textulariids, Millerella sp., Bradyina 

sp., and Kansanellal sp. Although R. C. Douglass 

(written commun., 1962) pointed out that the Triticites at 2,790 and 2,957 feet above the base of the 

member are hardly distinguishable from forms of 

Virgil age, the presence of fairly well preserved 

Missouri fusulinids in the top 5 feet of the member 

(unit 20), as well as in the lower part of the overlying Markham Peak Member, indicates that the 

entire Clipper Ridge Member is of Missouri age.

Syringoporoid corals are fairly common in the 

upper part of the Clipper Ridge Member. One of 

these, from unit 18 of the type section (USGS coUn. 

23890-PC), was identified by Miss Duncan as 

Syringopora multattemiata, McChesney ?. It is not an 

entirely typical example of the Missourian form ?.nd 

may actually represent an undescribed species 

closely allied to S. multattenuata.

MARKHAM PEAK MEMBER

The fossils in the type section of the Markham 

Peak Member are sparse and poorly preserved. No 

megafossils were collected in this section. The age 

determinations are based entirely upon evidence 

provided by fusulinids, most of which are referable 

to the genus Triticites. R. C. Douglass (written 

commun., 1966) recognized Triticites at levels D40 

(unit 11), 960 (unit 11), 1,025 (unit 11), 1,566 

(unit 13), 1,603 (unit 13), 2,547 (unit 15), 3,240 

(unit 19), and 3,989 (unit 21) feet above the b^se 

of the member in its type section. The only otl^er 

Foraminifera found associated with Triticites in

is member is Climacammina, sp. in units 11 rnd 

13.

R. C. Douglass (written commun., 1966) regarded
A54 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

the fusulinids of units 11 and 13 as Missouri in age. 

Those of unit 15 are similar but appear to have 

been reworked. Three collections of fusulinids, from 

units 19 and 21 were regarded by Douglass as containing Triticites of Virgil affinities. The highest 

of these collections occurred 1,462 feet below the top 

of the uppermost bed in the type section of the 

Markham Peak Member. No fossils were found in 

these highest beds.

Fauna collected near Lark. About 1*4 miles west 

of Lark, on the north slope of Copper Gulch, a very 

fossiliferous locality has yielded a fauna of 60 species of invertebrates. Three collections (USGS collns. 

18892-PC, 20311-PC, and 21151-PC) made in 1959 

and 1962 contained the following species:

Relative 

abundance

Foraminif era:

Bradyina sp ____________________ R

Corals:

Caninoid coral, gen. and sp. indet ______ R 

Michelinial sp _________________ R 

Cladochonusl sp ______________ R

Bryozoans:

Fistuliporoid, incrusting form ________ R

Fistuliporoid, ramose form ___________ R 

Ramiporalia sp ________________ R

Stenoporoid, incrusting form ___________ R

Rhomboporella sp _______________ X

Fenestella aff. F. austini Elias and Condra 

aff. F. archimediformis Elias and Condra R 

(Cervella) aff. F. (C.) cruciformis Elias

and Condra ________________ C

(Polyporella) sp _____________ R

Polypora cf. P. andina Chronic ________ X

sp _________________________ C 

Septopora sp ___________________ R

Penniretepora sp _________________ C

Acanthocladial sp ________________ R

Ptylopora sp ____________________ R

Coeloconusl sp ___________________ X

Rhombocladia sp _________________ C

Rhomboporoid, gen. and sp. indet ______ X

Brachiopods:

Derbyia sp ___________________ X

Chonetinella cf. C. alata (Dunbar and Condra) C 

Neochonetes cf. N. granulifer (Owen) ____ R 

Krotovia sp ________________ X

Kozlowskia aff. K. splendens (Norwood and

Pratten) ______________________ C 

Ret aria sp ___________________ R

Chaoiella sp _________________ C

Kochiproductus aff. K. peruvianus

(d'Orbigny) ___________________ X

Antiquatonia sp __________________ X

Linoprodnctus sp _______________ X

CancrineUa sp ______________.___ C

Rhynchopora sp ______________________ R

Neospirifer sp. indet _______________ R 

Phricodothyris perplexa (McChesney) ____ C

Relative 

abundance

Crurithyris planiconvexa (Shumard) X 

Cleiothyridina orbicularis (McChesney) X 

Hiistedia mormoni (Marcou) A 

Punctospirifer sp _ R 

Reticulariina sp _ R

Echinoderms:

Crinoid cohimnals __ X 

Echinoid spines _ R

Worms:

Spirorbis sp __ R 

Unidentified tubes _ ____________ X

Pelecypods:

Astartellat sp. indet _ R 

Conocardium sp. indet ____ ________ R

Gastropods:

Euphemites sp. indet ____ _ R 

Knightites (Retispira) sp. indet _ X 

Sinuatinal sp. indet -- R 

Baylea sp _ _ X 

Peruvispirat sp. indet _ - R 

Pleurotomariacean, gen. and sp. indet - R 

"Strophostylus" sp _ _- - X 

Naticopsis (Naticopsis) sp _- X 

(new subgenus) sp. indet R 

Meekospira sp ___ _ - R 

Omphalotrochus wolfcampensis Yochelson X 

Omphalotrochust cf. O. obtusispira (Shumard) R

Trilobites:

Ditomopyge sp ___ _ - X

The presence of such genera as Kochiproductus, 

Chaoiella, Pemvispirat, and Omphalotrochus suggest a late Virgil or early Wolfcamp age for this 

assemblage. The brachiopod fauna is very similar to 

that of the Omphalotrochus wolfcampensis-besucmg 

beds in the lower part of the Kessler Canyon Formation at the north end of the range. In the Kessler 

Canyon, fusulinid evidence indicates a late Virgil 

(or slightly younger) age for these beds. Similar 

fusulinids are found in the Markham Peak Member 

of the Bingham Mine Formation. The rocks west of 

Lark containing the Omphalotrochus wolfcampensis 

assemblage are assigned, therefore, to the Markham 

Peak Member despite the fact that this faunal 

assemblage was not recognized in the type section 

of that member.

Complicating this problem is the geograpHc position of this fossil locality in an area mapped as 

Clipper Ridge Member by Tooker and Roberts, at a 

point approximately where the Commercial limestone might be expected to crop out (E. W. Tooker, 

oral commun., 1969). We conclude that the fcssiliferous beds are part of an infaulted block of the Markham Peak Member not recognized as such in the 

field. Unfortunately, before this conclusion could be 

tested by further mapping in that area, tN fossil 

locality was engulfed by southward extension of the
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A55

waste piles from the Bingham open pit mine and 

buried beneath tons of loose rock.

CORRELATION AND AGE OF THE BINGHAM MINE FORMATION

The evidence recorded in the preceding discussion 

suggests that roughly the lower half of the Bingham 

Mine Formation, including the Clipper Ridge Member and the beds up to the middle of unit 13 of the 

type section of the Markham Peak Member, is equivalent to the Upper Pennsylvanian Missouri Series. 

The aggregate thickness of these beds is 4,590 feet. 

Missouri fusulinids 5,532 feet above the base of the 

formation are reworked and whether they are actually in beds of Missouri or Virgil age is a matter for 

conjecture.

Fusulinids of Virgil age occur in place 6,225 to 

6,975 feet above the base of the formation in the 

Markham Peak Member. It is to this part of the 

formation that the large Omphalotrochus wolfcampensis fauna collected west of Lark should be assigned. Our reasoning is based upon the relationship 

of the similar though less abundant fauna near the 

base of the Kessler Canyon Formation in the Rogers 

Canyon sequence and the fusulinids contained in 

that same formation.

No fossils of Permian age have been recognized 

in the Bingham Mine Formation. The type section 

for this formation was originally designated by 

Welsh and James (1961, p. 9) as occupying part of 

the main ridge of South Mountain, which borders 

the south edge of Tooele Valley at the western base 

of the Oquirrh Mountains. According to E. W. 

Tooker (oral commun., 1969) the rocks that make 

up South Mountain are part of a thrust sheet that 

is separate from the Bingham sequence. Welsh and 

James regarded the formation as restricted to beds 

of Late Pennsylvanian age. Even though the 1,462 

feet of unfossiliferous beds in the upper part of this 

formation in the Bingham sequence makes it impossible to say unequivocally that no Permian beds are 

present in it in the Oquirrh Mountains, it would 

seem reasonable to maintain Welsh and James' age 

assignment of the Bingham Mine Formation here 

as Late Pennsylvanian throughout unless evidence 

to the contrary becomes available.

The correlation of the lower part of the Bingham 

Mine Formation with the section in the Rogers 

Canyon sequence remains an enigma. Although 

more than 5,500 feet of this formation contains 

fusulinids of Missouri age, in the Rogers Canyon 

sequence no Missouri fossils have been recognized.

Beds of Missouri through Wolfcamp age, equivalent to the Bingham Mine Formation are known in

the Oquirrh Formation of the Timpanogos sequence 

in the central Wasateh Mountains (Baker, 1947), 

in the central facies of the same formation in the 

Gold Hill region south of Wendover, Utah (Nolan, 

1935, p. 35-39; L. C. Henbest, written commun. to 

R. Hose, 1957), in the Ferguson Springs Formation 

of Steele (1960, p. 101) at Ferguson Springs Mountain, Elko County, Nev., and at Spruce Mountain, 

farther west in the same county (R. C. Douglass, 

oral commun., 1969). A belt of such rocks extends 

through the southeastern and southern parts of tN 

Great Basin, particularly in Lincoln and Clark 

Counties, Nev. Sections of these Late Pennsylvania n 

and Early Permian rocks, within the Bird Sprir*? 

Formation, have been documented in the Arrow 

Canyon Range (Langenheim and Langenheim, 196E) 

and on Spring Mountain near Las Vegas (Rich, 

1961).

Over much of the central part of the Great Basin 

a hiatus, equivalent to all or part of the Bingham 

Mine Formation, is present. This hiatus has previously been delineated by Steele (1961, chart 1) 

who referred to it as the "Regional Middle Pennsylvanian unconformity." In some places the rocks 

below the unconformity are as old as Meramec 

(early Late Mississippian) in age and the rocks 

above it as young as middle Wolfcamp (Early Permian) in age. In figure 13, some of the sections in 

which this hiatus is well developed are shown.

In the Confusion Range this hiatus is marked by 

an unconformity within the Ely Limestone, between 

the Pennsylvanian and Permian parts of the formation (Hose and Repenning, 1959, p. 2174). Hose's 

mapping in this region and stratigraphic studies by 

Gordon have shown that over a considerable area 

carbonate rocks of Early Permian (Wolfcamp) age 

rest on carbonate and fine clastic rocks of Middle 

Pennsylvanian (Des Moines) age. The same urconformity has been recognized in the southern part 

of the Schell Creek Range in White Pine County, 

Nev., by Drewes (1967). It extends also into the 

Ely mining district where the name "Ely Limestone" 

has been restricted to beds of Pennsylvanian age. 

The overlying Lower Permian limestone has been 

given the name Riepe Spring Limestone (Steele, 

1960, p. 93, 102).

In the Eureka mining district, Nev., Early Permian (Wolfcamp) rocks above this unconformit" 

are referred to the Carbon Ridge Formation (Nolan 

and others, 1956, p. 62-64). Supposed Missouri 

fusulinids reported from the Carbon Ridge occur, 

according to Douglass (oral commun., 1970), with 

Wolfcamp species. The youngest rocks of the Ely
A56 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

LU 

CO

CC.

HSYLVANIAN

z

Q_

MISSISSIPPI

CO 

LLJ 

CC. 

LLJ

to

s

o

1

^

£

~"

=>

PROVINCIAL 

SERIES

WOLFCAMP

is 

cc.

^3 

O

~E

to

LLJ 

O

£3Q

 a:

 a:

0

to

LLJ 3;

1

TIMPANOGOS 

SEQUENCE 

WASATCH MTS

UTAH

o

I

o 

O

Manning 

Canyon 

Shale

2

BINGHAM 

SEQUENCE 

OQUIRRH MTS

UTAH

o

0

Bingham 

Mine

Formation

E

OE

|

O

Butterfield

Peaks

Formation

West

Canyon

Limestone

Manning 

Canyon 

Shale

3 

ROGERS 

CANYON 

SEQUENCE 

OQUIRRH MTS

UTAH

o

 5

O

Oquirrh Group

 ?

Kessler 

Canyon

Formation

Erda

Formation

Lake 

Point

Limestone

4

CONFUSION 

RANGE,

UTAH

Upper part 

of 

Ely Limestone

Lower part 

of 

Ely Limestone

Chainman 

Shale

5

SCHELL CREEK 

RANGE,

NEVADA

Upper part 

of 

Ely Limestone

Lower part 

of 

Ely Limestone

Chainman 

Shale

6

EGAN RANGE, 

ELY 

MINING 

DISTRICT

NEVADA

Riepe Spring 

Limestone

Ely 

Limestone

Chainman 

Shale

7

EUREKA 

MINING 

DISTRICT

NEVADA

Carbon Ridge 

Formation

\

Ely

Limeston

Diamond 

Peak 

Formation i

8

CARLIN 

REGION

NEVADA

Strathearn 

Formation 

of Dott

,

(1955)

/

Ely 

I Limestone

______

Diamond 

Peak 

Formation

9

ANTLER 

PEAK 

AREA

N:VADA

AnthrPeak 

Limestone

i

Battle

Conglomerate

FIGURE 13. Correlation chart of sections in the central Great Basin.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH / 57

r- -- -- - r - i

1 8.nElk° 3 DSalt Lake City '

I Q *

1 » y o»

i .1

Eureka Q _ 

NEVADA " 6^E'y -4 UTAH 5

\ 

\ 

\

\

\ I

\ 1 SOURCES 

\ 1. A. A. Baker (1947) 

\ r~xJ< 2. This paper 

\> 3. This paper 

i 4. R. K. Hose and 

\\ C. A. Repenning(1959) 

v 5. Harold Drewes (1967) 

6. Grant Steele (1960) 

7. T. B. Nolan, C. W. Merriam, 

and J. S. Williams (1956) 

8. R. H. Dott, Jr. (1955) 

9. R. J. Roberts (1964)

FIGURE 13. Continued 

mestone beneath the unconformity are Middle

shown on the correlation chart (fig. 1) is in excess 

of 7,000 square miles, but eventually we may f nd

that it occupied a much greater part of the Gr?at 

Basin region.

REGISTER OF LATE PALEOZOIC MEGAFAUNA 

COLLECTING LOCALITIES IN THE 

OQUIRRH MOUNTAINS, UTAH

U8QS CoUn. 

No. Descriptions and collectors

16318-PC Garfield 7% -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On ridge southwest of 6231 peak, in the 

NEUNW%NW% sec. 6, T. 2 S., R. 3 W., 

at approximately 5,500 ft elevation. Lake 

Point Limestone. Prominent 5-ft colonial coral 

bed, unit 4 of type section, 583 ft above base 

of formation. Collected by R. J. Roberts, 1?56.

16319- PC Garfield 7% -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same general locality as 16318-PC. Lake 

Point Limestone. Collected from dark-g~ay 

medium-bedded limestone about 34 ft ab^ve 

base of unit 5 of type section, 622 ft abrve 

base of formation. Collected by R. J. Roberts, 

1956.

Pennsylvanian (Atoka) in age. Locally, as at Conical 

Hill near Eureka, the Carbon Ridge Formation rests 

on rocks of late Meramec age of the Diamond Peak 

Formation.

In the Carlin region the same unconformity is 

present between the top of the Ely (Tomera Formation of Dott (1955) and the base of the Strathearn 

Formation of Dott (1955). The basal part of the Strathearn contains f usulinid-bearing beds of Late Pennsylvanian (Virgil) age. Locally, as in Carlin Canyon, the Strathearn rests on Diamond Peak beds of 

early Meramec age. At the last two localities, which 

lie along the Antler erogenic belt, uplift is indicated at an earlier time than in the region to the 

east.

In the Antler Peak area, near Battle Mountain, 

Nev., a similar unconformity occurs at the contact 

of the Battle Conglomerate, of Middle Pennsylvanian 

(Atoka) age, and the overlying Antler Peak Limestone of Late Pennsylvanian (Virgil) and Early 

Permian (Wolfcamp) age (Roberts, 1964). Like the 

Strathearn Formation, the Antler Peak includes 

fusulinid-bearing beds of late Virgil age in its lower 

part.

Not enough data are available to delimit the area 

covered by this unconformity. Subsequent tectonic 

events have combined to alter its original area 

somewhat. Rigid faunal control will be necessary to 

recognize its margins in places where its magnitude 

has dwindled. Its extent, measured by the sections

16322-PC Garfield 7%-minute quadrangle, Tooele Courty. 

Green Ravine-Rogers Canyon measured rection. Same general locality as 16318-PC. Lake 

Point Limestone. Collected in dark-gray limestone, 40 ft above base of unit 5 of type faction, 628 ft above base of formation. Collected 

by R. J. Roberts, 1956.

16323-PC Garfield 7%-minute quadrangle, Tooele Courty. 

Green Ravine-Rogers Canyon measured section. On ridge southwest of 6231 peak at approximately 5,700 ft elevation, in the 

NE^NW1^ sec. 6, T. 2 S., R. 3 W. Lake 

Point Limestone. Collected from dark-g^ay 

cherty limestone, 150 ft above base of unit 5 

of type section, 738 ft above base of formation. 

Collected by R. J. Roberts and E. W. Tool-er, 

1956.

16324-PC Garfield 1% -minute quadrangle, Tooele Courty. 

Green Ravine-Rogers Canyon measured section. Same general locality as 16323-PC, at 

approximately 5,800 ft elevation. Lake Pcfnt 

Limestone. Collected from cherty dark-g~ay 

limestone, 113 ft above base of unit 7 of t;npe 

section, 866 ft above base of formation. Collected by R. J. Roberts and E. W. TooHr, 

1956.

16325-PC Garfield 7 1A-minute quadrangle, Tooele Courty. 

Green Ravine-Rogers Canyon measured section. On ridge in center of sec. 31, T. 1 S., R. 

3 W. Erda Formation. From dark-gray calcareous shale probably at about same level as 

16326-PC. Collected by R. J. Roberts, It 56.

16326-PC Garfield 7%-minute quadrangle, Tooele Courty. 

Green Ravine-Rogers Canyon measured sec-
A58 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

CoUn. 

No.

16327-PC

16328-PC

16329-PC

16330-PC

16331-PC

16332-PC

Descriptions and collectors

tion. On ridge on north side of Rogers Canyon, slightly north of center of sec. 31, T. 1 

S., R. 3 W., at elevation of approximately 

6,200 ft. Erda Formation. Collected from 

dark-gray cherty limestone, 104 ft above base 

of unit 13 of type section, 1,494 ft above 

base of formation. Collected by R. J. Roberts 

and E. W. Tooker, 1956.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured sec. 

tion. Same general locality as 16326-PC, from 

about 6,300 ft in elevation. Erda Formation. 

Collected in dark-gray cherty limestone, 10 

ft above base of unit 14 of type section, 1,703 

ft above base of formation. Collected by R. J. 

Roberts and E. W. Tooker, 1956.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. North side of Rogers Canyon in north 

center sec. 31, T. 1 S., R. 3 W., at elevation 

of approximately 6,600 ft. Erda Formation. 

Collected from 4-ft light-gray crinoidal limestone, unit 25 of type section, 2,515 ft above 

base of formation. Collected by R. J. Roberts 

and E. W. Tooker, 1956.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On ridge south of Green Ravine below 

tramway tower, approximately on 5,400-ft 

contour, in the NW^SW^ sec. 6, T. 2 S., 

R. 3 W. Green Ravine Formation. Collected in 

interbedded dark-gray limestone and bioclastic 

limestone, 189 ft above base of unit 11 of type 

section, 1,060 ft above base of formation. 

Collected by E. W. Tooker and R. J. Roberts, 

1956.

Garfield 7^-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality as 16329-PC. Green Ravine 

Formation. Collected in limestone, 203 ft 

above base of unit 11 of type section, 1,074 ft 

above base of formation. Collected by E. W. 

Tooker and R. J. Roberts, 1956.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality as 16329-PC, at 5,475 ft 

elevation. Green Ravine Formation. Collected 

in interbedded limestone and argillaceous 

limestone, 258 ft above base of unit 11 at type 

section, 1,129 ft above base of formation. 

Collected by E. W. Tooker and R. J. Roberts, 

1956.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. At 5,300 ft elevation on north side of 

Green Ravine, one-eighth mile east of 5244

USGS CoUn. 

No.

16333-PC

16334-PC

16335-PC

16337-PC

17031-PC

17143-PC

Descriptions and collectors

hill, in SW^NWH sec. 6, T. 2 S., R 3 W. 

Green Ravine Formation. Collected in interbedded limestone, cherty limestone, and arenaceous limestone, 158 ft above base of unit 

11 of type section, 1,029 ft above base of 

formation. Collected by R. J. Roberts and 

E. W. Tooker, 1956.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measrred section. Same general locality as 16332-PC. 

Green Ravine Formation. Collected across a 

60-ft section of dark-gray limestone and 

argillaceous limestone beginning 97 ft above 

base of unit 12 of type section and 1,299 ft 

above base of formation. Collected by R. J. 

Roberts and E. W. Tooker, 1956.

Garfield 7%-minute quadrangle, Tooele County. 

At about 6,000 ft elevation in tributary of 

Big Canyon (just north of word "Big" on 

topo sheet) in NE^NE^NW^ se-. 7, T. 

2 S., R. 3 W. Erda Formation. Collected from 

dark-gray fossiliferous limestone near base of 

unit 1. Collected by R. J. Roberts an<l E. W. 

Tooker, 1956.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On ridge south of Green Ravine north 

of tramway tower at approximate elevation 

of 5,300 ft above sea level, in NW^iSW^i 

sec. 6, T. 2 S., R. 3 W. Green Ravine Formation. Collected from interbedded banded 

cherty limestone and arenaceous 1 4 oclastic 

limestone, at base of unit 10 of type section, 

799 ft above base of formation. Collected by 

E. W. Tooker and R. J. Roberts, 1956.

Garfield 7%-minute quadrangle, Tooele County. 

At 5,480 ft elevation on north side of Big 

Canyon, in NW^NW^ sec. 7, T. 2 S., R. 

3 W. Lake Point Limestone. Collected from 

fossiliferous argillaceous limestone in upper 

part of formation. Collected by R. J. Roberts, 

1956.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measrred section. Same general locality as 17145-PC but 

from crinoidal limestone bed about 30 ft 

higher stratigraphiqally. Lake Poirt Limestone. Collected by M. Gordon, Jr., R. J. 

Roberts, and E. W. Tooker, July 8, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measrred section. Below 5,400-ft contour, a few feet up north 

slope from bottom of Green Ravine, about 

one-eighth mile east of 5244 hill in the 

SE%SW%NW% sec. 6, T. 2 S., R. 3 W. 

Green Ravine Formation. Collected from in-
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A59

U8G8 GoUn.

No.

17144-PC

17145-PC

17146-PC

17147-PC

17148-PC

17149-PC

17150-PC

Descriptions and collectors

terbedded limestone and argillaceous limestone, 258 ft above base of unit 11 of type 

section, 1,129 ft above base of formation. 

Collected by M. Gordon, Jr., and R. J. Roberts, 

July 8,1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same general locality as 17143-PC. 

Green Ravine Formation. Collected from 

impure gray limestone, a few feet below 

16333-PC, approximately 1,290 ft above base 

of formation. Collected by M. Gordon, Jr., and 

R. J. Roberts, July 8, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. At cairn on lower slopes of ridge southwest of 6231 peak, a few tens of feet north 

of unnamed ravine north of Green Ravine, 

near center of NW*4 sec. 6, T. 2 S., R. 3 

W. Lake Point Limestone. Collected from 

medium-dark-gray limestone with shale partings, 143 ft above base of unit 1 of type 

section. Collected by M. Gordon, Jr., R. J. 

Roberts, and E. W. Tooker, July 8, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality and bed as 16318-PC. 

Collected by M. Gordon, Jr., R. J. Roberts, 

and E. W. Tooker, July 8, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Same general locality as 16318-PC. Lake 

Point Limestone. Collected from dark-gray 

limestone and argillaceous limestone, 55 ft 

above base of unit 5 of type section and 643 

ft above base of formation. Collected by M. 

Gordon, Jr., R. J. Roberts, and E. W. Tooker, 

July 8,1957.

Garfield 7 1/&-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same general locality as 16318-PC but 

higher on ridge. Lake Point Limestone. Collected from medium-dark-gray limestone, 

about 20 ft above base of unit 7 of type section, 773 ft above base of formation. Collected by M. Gordon, Jr., R. J. Roberts, and 

E. W. Tooker, July 8, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same general locality as 16318-PC at 

elevation of 5,690 ft above sea level. Lake 

Point Limestone. Collected in limestone, about 

117 ft above base of unit 7 of type section, 

870 ft above base of formation. Collected by 

M. Gordon, Jr., R. J. Roberts, and E. W. 

Tooker, July 8, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured secUSGS CoUn. 

No.

17151-PC

17152-PC

17153-PC

17154-PC

17155-PC

17156-PC

Descriptions and collectors

tion. On ridge southwest of 6231 peal- at 

about 5,725 ft elevation, in the NE%N"V% 

sec. 6, T. 2 S., R. 3 W. Lake Point Limestone. 

Collected from limestone bed just below 4-ft 

yellow quartzite, 155 ft above base of urit 7 

of type section, 908 ft above base of formation. Collected by M. Gordon, Jr., R, J. 

Roberts, E. W. Tooker, July 8, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. About 700 ft southwest of summit of 

6231 peak on ridge in SW^SEiiSW1^ sec. 

31, T. 1 S., R. 3 W., at elevation of 5,79 r ft 

above sea level. Erda Formation. Collected 

from light-gray limestone, 157 ft above base 

of unit 1 of type section. Collected by M. 

Gordon, Jr., R. J. Roberts, and E. W. Tooker, 

July 9,1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On north side of Rogers Canyon about 

75 ft above canyon bottom, at elevatior of 

about 5,500 ft above sea level, in the 

NE%SWH sec. 31, T. 1 S., R. 3 W. F-da 

Formation. Collected from fossiliferous gray 

limestone, 182 ft above base of unit 1 in type 

section. Collected by M. Gordon, Jr., R. J. 

Roberts, and E. W. Tooker, July 9, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality as 17152-PC. Frda 

Formation. Collected from limestone a few 

feet above 17152-PC. Collected by M. Gordon, 

Jr. and E. W. Tooker, July 9, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same general locality at 17152-PC. 

Erda Formation. Collected from light-pray 

limestone, 6 ft thick, below crossbedded calcareous sandstone or sandy limestone, 12r ft 

above base of unit 3 of type section, 52? ft 

above base of formation. Collected by M. 

Gordon, Jr., R. J. Roberts, and E. W. Tooker, 

July 9,1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same general locality as 17152-PC but 

at elevation of roughly 5,700 ft. Erda Formation. Collected in light-gray limestone, 10-12 

feet thick, underlying calcareous sandstone, 

72 ft above base of unit 4 of type section, 604 

ft above base of formation. Collected by M. 

Gordon, Jr., and R. J. Roberts, July 9, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality as 17155-PC, but from 

base of 6-ft light-gray limestone separated
AGO GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

rSGS CoUn,

No. Descriptions and collectors

by 4 ft of calcareous sandstone from limestone of 17155-PC. Overlain by 15 ft of yellowish chert. Collected by R. J. Roberts and 

E. W. Tooker, July 9,1957.

17157-PC Garfield 7^-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same ridge as 17155-PC but roughly 

50 ft higher. Erda Formation. Bryozoans and 

Linnproductus from 5-ft yellow chert bed; 

Spirifer and Composita and corals from overlying dark-gray limestone and shale; 30 ft 

above base of unit 6 of type section, 752 ft 

above base of formation. Collected by M. 

Gordon, Jr., and R. J. Roberts, July 9, 1957.

17158-PC Garfield 7 % -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. North slope of Rogers Canyon in 

NE^NE^SW1^ sec. 31, T. 1 S., R. 3 W. 

Erda Formation. Collected from dark-gray 

argillaceous limestone, at base of unit 8 of 

type section, 921 ft above base of formation. 

Collected by M. Gordon, Jr., R. J. Roberts, 

E. W. Tooker, July 10, 1957.

17159-PC Garfield 7 %-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. North slope of Rogers Canyon in 

SW%SW^NE% sec. 31, T. 1 S., R. 3 W. 

Erda Formation. Collected from gray impure 

limestone with chert, 30 ft above base of unit 

10 of type section, 1,097 ft base of formation. 

Collected by M. Gordon, Jr., R. J. Roberts, 

and E. W. Tooker, July 10, 1957.

17161-PC Garfield 7 V2 -minute quadrangle, Tooele County. 

Same locality as 17159-PC but from bed 

about 30 ft higher stratigraphically. Collected 

by R. J. Roberts, July 10, 1957.

17163-PC Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Near middle sec. 31, T. 1 S., R. 3 W. 

Erda Formation. Collected from gray cherty 

limestone, 74 ft above base of unit 11 of type 

section, 1,280 ft above base of formation. 

Collected by M. Gordon, Jr., R. J. Roberts, 

and E. W. Tooker, July 10, 1957.

17164-PC Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same general locality as 17163-PC in 

saddle on ridge. Erda Formation. Collected 

from two 1-ft beds separated by 10 ft of 

dark-gray impure limestone, beginning 297 ft 

above base of unit 13 of type section, 1,687 

ft above base of formation. Collected by M. 

Gordon, Jr., R. J. Roberts, and E. W. Tooker, 

July 10,1957.

17165-PC Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Higher on same ridge. Erda Formation. 

Collected from medium-gray cherty limestone, 

16 ft above base of unit 19 of type section,

USGS CoUn. 

No.

17166-PC

17167-PC

17168-PC

17169-PC

17170-PC

18486-PC

Descriptions and collectors

2,153 ft above base of formation. Collected 

by M. Gordon, Jr., R. J. Roberts, and E. W. 

Tooker, July 10,1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On flatter part of ridge at elevr.tion of 

approximately 5,475 ft, on line between 

SE^SE^NW1^ and SW^SE^NE^ sec. 31, 

T. 1 S., R. 3 W. Erda Formation. Collected 

from medium-gray thin-bedded to plat7 argillaceous limestone, 67 ft above base of unit 19 

of type section, 2,204 ft above base of formation. Collected by M. Gordon, Jr., R. J. Poberts, 

and E. W. Tooker, July 10, 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section. Or north 

slope of canyon roughly 75 ft in elevation 

above stream, approximately in certer of 

south line of SE%NE% sec. 34, T. 4 S., 

R. 4 W. West Canyon Limestone. Collected 

from argillaceous limestone, 12-30 feet 

above base of unit 2 of reference section, 

53 ft above base of formation. Collected by M. 

Gordon, Jr., R. J. Roberts, and E. W. Tooker, 

July 11, 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section. Sarre general locality as 17167-PC but higher on ridge 

in SE^iNEH sec. 34, T. 4 S., R. 4 W. 

West Canyon Limestone. Collected from darkgray argillaceous limestone, 2-7 ft above base 

of unit 4 of reference section, 354 f", above 

base of formation. Collected by M. Gordon, 

Jr., R. J. Roberts, and E. W. Tooker, July 11, 

1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section. Sarre general locality as last but higher on slop?. West 

Canyon Limestone. Collected from grray to 

brownish-gray arenaceous and argillaceous 

limestone about 15 ft above base of unit 7 

of reference section, 513 ft above base of 

formation. Collected by M. Gordon, Jr., R. J. 

Roberts, and E. W. Tooker, July 11, 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section. Upslope 

from 17169-PC in the SE%NE% sec. 34, 

T. 4 S., R. 4 W. West Canyon Limestone. 

Collected from light-gray cherty argillaceous 

limestone, 30-41 ft above base of unit 14 of 

reference section, 962 ft above base of formation. Collected by M. Gordon, Jr., R. J. Roberts, and E. W. Tooker, July 11, 1957.

Garfield 7^-minute quadrangle, Tooele County. 

Black Rock Canyon measured section. Slope 

on west side of Black Rock Canyon at elevation of 5,700 ft in middle part of NE% sec. 

30, T. 1 S., R. 3 W. Kessler Canyon Formation. Collected from fossiliferous light-brown-
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A61

.S' Colln. 

No.

18490-PC

18892-PC

18893-PC

19948-PC

19949-PC

20232-PC

20235-PC

Descriptions and collectors

ish-gray cherty limestone, unit 10 of type section, 675 ft above base of formation. Collected 

by R. J. Roberts and E. W. Tooker, 1958.

Garfield 7%-minute quadrangle, Salt Lake Co. 

At 6,280 ft elevation on ridge, about 0.3 mile 

northeast of summit of hill 7037, on east 

slope of Oquirrh Mountains, in the NW}4- 

SEHNEH sec. 3, T. 2 S., R. 3 W. Grandeur 

Member of Park City Formation. Collected by 

R. J. Roberts, 1958.

Lark 7 Vz minute quadrangle, Salt Lake County. 

Copper Gulch, west of Lark, near old Dalton 

and Lark mine, along west edge of SE^SE 1/^ 

sec. 25, T. 3 S., R. 3 W., by powerline just 

north of road at west edge of Lark quadrangle. Bingham Mine Formation, uncertain 

stratigraphic position. Collected by E. L. 

Yochelson, R. J. Roberts, and E. W. Tooker, 

July 4, 1959.

Garfield 7%-minute quadrangle, Tooele County. 

Black Rock Canyon measured section. Same 

locality and stratigraphic unit as 18486-PC. 

Collected by E. L. Yochelson, R. J. Roberts, 

and E. W. Tooker, July 4, 1959.

Magna 7%-minute quadrangle, Salt Lake County. 

On slope west of town of Magna (west of 

word "Mining" on topo sheet) in NW^SW1^ 

sec. 30, T. 1 S., R. 2 W. Grandeur Member of 

Park City Formation. Same unit as 19949-PC 

but 7.5 ft higher stratigraphically in an overlying bed. Collected by R. J. Roberts, 1961.

I»Iagna 7%-minute quadrangle, Salt Lake County. 

West of town of Magna in SW^NW 1/! sec. 30, 

T. 1 S., R. 2 W., on Provo Bench (at about 

4,800-ft contour) just north of small draw 

that lies at intersection of powerline and 

section line. Grandeur Member of Park City 

Formation, basal limestone bed. Collected by 

R. J. Roberts, 1961.

Garfield 7 }&-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. At nose on ridge just above 6.850 ft elevation in SW%NW%NE%, sec. 31, T. 1 S., 

R. 3 W. above prominent cliff of dark-gray 

cherty limestone with medial band of lightgray crinoidal limestone. Erda Formation. 

Collected from dark-gray cherty limestone, 

149 ft above base of unit 27 of type section, 

2,686 ft above base of formation. Collected by 

E. W. Tooker and R. J. Roberts, 1957. Fusulinids, f22568, from same unit 1 mile eastnortheast of type section.

Garfield 7%-minute quadrangle, Tooele County. 

Black Rock Canyon, bed and east slope of 

middle fork, in the NWHNE%NE% sec. 32, 

T. 1 S., R. 3 W., between 6,200- and 6,240- 

foot contours. Erda Formation. Collected from 

same gray cherty limestone as in 20232-PC

U8G8 Colln.

No. Descriptions and collectors

from unit 27 of type section, 1 mile to vestsouthwest. Collected by E. W. Tooker, 1957.

20236-PC Garfield 7^-minute quadrangle, Tooele Cornty. 

On south slope of Big Canyon at 6,840-ft 

contour, 1,300 ft west of tramway tower 

marked 7417 on topo sheet, in the NE&NW^i 

sec. 7, T. 2 S., R. 3 W. Erda Formation. Random collection from upper 50 ft of same ch°.rty 

limestone that is unit 27 in type section, about 

2 miles to north. Collected by E. W. Tooker, 

1957. Fusulinids, f22569, from unit 1% miles 

south of type section.

20238-PC Garfield 7%-minute quadrangle, Salt Lake 

County. East slope of hill 5561 capped1 by 

flagpole north of Little Valley. Outcrops 1,300 

ft southeast of flagpole and 500 ft northeast 

from check spot elevation 5,166 at 5,240-ft 

contour, in the SE^NW 1! sec. 25, T. ] S., 

R. 3 W., 1 mile southeast of copper mill at 

Arthur. Grandeur Member of Park City Formation. Collected from fossiliferous sv aly 

limestone in basal limestone units. Collected 

by E. W. Tooker, 1957.

20240-PC Garfield 7%-minute quadrangle, Salt Lake 

County. Coon Canyon, 400 ft due east of 

junction of Right Hand and Left Hand Forks 

of Coon Creek, 150 ft north of road at or near 

base of hill approximately at 5,800-ft contour, in the NWHNW1^ sec. 14, T. 2 S., 

R. 3 W. Grandeur Member of Park City Formation. Collected from fossiliferous mediumto thin-bedded limestone in upper part of unit 

1 of measured section. Collected by E. W. 

Tooker, 1957.

20241-PC Garfield 7 V2 -minute quadrangle, Salt Lake 

County. In Porter Hollow in the SE^SW 1^ 

sec. 11, T. 2 S., R. 3 W., near 20240-PC but 

along strike north of Coon Creek; outcrops 

100 ft above stream. Grandeur Member of 

Park City Formation, unit 1. Collected by 

E. W. Tooker, 1957.

20242-PC Garfield 7 ^-minute quadrangle, Salt Lake 

County. In Porter Hollow in vicinity of 

20241-PC but farther along strike north of 

Coon Creek, in SE%SW% sec. 11, T. ?, S., 

R. 3 W. Grandeur Member of Park City Formation, unit 1. Collected by E. W. Tooker, 

September 18, 1957.

20243-PC Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On lower western slope of Oquirrh 

Mountains, south of tramway in NE^iTE^ 

sec. 1, T. 2 S., R. 4 W., almost on qurrter 

section line. Green Ravine Formation. Collected from light-olive-gray calcareous ?andstone, 3 ft thick, 26 ft above base of unit 6 

of type section, 92 ft above base of formation. 

Collected by H. M. Duncan, E. W. Tooker, 

and R. A. Lewandowski, July 20, 1961.
A62 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

rKGS CoUn.

No. Descriptions and collectors

20246-PC Garfield 7 V2 -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. About 200 ft along strike from 20243- 

PC and including limestone ledges higher in 

section. Green Ravine Formation. Collected 

from same sandstone as 20243-PC and from 

higher limestone beds, 26-45 ft above base of 

unit 6 of type section, 92 ft above base of 

formation. Collected by H. M. Duncan, E. W. 

Tooker, and R. A. Lewandowski, July 20, 1961.

20247-PC Garfield 7 V2 -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same general locality as 20246-PC at 

4,960-ft contour. Green Ravine Formation. 

Collected from limestone about 10 ft higher 

stratigraphically than 20246-PC. Collected by 

H. M. Duncan, E. W. Tooker, and R. A. 

Lewandowski, July 20, 1961.

20248-PC Garfield 7 V2 -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Northern part of SW^SW 1^ sec. 6, 

T. 2 S., R. 3 W., at 5,320-ft contour. Green 

Ravine Formation. Collected in limestone of 

unit 11, about 20 ft above locality 20249-PC. 

Collected by H. M. Duncan, E. W. Tooker, and 

R. A. Lewandowski, July 20, 1961.

20249-PC Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine measured section, on north edge 

of SWHSWH sec. 6, T. 2 S., R. 3 W., approximately at 5400-ft contour. Green Ravine 

Formation. Collected from interbedded limestone, cherty limestone, and arenaceous limestone, 168 ft above base of unit 11 of type section, 1,039 ft above base of formation. Collected 

by M. Gordon, Jr., H. M. Duncan, E. W. 

Tooker, and R. A. Lewandowski, July 20, 1962.

20250-PC Garfield 7%-minute quadrangle, Tooele County. 

South of tramway in NW^SW^SW^ sec. 

6, T. 2 S., R. 3 W., at 5,480-ft contour. Green 

Ravine Formation. Collected in limestone of 

unit 11, one-half mile southeast of type section, about 100 ft above locality 20249-PC. 

Collected by H. M. Duncan, E. W. Tooker, and 

R. A. Lewandowski, July 20, 1961.

20251-PC Garfield 7 Ms-minute quadrangle, Tooele County. 

Same locality as 20250-PC but from about 5 ft 

higher in section. Collected by H. M. Duncan, 

E. W. Tooker, and R. A. Lewandowski, July 

20, 1961.

20252-PC Garfield 7 Vz -minute quadrangle, Tooele County. 

Random collection from limestone beds in unit 

11 between localities 20249-PC and 20250-PC. 

Collected by H. M. Duncan and R. A. Lewandowski, July 20, 1961.

20253-PC Garfield 7 Vz -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. North slope of Green Ravine at 5,320-ft 

contour in SW^SE^NW^ sec. 6, T. 2 S., 

R. 3 W. Green Ravine Formation. Collected

USGS Colln. 

No.

20254-PC

20256-PC

20257-PC

20258-PC

20259-PC

20295-PC

Descriptions and collectors

from limestone about 160 ft above base of unit 

11 of type section, near locality 16F32-PC, 

1,031 ft above base of formation. Collected by 

H. M. Duncan, E. W. Tooker, and R. A. 

Lewandowski, July 21, 1961.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. North of Green Ravine near middle of 

west line of SE^NW^ sec. 6, T. 2 S., P. 3 W., 

at 5,400-ft contour. Green Ravine Formation. 

Collected from interbedded fissile limestone 

and argillaceous limestone, 87 ft above base 

of unit 12 of type section, 1,289 ft above base 

of formation. Collected by H. M. F-incan, 

E. W. Tooker, and R. A. Lewandowski, July 

21, 1961.

Garfield 7 1/2 -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measur?d section. On ridge north of Green Ravine in the 

NE^SW^NW1! sec. 6, T. 2 S., R. 3 W., at 

5,320-ft contour. Green Ravine Formation. 

Collected from argillaceous limestone, 298 ft 

above base of unit 11 of type section, 1,169 ft 

above base of formation. H. M. Duncan, E. W. 

Tooker, and R. A. Lewandowski, July 21, 1961.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On ridge north of Green Ravine, same 

locality as 17143-PC. Green Ravine Formation, first limestone ledge below yellowish 

shale, 258 ft above base of unit 11 of type 

section, 1,129 ft above base of formation. 

H. M. Duncan, E. W. Tooker, and R. A. 

Lewandowski, July 21, 1961.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality as 20257-PC but from 

5,240-ft contour. Green Ravine Formation. 

Collected from limestone, 198 ft above base of 

unit 11 of type section, 1,069 ft above base of 

formation. Collected by H. M. Duncan, E. W. 

Tooker, and R. A. Lewandowski, July 21, 1961.

Garfield 7y2-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality as 16318-PC and 17146-PC. 

Lake Point Limestone. Orygmophylluml bed, 

unit 4 of type section. Collected by H. M. 

Duncan, E. W. Tooker, and R. A. Lewandowski, July 21, 1961.

Bingham Canyon 7 ^-minute quadrangle, Tooele 

County. Middle Canyon measured section. On 

ridge that trends southwest from 8745 peak, 

then curves southeastward, in NE^SW^iSE^ sec. 31, T. 3 S., R. 3 W., at 7,940 ft in 

elevation. Clipper Ridge Member of Bingham 

Mine Formation. Collected from limes^ne at 

base of unit 15, same locality as f22574. Collected by R. J. Roberts, 1959.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A63

UflGS Colln. 

No.

20299-PC

20302-PC

20303-PC

20305-PC

20306-PC

20307-PC

20308-PC

Descriptions and collectors

Fairfield 15-minute quadrangle. Toole-Utah 

Counties boundary. Measured section on ridges 

at head of West Canyon. On crest of main 

ridge approximately at 9,200 ft elevation in 

SW%NE% sec. 20, T. 4 S., R. 3 W. Butterfield Peaks Formation. Collected from arenaceous limestone, 431 ft above base of unit 4 

of type section, 1,327 ft above base of formation. Collected by R. J. Roberts and E. W. 

Tooker, 1959.

Fairfield 15-minute quadrangle, Tooele-Utah 

Counties boundary. Measured section on 

ridges at head of West Canyon. Along crest 

roughly 800 ft west of 20299-PC approximately at 9,600-ft contour. Butterfield Peaks 

Formation. Collected from limestone, 287 ft 

above base of unit 5 of type section, 1,813 ft 

above base of formation. Collected by R. J. 

Roberts and E. W. Tooker, 1959.

Fairfield 15-minute quadrangle, Tooele-Utah 

Counties boundary. Measured section on 

ridges at head of West Canyon. Along crest 

roughly 900 ft west-southwest of 20302-PC, 

approximately at 9,900-ft contour, in the SE 1^ 

NW% sec. 20, T. 4 S., R. 3 W. Butterfield Peaks 

Formation. Collected from fossiliferous limestone, 165 ft above base of unit 7 of type section, 2,592 ft above base of formation. Collected by R. J. Roberts and E. W. Tooker, 1959.

Fairfield 15-minute quadrangle, Tooele County. 

Measured section on ridge between Middle 

and Settlement Canyons. On northwest flank 

of 9745 peak on ridge, just above 9,600-ft 

contour, near center NE% sec. 18, T. 4 S., 

R. 3 W. Butterfield Peaks Formation. Collected from arenaceous limestone, 318 ft above 

base of unit 14 of type section, 3.811 ft above 

base of formation. Collected by R. J. Roberts 

and E. W. Tooker, 1959.

Fairfield 15-minute quadrangle, Tooele County. 

Measured section on ridge between Middle 

and Settlement Canyons. In saddle southeast 

of 9590 peak on ridge, roughly 1,000 ft northwest of 20305-PC, in the NW%NEU sec. 18. 

Butterfield Peaks Formation. Collected from 

arenaceous limestone, 9 ft above base of unit 

18 of type section, 4,131 ft above base of formation. Collected by R. J. Roberts and E. W. 

Tooker, 1959.

Fairfield 15-minute quadrangle, Tooele County. 

Measured section on ridge between Middle and 

Settlement Canyons. On 9590 peak on ridge, 

roughly 1,600 ft northwest of 20306-PC. 

Butterfield Peaks Formation. Collected from 

cherty limestone, 347 ft above base of unit 20 

of type section, 4,675 ft above base of formation. Collected by R. J. Roberts and E. W. 

Tooker, 1959.

Fairfield 15-minute quadrangle, Tooele County. 

Measured section on ridge between Middle and

U8G8 Colln. 

No.

20311-PC

20315-PC

20316-PC

20317-PC

20318-PC

20319-PC

203 20-PC

Descriptions and collectors

Settlement Canyons. On ridge roughly 3,900 

ft northwest of 20307-PC where crossed by 

line between R. 3 W. and R. 4 W., just above 

8,850-ft contour line. Butterfield Peaks Formation. Collected from fossiliferous cherty 

limestone, 165 ft above base of unit 26 of type 

section, 5,419 ft above base of formation. 

Collected by R. J. Roberts and E. W. Tooker, 

1959.

Lark 7%-minute quadrangle, Salt Lake County. 

On nose on northwest slope of Copper Gulch, 

6,400 ft due west of Lark, in SE%SE% sec. 

25, T. 3 S., R. 3 W. Same locality and horizon 

as 18892-PC. Bingham Mine Formation, Collected by R. J. Roberts, 1959.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section. Same ridge 

as that of 17168-PC but near 7,200-ft contour, SE%NE% sec. 34, T. 4 S., R. 4 W., 

Butterfield Peaks Formation. Collected from 

medium-light-gray limestone, 241 ft above 

base of unit 3 of reference section, 5<?5 ft 

above base of formation. Collected by R. J. 

Roberts and E. W. Tooker, July 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section. Approximately at 7,300-ft contour. Butterfield Peaks 

Formation. Collected from interbedded limestone and bioclastic limestone, 371 ft above 

base of unit 3 of reference section, 6 r5 ft 

above base of formation. Collected by R. J. 

Roberts and E. W. Tooker, July 1957.

Stockton 15-minute quadrangle, Tooele CcTinty. 

Soldier Canyon measured section, NE%NEH 

sec. 34, approximately at 7,500-ft contour. 

Butterfield Peaks Formation. Collected from 

medium-gray limestone, 58 ft above base of 

unit 4 of reference section, 783 ft above base 

of formation. Collected by R. J. Roberta and 

E. W. Tooker, July 1957.

Stockton 15-minute quadrangle, Tooele Ccunty. 

Soldier Canyon measured section, near 7,700- 

ft contour. Butterfield Peaks Formation. Collected from medium-gray limestone, 54 ft 

above base of unit 5 of reference sectior. 920 

ft above base of formation. Collected by R. J. 

Roberts and E. W. Tooker, July 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section, at 7,000-ft 

contour. Butterfield Peaks Formation. Collected from cherty limestone, 192 ft above base 

of unit 6 of reference section, 1,204 ft above 

base of formation. Collected by E. W. Tooker 

and R. J. Roberts, July 1957.

Stockton 15-minute quadrangle, Tooele Ccunty. 

Soldier Canyon measured section, at 8,000-ft 

contour. Butterfield Peaks Formation. Collected from medium-gray limestone, 183 ft 

above base of unit 7 of reference section,
A64 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

8 Colln.

No.

20321-PC

20322-PC

20323-PC

20324-PC

20325-PC

20329-PC

20330-PC

Descriptions and collectors

1,466 ft above base of formation. Collected by 

R. J. Roberts and E. W. Tooker, July 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section, SW^SW 1^ 

sec. 26, T. 4 S., R. 4 W., at approximately 

8,500-ft contour. Butterfield Peaks Formation. 

Collected from medium-dark-gray arenaceous 

limestone, 101 ft above base of unit 10 of 

reference section, 2,300 ft above base of formation. Collected by R. J. Roberts and E. W. 

Tooker, July 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section, approximately at 8,600-ft contour. Butterfleld Peaks 

Formation. Collected from interbedded bioclastic and argillaceous limestone, 319 ft 

above base of unit 11 of reference section, 

2,813 ft above base of formation. Collected 

by R. J. Roberts and E. W. Tooker, July 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section, approximately at 8,850-ft contour. Butterfield Peaks 

Formation. Collected from interbedded medium-gray limestone, cherty limestone, and bioclastic limestone, 611 ft above base of unit 11 

of reference section, 3,105 ft above base of 

formation. Collected by R. J. Roberts and 

E. W. Tooker, July 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section, approximately at 8,900-ft contour. Butterfield Peaks 

Formation. Collected from thin-bedded darkgray cherty and argillaceous limestone, 330 

ft above base of unit 13 of reference section, 

3,553 ft above base of formation. Collected by 

R. J. Roberts and E. W. Tooker, July 1957.

Stockton 15-minute quadrangle, Tooele County. 

Soldier Canyon measured section, SW^SWH 

sec. 26, T. 4 S., R. 4 W., approximately at 

8,950-ft contour. Butterfield Peaks Formation. 

Collected from medium-dark-gray arenaceous 

cherty limestone, 404 ft above base of unit 

13 of reference section, 3,627 ft above base 

of formation. Collected by R. J. Roberts and 

E. W. Tooker, July 1957.

Fairfield 15-minute quadrangle, Utah County. 

West Canyon measured section. Ridge on 

north slope of West Canyon at Maple Flat, 

in the SE^NW^ sec. 27, T. 4 S., R. 3 W., 

between 6,800- and 6,850-ft contours. West 

Canyon Limestone. Fossils weathering from 

several feet of argillaceous limestone, beginning 60 ft above base of unit 2 of reference 

section, 142 ft above base of formation. Collected by R. J. Roberts and E. W. Tooker, 

July 25, 1957.

Fairfield 15-minute quadrangle, Utah County. 

West Canyon measured section. Same ridge as 

20329-PC, approximately at 7,050-ft contour.

V8G8 Colln. 

No.

20331-PC

20332-PC

20333-PC

21128-PC

21129-PC

21130-PC

Descriptions and collectors

West Canyon Limestone. Collected from argillaceous and arenaceous limestone near base 

of unit 5 of reference section, 438 ft above 

base of formation. Collected by E. W. Tooker 

and R. J. Roberts, July 25, 1957.

Fairfield 15-minute quadrangle, Utah County. 

West Canyon measured section. On same ridge 

as 20329-PC, in SE^SE^SW1^ sec. 22, 

T. 4 S., R. 3 W., approximately at 7,350-ft 

contour. West Canyon Limestone. CoUected 

from limestone, 40 ft above base of unit 12 

of reference section, 1,173 ft above base of 

formation. Collected by R. J. Robert^ and 

E. W. Tooker, July 25, 1957.

Fairfield 15-minute quadrangle, Utah County. 

West Canyon measured section. On same ridge 

as 20329-PC, just below 7,500-ft contour. 

Butterfield Peaks Formation. Collected in 

limestone, approximately 150 ft above base of 

unit 3 of reference section, 436 ft abov? base 

of formation. Collected by R. J. Roberts and 

E. W. Tooker, July 25, 1957.

Fairfield 15-minute quadrangle, Utah County. 

West Canyon measured section. Same ridge 

as 20329-PC, in NW%SW%SE% se~. 22, 

T. 4 S., R. 3 W., approximately on 7,650-ft 

contour. Butterfield Peaks Formation, Collected in limestone, approximately 316 ft above 

base of unit 3 of reference section, 752 ft 

above base of formation. Collected by R. J. 

Roberts and E. W. Tooker, July 25, 1957.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Just above jeep road south of aerial 

tramway on slope about 20 ft below Provo 

level (about 4,800-ft contour), in NE%SE% 

sec. 1, T. 2 S., R. 4 W. Green Ravine Formation. Collected from light-buff-gray argillaceous limestone, 4 ft thick, top of which is 

13 ft stratigraphically below base of bed of 

20243-PC. Collected by M. Gordon, Jr., H. M. 

Duncan, E. W. Tooker, and R. A. Lewandowski, September 8, 1962.

Garfield 7 V2 -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality and approximately same 

stratigraphic interval as 20246-PC. Collected by M. Gordon, Jr., H. M. Duncan, E. W. 

Tooker, and R. A. Lewandowski, September 8, 

1962.

Garfield 7 V2 -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Summit of ridge north of Green Favine, 

about one-eighth mile east of 5244 knoll; same 

general locality as 20258-PC. Green Ravine 

Formation. Collected from 8 ft of darV-gray 

shaly limestone immediately underlying base 

of bed of 20258-PC. Collected by M. Gordon, 

Jr., and R. A. Lewandowski, September 8, 

1962.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A6<5

t'KGf! ColJn. 

No.

21131-PC

21132-PC

21134-PC

21135-PC

21136-PC

21137-PC

21138-PC

DcMcriptions and collectors

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality and bed as 20257-PC. 

Green Ravine Formation. Collected from 15 ft 

of massive dark-gray limestone underlying 

shaly limestone, in unit 11 of type section. 

Collected by M. Gordon, Jr., H. M. Duncan, 

E. W. Tooker, and R. A. Lewandowski, September 8, 1962.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Along trail about 50 ft above bottom of 

first ravine north of Green Ravine, on its 

south slope, in the NW%SE%NWU sec. 6, 

T. 2 S., R. 3 W. Approximately same locality 

and stratigraphic interval as 17144-PC. Green 

Ravine Formation. Collected through 10 ft of 

dark-gray silty limestone exhibiting fracture 

cleavage, in unit 12 of type section. Collected 

by M. Gordon, Jr., H. M. Duncan, E. W. 

Tooker, and R. A. Lewandowski, September 8, 

1962.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Near base of south slope of 6231 hill. 

Same locality as 17145-PC (marked by cairn). 

Lake Point Limestone. From dark-gray silty 

limestone, 147 150 ft above base of unit 1 of 

type section. Collected by M. Gordon, Jr., H. M. 

Duncan, E. W. Tooker, and R. A. Lewandowski, September 8, 1962.

Garfield 7^-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality as 17145-PC but 10-15 ft 

stratigraphically higher. Lake Point Limestone. Collected from 5-ft crinoidal limestone 

with silicified Rhipidomella, 154-159 ft above 

base of unit 1 of type section. Collected by 

M. Gordon, Jr., H. M. Duncan, E. W. Tooker, 

and R. A. Lewandowski, September 9, 1962.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On ridge extending southwestward from 

summit of 6231 hill, approximately at 5,280-ft 

contour. Lake Point Limestone. Loose block 

with Archimedes on slope, 296 ft stratigraphically below base of unit 4 of type section. 

Collected by R. A. Lewandowski, September 8, 

1962.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality as 21136-PC but from 4-in. 

Archimedes-bearing limestone bed, 54 ft stratigraphically higher. Collected by M. Gordon, 

Jr., and R. A. Lewandowski, September 8, 

1962.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. Same locality as 21137-PC but from

U8O8 Colln. 

No.

21139-PC

21140-PC

21141-PC

21151-PC

21152-PC

Descriptions and collectors

loose block on slope, 12 ft stratigraphically 

lower and believed to be approximately in 

place. Collected by M. Gordon, Jr., September 

8, 1962.

Garfield 7 V2 -minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. From lower part of cliff-forming limestone bed in the NW%NW%NW% sec. 6, 

T. 2 S., R. 3 W., one-fourth mile northwest 

of line of type section, approximately at 5,200- 

ft contour. Lake Point Limestone. Collected 

from massive impure limestone; interval in 

type section lies in unit 2, 69-76 ft belo^v 

base of unit 4. Collected by M. Gordon, Jr., 

H. M. Duncan, E. W. Tooker, and R. A. 

Lewandowski, September 9, 1962.

Garfield 7 Ms-minute quadrangle, Tooele Countj. 

Green Ravine-Rogers Canyon measured section. About 300 yards upslope from 21139-PD 

in the NE&NW%NW% sec. 6, T. 2 S., R. 3 

W., at about 5,400 ft elevation. Same locality 

as 16318-PC and 17146-PC. Lake Point Limestone. Brachiopod-bearing gray limestone, 

base of which is 24 ft stratigraphically above 

top of cliff-forming limestone (unit 2) ard 

24 ft below base of Orygmophylluml bed 

(unit 4). Collected by M. Gordon, Jr., H. M. 

Duncan, E. W. Tooker, and R. A. Lewandowski, September 9, 1962.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On ridge trending southwest from summit of 6231 hill. Same locality as 21140-PC. 

Lake Point Limestone. Fossils from upper ?0 

ft of cliff-forming limestone (unit 2 of type 

section), top of which is 48 ft stratigraptically below base of Orygmophyllumt bed 

(unit 4). Collected by M. Gordon, Jr., E. V^. 

Tooker, and R. A. Lewandowski, September 

9, 1962.

Lark 7^-minute quadrangle, Salt Lake County. 

Fossiliferous limestone exposed on south side 

of hill at north side of Copper Gulch alor<r 

line of telephone poles between 6,480 ard 

6,500 ft in elevation in the SW^iSE^SE^i 

sec. 25, T. 3 S., R. 3 W., a little over 1 mile 

west of Lark. Same locality as 18892-PC ard 

20311-PC. Collected by M. Gordon, Jr., H. 1*. 

Duncan, E. W. Tooker, and R. A. Lewandovski, September 13, 1962.

Garfield 7 ^-minute quadrangle, Salt Lake 

County. Outcrops on north side of Coon Canyon, about 0.1 mile downstream from junction of Left Hand and Right Hand Forks, 

in the SE%NW%NW% sec. 14, T. 2 S., 

R. 3 W. Same locality as 20240-PC and aho 

from outcrops ascending slope to east. Grandeur Member of Park City Formation. Basal 

30-ft limestone, unit 1 of Tooker-Roberts station. Collected by M. Gordon, Jr., H. M. Dun-
A66 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

UBG8 Colln.

21154-PC

21155-PC

21156-PC

21157-PC

22484-PC

22486-PC

23854-PC

Descriptions and collectors

can, E. W. Tooker, and R. A. Lewandowski, 

September 13, 1962.

Fairfield 15-minute quadrangle, Utah County. 

West Canyon measured section. North slope 

of West Canyon due north of mouth of Maple 

Canyon and east of unnamed spring, in the 

SW%NE%NW& sec. 27, T. 4 S., R. 3 W. 

West Canyon Limestone. Weathered out fossils from lowest covered outcrop on slope, 1 GO150 ft above canyon floor. Same locality and 

approximately same interval as 20329-PC. 

Collected by M. Gordon, Jr., H. M. Duncan, 

E. W. Tooker, and R. A. Lewandowski, September 14, 1962.

Fairfield 15-minute quadrangle, Utah County. 

West Canyon measured section. About 100 

yards east of line of section in next little depression on slope. West Canyon Limestone. 

Silicified bracihopods from 1-ft band in lowest 

outcrop in place, approximately in middle of 

interval from which float fossils of 21154-PC 

were collected, probably in unit 2 of TookerRoberts section. Collected by M. Gordon, Jr., 

H. M. Duncan, E. W. Tooker, and R. A. Lewandowski, September 14, 1962.

Fairfield 15-minute quadrangle, Utah County. 

West Canyon measured section. From approximate line of section in 2-ft bed in place, 

roughly 100 ft above base of unit 3 of type 

section. Collected by M. Gordon, Jr., H. M. 

Duncan, E. W. Tooker, and R. A. Lewandowski, September 14, 1962.

Fairfield 15-minute quadrangle, Utah County. 

West Canyon measured section. Fossils weathered out from slightly more than 100 ft of 

beds in unit 4 of Tooker-Roberts section. Fossils consisted almost exclusively of Flexaria. 

Collected by M. Gordon, Jr., H. M. Duncan, 

E. W. Tooker, and R. A. Lewandowski, September 14, 1962.

Magna 7^-minute quadrangle, Salt Lake County. 

SWHNW 1^ sec. 30, T. 1 S., R. 3 W., at 4,800- 

4,820 ft elevation, on Provo Terrace, west of 

Magna. Same as 19948-PC. Grandeur Member of Park City Formation. Collected from 

basal limestone unit. Collected by R. J. Roberts and E. W. Tooker, October 1961.

Bingham Canyon 7%-minute quadrangle, Tooele 

County. Middle Canyon measured section. On 

northwest side of ravine in the SE^NW1^ 

sec. 6, T. 4 S., R. 3 W., at altitude 6,240 ft. 

Clipper Ridge Member of Bingham Mine Formation. Collected from thin-bedded limestone, 

104 ft above base of unit 2 of type section. 

Collected by E. W. Tooker and R. J. Roberts, 

October 1961.

Garfield 7%-minute quadrangle, Tooele County. 

Green Ravine-Rogers Canyon measured section. On southwest-trending ridge of hill 6231,

USG8 Colln. 

No.

23855-PC

23890-PC

Descriptions and collectors

approximately in NE. cor NW 1/4NV'r }i sec. 6, 

T. 2 S., R. 3 W., at altitude of approximately 

5,850 ft. Lake Point Limestone. Collected from 

2-ft bed of gray argillaceous limestone, 15 ft 

above top of yellowish-brown-weatl ?ring bed 

(unit 8 of type section). Collected ty M. Gordon, Jr., and K. R. Moore, August 22, 1969.

Garfield 7%-minute quadrangle, Tooe1 *? County. 

Green Ravine-Rogers Canyon measured section. Southwest-trending ridge of 6231 hill 

approximately at line between T. 1 S. and 

T. 2 S. Lake Point Limestone. Collected from 

2-ft bed of argillaceous limestone, ton of which 

is 100 ft stratigraphically below top of formation. Collected by M. Gordon, Jr., and K. R. 

Moore, August 22, 1969.

Bingham Canyon 7%-minute quadrangle, Tooele 

County. Middle Canyon measured section. On 

south of 8745 summit, in NE%SE% sec. 31, 

T. 3 S., R. 3 W., at 8,420-ft contour. Clipper 

Ridge Member of Bingham Mine Formation. 

Collected from fine-grained arenaceous limestone, 5 ft above base of unit 18 of type section, 2,957 ft above base of member. Collected 

by R. J. Roberts and E. W. Tooker, October 

1961.

REGISTER OF LATE PALEOZOIC FUSULINID

COLLECTING LOCALITIES IN TFE

OQUIRRH MOUNTAINS, UTAH

Identification of and comments concerning fumlinids 

by R. C. DOUGLASS

[Dates following Douglass' comments are of his written reports]

USGS Colln.

No. Descriptions and collectors

f 20479 Garfield 7 ^-minute quadrangle, Fait Lake

County. Center of east side, SE 1^ sec. 22,

T. 1 S., R. 3 W., approximately 1 mile north

of type section near 4,820-ft contour. Kessler

Canyon Formation. Collected from bioclastic

limestone lens in fusulinid chert bed 6 ft

above base of unit 29, 3,027 ft above base of

formation. Collected by R. J. Roberts, 1958.

"limestone * * * has been recrystallized,

destroying all but gross structures. Triticites sp. Possibly a Pseudofusulinella also

present, but too badly recrystallized for

positive identification. Late Pennsylvanian

or Early Permian age is indicate!." 1959.

f20486 Garfield 7%-minute quadrangle, Tooele County. 

North slope Rogers Canyon, center sec. 31, 

T. 1 S., R. 3 W. Erda Formation. Collected 

from limestone 101 ft above base of unit 3 of 

type section, 502 ft above base of formation. 

Collected by R. C. Douglass and R. J. Roberts, 

1958.

" * * * Sample contains a few scattered 

specimens of Profusulinella which suggests 

an early Atoka-early Middle Pennsylvanian 

age." 1961.
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A67

USG8 Colln.

No. Descriptions and collectors

£21018 Garfield 7%-minute quadrangle, Salt Lake 

County. West side tributary of Little Valley 

Wash, SW^SW^NE 1^ sec. 35, T. 1 S., 

R. 3 W., at 5,400-ft contour, approximately 

% mile southeast of type section. Kessler 

Canyon Formation. Collected from poorly 

sorted fine-grained sandstone nearly 200 ft 

above base of unit 37, 4,409 ft above base of 

formation. Collected by R. J. Roberts, 1958.

" * * * Clear area [in sandstone] representing recrystallized fusulines. Some specimens showing a little residual structure. 

Triticit.es sp. probably Upper Pennsylvanian." 1959.

f22568 Garfield 7 Vz -minute quadrangle, Tooele County, 

Black Rock Canyon area, same locality as 

20232-PC, 1 mile east-northeast of type section, NE^NW^ sec. 32, T. 1 S., R. 3 W. 

Erda Formation. Collected from gray cherty 

limestone. Collected by E. W. Tooker, 1957.

"This sample represents late Middle Pennsylvanian age (Des Moines equivalent). 

Climacammina sp. 

Bradyina sp. 

Fusulina sp. 

Wedekindellinal." 1962.

f22569 Garfield 7%-minute quadrangle, Tooele County. 

Big Canyon area, 1% miles south of type section, Vs mile west of tower 7417 on tramway, 

SW%NE% sec. 7, T. 2 S., R. 3 W., same 

locality as 20232-PC. Erda Formation. Collected from cherty limestone. Collected by 

E. W. Tooker, 1957.

"This sample represents late Middle Pennsylvanian (Des Moines) age. 

Fusulina sp." 1962.

f22570 Garfield 7%-minute quadrangle, Tooele County. 

Type locality north side Rogers Canyon, 

SW%NE% sec. 31, T. 1 S., R. 3 W., near 

6,440-ft contour. Erda Formation. Collected 

from thin-bedded cherty limestone 11 ft above 

base of unit 24, 2,488 ft above base of formation. Collected by R. J. Roberts and E. W. 

Tooker, 1957.

"This sample represents late Middle Pennsylvanian (Des Moines) age. 

Textularid 

Fusulina sp." 1962.

f 22512 Bingham Canyon 7%-minute quadrangle, Tooele 

County. Ridge nose north of Middle Canyon, 

NW%SE%SE% sec. 31, T. 3 S., R. 3 W., 

8,440-ft contour southwest of summit 8745. 

Clipper Ridge Member, Bingham Mine Formation. Collected from limestone at base of 

unit 18 of type section, a few tens of feet west 

of the type section, 2,952 ft above base of 

member, 2,952 ft above base of formation. 

Collected by R. J. Roberts, 1959.

U8Q8 Colln. 

No.

f22574

f22576

f22577

f22578

f22580

Descriptions and collectors

"Fragments of textularids and Triticites sp. 

in a fine sand matrix. The age suggested by 

the Triticites is Late Pennsylvanian, probsbly Missouri equivalent." 1962.

Bingham Canyon 7 }&-minute quadrangle, Tooele 

County. Ridge nose south north of Middl0 

Canyon, SW^NE^iSE^i sec. 31, T. 3 S-, 

R. 3 W., at 7,940-ft contour south-southwest 

of summit 8745. Clipper Ridge Member, 

Bingham Mine Formation. Collected frorr 

coarse bioclastic limestone at the base of unit 

15 of type section, 2,627 ft above base of th? 

member and formation. Collected by R. J. 

Roberts and E. W. Tooker, 1959.

"Coarse bioclastic limestone with textularid'' 

and Triticites sp. suggesting Late Pennsylvanian age, probably Missouri equivalent." 

1962.

Fairfield 15-minute quadrangle, Tooele County. 

Ridge on south side of Middle Canyon about 

1,000 ft north of 8944 Peak, NE%NE% sec. 

12, T. 4 S., R. 4 W., at 8,500-ft contour. 

Butterfield Peaks Formation. Collected from 

arenaceous limestone approximately 109 ft 

above base of unit 33 of type section, 6,476 ft 

above base of formation. Collected by R. J. 

Roberts and E. W. Tooker, 1959.

"Fine sand with textularids and abundant 

fusulinids including Fusulina sp. and Wedekindellina sp. The age indicated is Middle 

Pennsylvanian, Des Moines equivalent." 1962.

Fairfield 15-minute quadrangle, Utah County. 

Ridge east of White Pine Canyon, SE^NW^, 

sec. 20, T. 4 S., R. 3 W., at 9,200-ft contour. 

Butterfield Peaks Formation. Collected frorr 

bioclastic limestone 431 ft above base of unit 

4 of type section, 1,327 ft above base of formation. Location of colln. 20299-PC. Collected 

by R. J. Roberts and E. W. Tooker, 1959. 

"Bioclastic limestone with textularids, Fusulina sp. and Wedekindellina sp. similar 

in age to f22576 above." 1962.

Fairfield 15-minute quadrangle, Tooele-Utah 

County line. Ridge separating White Pine an'* 

West Canyon at 9,750-ft contour, SE^NW^i 

sec. 20, T. 4 S., R. 3 W. Butterfield Peaks 

Formation. Collected from bioclastic limestone 775 ft above base of unit 5 of type section, 2,301 ft above base of formation. Co'- 

lected by R. J. Roberts and E. W. Tooker, 

1959.

"Fine bioclastic limestone with Fusulinella 

sp. The age suggested is Middle Pennsylvania^ early Des Moines equivalent," 1962.

Fairfield 15-minute quadrangle, Tooele County. 

Ridge southwest of Middle Canyon in saddle 

south of 8944 Peak, SE%NE% sec. 12, T. 4 S., 

R. 4 W. Butterfield Peaks Formation. Co1 - 

lected from bioclastic limestone layer in chert v
A68 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

-S Colln. 

AT o.

£22581

£22582

£22583

£22584

£22588

Descriptions and collectors

limestone 175 ft above base of unit 26 of type 

section, 5,429 ft above base of formation. 

Collected by R. J. Roberts and E. W. Tooker, 

1959.

"Bioclastic limestone with textularids and 

abundant Fusulina sp. of an advanced type. 

The age indicated is Middle Pennsylvanian, 

late Des Moines equivalent." 1962.

Fairfield 15-minute quadrangle, Tooele County. 

Same locality as f22580, about 3 ft higher in 

section. Collected by R. J. Roberts and E. W. 

Tooker, 1959.

"The lithology and fauna are similar and 

the same age is suggested." 1962.

Fairfield 15-minute quadrangle, Tooele County. 

Same locality as f22580, 20 ft higher in section. Butterfield Peaks Formation. Collected 

from silty bioclastic limestone of type section. 

Collected by R. J. Roberts and E. W. Tooker, 

1959.

"The limestone * * * contains abundant 

bryozoa in addition to the Fusulina sp. The 

age suggested is still Middle Pennsylvanian, 

late Des Moines equivalent." 1962.

Fairfield 15-minute quadrangle, Tooele County. 

Ridge southwest of Middle Canyon, 8944 Peak, 

NE%NE%, sec. 12, T. 4 S., R. 4 W. Butterfield Peaks Formation. Collected from arenaceous limestone 12 ft above base of unit 31 of 

type section, 6,048 ft above base of formation. 

Collected by E. W. Tooker and R. J. Roberts, 

1959.

"Fine sand with Fiisulinella sp. The age 

suggested is Middle Pennsylvania." 1962.

Fairfield 15-minute quadrangle, Tooele County. 

Same locality as f22583, but 33 ft higher 

stratigraphically. Butterfield Peaks Formation. Collected from fine sand of type section. 

Collected by E. W. Tooker and R. J. Roberts, 

1959.

"Fine sand with Fusulina sp. The age suggested is Middle Pennsylvanian, Des Moines 

equivalent." 1962.

Garfield 7 *£-minute quadrangle, Salt Lake 

County. Nose of ridge on slope southeast of 

Kessler Canyon, west of Peak 5984, center 

SEV4 SE% sec. 27, T. 1 S., R. 3 W., approximately at 5,720-ft contour. Kessler Canyon 

Formation. Collected from arenaceous limestone 92 ft above base of unit 21 of type section, 2,221 ft above base of formation. Collected by R. J. Roberts and E. W. Tooker, 

1959.

"The rock of this sample is completely altered. It looks like it may have been a fine 

bioclastic limestone, and it apparently contained small brachiopods and fusulinids. 

Only the gross features of the fusulinids 

are left, and I would not feel safe in any

U8GS Colln. 

No.

f22597

f22598

£22599

f22600

f22601

Descriptions and collectors

generic identification of this material. Comparisons with the other samples from the 

area suggest closest relationship to some 

of the Triticites of Late Pennsylvsnian age, 

but I certainly couldn't count on this. Early 

Pennsylvanian and Permian ager are not 

likely." 1962.

Bingham Canyon 7%-minute quadrangle, Tooele 

County. North side Middle Canyon, r'dge leading to Peak 8745, center west side 1 T EM sec. 

6, T. 4 S., R. 4 W., at 6,360-ft contour Clipper 

Ridge Member, Bingham Mine Formation. 

Collected from arenaceous limestore in the 

lower 8 ft of unit 2 of type section, 10 ft 

above base of member and the formation. 

Collected by R. J. Roberts and E. W. Tooker, 

1961.

"Fine sand with scattered worn Triticites 

sp. The age suggested is Late Pennsylvanian, Missouri equivalent." 1962.

Bingham Canyon 7 % -minute quadrangle, Tooele 

County. Same locality as £22597,- NV'%NE%, 

sec. 6, T. 4 S., R. 3 W., at 7,760-ft contour. 

Clipper Ridge Member, Bingham Mine Formation. Collected from arenaceous limestone 

about 7 ft above base of unit 6 of typ« section, 

1,284 ft above base of the member and the 

formation. Collected by E. W. Tooker and 

R. J. Roberts, 1961.

"Fine sand with abundant Triticites sp. 

The age suggested is Late Penrsylvania, 

Missouri equivalent." 1962.

Bingham Canyon 7%-minute quadrangle, Tooele 

County. Same locality as f22597, SW^SE^ 

sec. 31, T. 3 S., R. 3 W., at 7,760-ft contour. 

Clipper Ridge Member, Bingham Fine Formation. Collected from arenaceous limestone 

2 ft above base of unit 9 of type section, 

1,967 ft above base of the member and of 

the formation. Collected by R. J. Roberts and 

E. W. Tooker, 1961.

"Fine sand with fragments of Triticites 

sp. The age is probably still Missouri 

equivalent." 1962.

Bingham Canyon 7%-minute quadrangle, Tooele 

County. Ridge on north side Middle. Canyon, 

south of Peak 8745, SW%SE% sec. 31, T. 3 

S., R. 3 W., at 8,000-ft contour. Clipper Ridge 

Member, Bingham Mine Formation. Collected 

from 2-ft-thick coarse bioclastic limestone 

309 ft above base of unit 11 of typ« section, 

2,379 ft above base of member and formation.. 

Collected by R. J. Roberts and E. W. Tooker, 

1961.

"Coarse bioclastic limestone with Bradyina 

sp., bryozoa, and Triticites sp. The age 

suggested is still Late Pennsylvar ian, Missouri equivalent." 1962.

Bingham Canyon 7 Vz -minute quadrangle, Tooele 

County. Same locality as f22600, N
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH A 69

T'flOS Colln.

No. DeKcriptions and collectors

sec. 31, T. 3 S., R 3 W., at 8,280-ft contour. 

Clipper Ridge Member, Bingham Mine Formation. Collected from fine-grained arenaceous limestone 3-5 ft above base of unit 16 

of type section, 2,772 ft above base of member and formation. Collected by E. W. Tooker 

and R. J. Roberts, 1961.

"Fine sand with fragments of textularids 

and Triticites sp. of Late Pennsylvanian 

age." 1962.

f22602 Bingham Canyon 7 Vz -minute quadrangle, Tooele 

County. Same locality as f22600, NW^SE 1^ 

sec. 31, T. 3 S., R. 3 W., at 8,300-ft contour. 

Clipper Ridge Member, Bingham Mine Formation. Collected from fine-grained arenaceous limestone 21 ft above base of unit 16 

of type section, 2,790 ft above base of member 

and formation. Collected by R. J. Roberts and 

E. W. Tooker, 1961.

"Fine sand with Triticites sp. This sample 

looks more advanced than the others along 

this line of section. If I saw it by itself, 

I would call it Virgil equivalent. It may be 

late Missouri, however." 1962.

f 22603 Bingham Canyon 7 % -minute quadrangle, Tooele 

County. Same locality as f22600, NE^SE 1^ 

sec. 31, T. 3 S., R. 3 W., at 8,420-ft contour. 

Clipper Ridge Member, Bingham Mine Formation. Collected from fine-grained arenaceous limestone 5 ft above base of unit 18 

of type section, 2,957 ft above base of member and formation. Collected by R. J. Roberts 

and E. W. Tooker, 1961.

"Fine sand with textularids and Triticites 

sp. Again, this sample has an early Virgil 

aspect but could be late Missouri." 1962.

f22604 Bingham Canyon 1% -minute quadrangle, Tooele 

County. Same locality as f22600, NE^SE 1^ 

sec. 31, T. 3 S., R. 3 W., at 8,440-ft contour. 

Clipper Ridge Member, Bingham Mine Formation. Collected from arenaceous limestone 

at base of unit 20 of type section, 2,980 ft 

above base of member and formation. Collected by R. J. Roberts and E. W. Tooker, 

1961.

" * * * Includes some specimens of Triticites 

sp. [and] * * * common IKansanella sp., 

a form originally described from beds of 

Missouri age in the midcontinent area. 

MillereUa sp. and the bryozoans are also 

found in this sample. The range of Kansanella in the Basin Ranges is not yet 

established." 1962.

f23112 Bingham Canyon 7%-minute quadrangle, Tooele 

County. Ridge between Peak 8745 and 8536, 

SWi/iNE^NE^ sec. 31, T. 3 S., R. 3 W., at 

8,600-ft contour. Markham Peak Member, 

Bingham Mine Formation. Collected from 

silty limestone of unit 10 of type section,

U8GS Colln. 

No.

f23105

f23106

f23107

f23108

f23109

f23111

Descriptions and collectors

883 ft above base of member, 3,868 ft above 

base of formation. Collected by R. J. Roberts 

and E. W. Tooker, 1963.

"Recrystallized specimens of small fu^ulinids which resemble the Triticites of 

many of the other samples in size rnd 

shape, but which are indeterminate." 1964.

Bingham Canyon 7%-minute quadrangle, Tocele 

County. Clipper Ridge north of Middle Canyon, NE^SE^SW^ sec. 36, T. 3 S., R. 3 W., 

at 6,280-ft contour. Markham Peak Memler, 

Bingham Mine Formation. Collected from 

arenaceous limestone approximately 53 ft 

above base of unit 11 (in reference section) 

about 1 mile west of type section, 940 ft above 

base of member. Collected by R. J. Roberts 

and E. W. Tooker, 1963. 

"Triticites sp." 1964.

Bingham Canyon 7%-minute quadrangle, Tootle 

County. Same locality as f23105 but 20 ft 

higher in section. Markham Peak Member, 

Bingham Mine Formation. Collected fr?m 

arenaceous limestone of unit 14. Collected by 

R. J. Roberts and E. W. Tooker, 1963. 

"Triticites sp." 1964.

Bingham Canyon 7 % -minute quadrangle, Tootle 

County. Same locality as f22105, but 85 ft 

higher in section. Markham Peak Member, 

Bingham Mine Formation. Collected from 

arenaceous limestone of unit 14 in referer^e 

section. Collected by R. J. Roberts and E. W. 

Tooker, 1963. 

"Triticites sp. 

Climacammina" 1964.

Bingham Canyon 7%-minute quadrangle, Tootle 

County. Same locality as f22105. Markham 

Peak Member, Bingham Mine Formation. 

Collected from cherty arenaceous limestone 

104 ft above base of unit 14 of refererce 

section, 1 mile west of type section, 1,566 ft 

above base of member, 4,551 ft above base of 

formation. Collected by R. J. Roberts and 

E. W. Tooker, 1963.

"Triticites sp. abundant and well preserved. 

Climacammina sp." 1964.

Bingham Canyon 7^-minute quadrangle, Tooele 

County. Same locality as f23108, but 37 ft 

higher in section. Markham Peak Member, 

Bingham Mine Formation. Collected from 

limestone of unit 14 of reference section. Collected by R. J. Roberts and E. W. Tooker. 

"Triticites sp." 1964.

Bingham Canyon 7%-minute quadrangle, Tooele 

County. Ridge west of Spring Canyon, north 

center SE^NW^ sec. 30, T. 3 S., R. 3 V., 

at 7,125-ft contour. Markham Peak Member, 

Bingham Mine Formation. Collected from 

sandy limestone 14 ft above base of unit 15
A70 GEOLOGIC STUDIES OF THE BINGHAM MINING DISTRICT, UTAH

Colln. 

JVo. Descriptions and collectors

of type section, 2,547 ft above base of member, 

5,532 ft above base of formation. Collected by 

R. J. Roberts and E. W. Tooker, 1963.

"Triticites sp. but reworked specimens." 

1964.

f22431 Bingham Canyon 7%-minute quadrangle, TooeleSalt Lake Counties. Ridge northeast of Clipper Peak separating Baltimore Gulch and 

Bingham Canyon, immediately north of abandoned tramway, NE%SE%SE% sec. 28, T. 3 

S., R. 3 W., at 8,340-ft contour. Markham 

Peak Member, Bingham Mine Formation. Collected from limestone at base of unit 11 (1 

mile south along ridge from measured section), approximately 1,370 ft above base of 

member, 4,355 ft above base of formation. 

Collected by E. W. Tooker and R. J. Roberts, 

1964.

"Triticites sp." 1966.

f23432 Bingham Canyon 7%-minute quadrangle, Salt 

Lake County. Ridge east from Markham Peak, 

center south edge SE^NW^i sec. 22, T. 3 S., 

R. 3 W., at about 8,000-ft contour. Markham 

Peak Member, Bingham Mine Formation. Collected from calcareous sandstone 76 ft above 

base of unit 13 of Markham Peak (continuation of the upper part) type section, 1,446 ft 

above base of member, 4,431 ft above base of 

formation. Collected by E. W. Tooker and 

W. J. Moore, 1964.

"Triticites sp.

Pseudofusulinella sp." 1966.

f23433 Bingham Canyon 7 Ms-minute quadrangle, Salt 

Lake County. Same locality as f23432, at 

about 8,080-ft contour. Markham Peak Member, Bingham Mine Formation. Collected from 

calcareous sandstone 224 ft above base of 

unit 13 in Markham Peak type section, 1,594 

ft above base of member, 4,579 ft above base 

of formation. Collected by E. W. Tooker and 

W. J. Moore, 1964.

"The fusulinids are recrystallized, obliterating almost all structure. They appear to 

represent a large Triticites suggestive of a 

Virgil age." 1966.

REFERENCES

American Commission on Stratigraphic Nomenclature, 1961, 

Code of stratigraphic nomenclature: Am. Assoc. Petroleum Geologists Bull., v. 45, no. 5, p. 645-665.

Baker, A. A. 1947, Stratigraphy of the Wasatch Mountains 

in the vicinity of Provo, Utah: U.S. Geol. Survey Prelim. 

Inv. Oil and Gas Chart 30, scale approx. 1 in. to 5 miles.

Baker, A. A., Huddle, J. W., and Kinney, D. M., 1949, 

Paleozoic geology of north and west sides of Uinta 

Basin, Utah: Am. Assoc. Petroleum Geologists Bull., 

v. 33, no. 7, p. 1161-1197.

Bissell, H. J., 1936, Pennsylvanian and Lower Permian stratigraphy of the southern Wasatch Mountains. Utah. 

Iowa Univ., Iowa City, M.S. thesis.

_____1959, Stratigraphy of the southern Oquirrl Mountains, Upper Paleozoic succession, Pennsylvanian system in Bissell, H. J., ed., Geology of the southern Oquirrh 

Mountains and Fivemile Pass-northern Boulter Mountain area, Tooele and Utah Counties, Utah: Utah Geol. 

Soc. Guidebook 14, p. 93-127.

_____1962, Pennsylvanian-Permian Oquirrh Basin of 

Utah: Brigham Young Univ. Geology Studies, v. 9, 

p. 26-49.

Boutwell, J. M., 1905, Economic geology of the Pmgham 

mining district, Utah: U.S. Geol. Survey Prof. Prper 38, 

p. 73-387.

_____1907, Stratigraphy and structure of the Prrk City 

mining district, Utah: Jour. Geology, v. 15, p. 434-458.

Cheney, T. M., Swanson, R. W. Sheldon, R. P., and McKelvey, V. E., 1959, Grandeur Member, in McKelvey, V. E., 

and others, The Phosphoria, Park City and Shedhorn 

Formations in the western phosphate field: U.S. Geol. 

Survey Prof. Paper 313-A, p. 12-14.

Cook, D. R., ed., 1961, Geology of the Bingham mining district 

and northern Oquirrh Mountains: Utah Geol. Soc. Guidebook 16, 145 p.

Crittenden, M. D., 1959, Mississippian stratigraphy of the 

central Wasatch and western Uinta Mountains, Utah, in 

Wiliams, N. C., ed., Guidebook to the geology of the 

Wasatch and Uinta Mountains transition area: Intermountain Assoc. Petroleum Geologists Guidebook, 19th 

Ann. Field Conf., 1959, p. 63-74.

_____1961, Magnitude of thrust faulting in northern Utah, 

in Geological Survey research, 1961: U.S. Geol. Survey 

Prof. Paper 424-D, p. D128-D131.

Dott, R. H., Jr., 1955, Pennsylvanian stratigraphy of Elko 

and northern Diamond Ranges, northeastern Nevada: 

Am. Assoc. Petroleum Geologists Bull., v. 39, no. 11, 

p. 2211-2305, 19 figs., 5 tables.

Drewes, Harald, 1967, Geology of the Conners Pass quadrangle, Schell Creek Range, east-central Nevada: U.S. 

Geol. Survey Prof. Paper 557, 93 p., 3 pis., 14 figs., 

16 tables.

Dutro, J. T., and Sando, W. J., 1963, New Mississiprian formations and faunal zones in the Chesterfield Range, 

Portneuf quadrangle, southeast Idaho: Am. Afsoc. Petroleum Geologists Bull., v. 47, no. 11, p. 19^-1986, 

6 figs.

Furnish, W. M., and Knapp, W. D., 1966, Lower Pennsylvanian fauna from Kentucky Part 1, Ammonou's: Jour. 

Paleontology, v. 40, no. 2, p. 296-308, pi. 35, 5 figs.

Gilluly, James, 1932, Geology and ore deposits of th« Stockton and Fairfield quadrangles, Utah: U.S. Geol, Survey 

Prof. Paper 173, 171 p.

Gordon, Mackenzie, Jr., 1970, Carlinia, a Late Mississippian 

genus of Productidae from the western Unitec1 States, 

in Paleozoic Precepts; Smithsonian Contributions to 

Paleobiqlogy, no. 2 (in press).
UPPER PALEOZOIC ROCKS IN THE OQUIRRH MOUNTAINS AND BINGHAM MINING DISTRICT, UTAH ATI

Hewitt, W. P., 1966, Pennsylvanian and Permian basins in 

northwestern Utah, northeastern Nevada, and south 

central Idaho Discussion: Am. Assoc. Petroleum Geol 

ogists Bull., v. 30, no. 7, p. 1523.

Hose, R. K., and Repenning, C. A., 1959, Stratigraphy of 

Pennsylvanian, Permian, and Triassic rocks of Confusion Range, west-central Utah: Am. Assoc. Petroleum 

Geologists Bull., v. 43, p. 2167-2196, 6 figs.

Hunt, R. N., 1924, The ores in the limestones at Bingham 

Utah: Am. Inst. Mining Engineers Trans., v. 70, p. 856- 

883.

James, A. H., Smith, W. H., and Welsh, J. E., 1961, General 

geology and structure of the Bingham district, Utah, 

in Cook, D. R., ed., Geology of the Bingham mining district and northern Oquirrh Mountains: Utah Geol. Soc. 

Guidebook 16, p. 49-69.

James, A. H., Smith, W. H., Welsh, J. E., and others, 1961, 

Kennecott Copper Corporation surface geology map of 

the Bingham district, in Cook, D. R., ed., Geology of the 

Bingham mining district and northern Oquirrh Mountains: Utah Geol. Soc. Guidebook 16, pi. 2.

Keith, Arthur, 1905, Areal geology of the Bingham district, 

in Boutwell, J. M., Economic geology of the Bingham 

mining district, Utah: U.S. Geol. Survey Prof. Paper 38, 

p. 29-72.

Langenheim, V. A. M., and Langenheim, R. L, Jr., 1965, The 

Bird Spring Group, Chesterian through Wolfcampian at 

Arrow Canyon Range, Clark County, Nevada: Ilinois 

State Acad. Sci., Trans., v. 58, no. 4, p. 225-240, 6 figs.

Morris, H. T., and Lovering, T. S. 1961, Stratigraphy of the 

east Tintic Mountains, Utah: U.S. Geol. Survey Prof. 

Paper 361, 145 p.

Morse, W. C., 1931, The Pennsylvanian invertebrate fauna: 

Kentucky Geol. Survey ser. 6, v. 36, p. 293-348, 2 figs., 

10 pis.

Nolan, T. B., 1935, The Gold Hill mining district, Utah: U.S. 

Geol. Survey Prof. Paper 177, 172 p., 15 pis., 31 figs.

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

stratigraphic section in the vicinity of Eureka, Nevada: 

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

Nygreen, P. W. 1958, The Oquirrh Formation Stratigraphy 

of the lower portion in the type area and near Logan, 

Utah: Utah Geol. Mineralog. Survey Bull., v. 61, 67 p.

Peters, W. C., James, A. H., and Field, C. W., 1966, Geology 

of the Bingham Canyon porphyry copper deposit, Utah, 

in Titley, Spencer, and Hicks, Carol, eds., Geology of the 

porphyry copper deposits, southwestern North America: 

Tucson, Ariz., Univ. Arizona Press, p. 165-175.

Rich, Mark, 1961, Stratigraphic section and fusulinids of the 

Bird Spring formation near Lee Canyon, Clark County, 

Nevada: Jour. Paleontology, v. 35, no. 6, p. 1159-1180, 

pis. 142-146, 4 figs.

Roberts, R. J., 1964 [1965], Stratigraphy and structure of 

the Antler Peak quadrangle, Humboldt and Lan<Jer 

Counties, Nevada: U.S. Geol. Survey Prof. Paper 459-A, 

p. A1-A93, 7 pis., 37 figs., 10 tables.

Roberts, R. J., Crittenden, M. D., Jr., Tooker, E. W., Morris, 

H. T., Hose, R. K, and Cheney, T. M., 1965, Pennsylvanian and Permian basins in northwestern Utah, northeastern Nevada and south-central Idaho: Am. Assoc. 

Petroleum Geologists Bull., v. 49, no. 11, p. 1926-195?.

Roberts, R. J., and Tooker, E. W., 1961, Structural geology of 

the north end of the Oquirrh Mountains, Utah, in Cock, 

D. R., ed., Geology of the Bingham mining district and 

northern Oquirrh Mountains: Utah Geol. Soc. Guidebook 16, p. 36-48.

Schwartz, G. M., 1947, Hydrothermal alteration in the 

"porphyry copper" deposits: Econ. Geology, v. 42, no. 4, 

p. 319-352.

Silberling, N. J., and Roberts, R. J., 1962, Pre-Tertiary 

stratigraphy and structure of northwestern Nevada: Geol. 

Soc. America Spec. Paper 72, 58 p.

Smith, W. H., 1961, The volcanics of the eastern slopes of tl <?. 

Bingham district, Utah, in Cook, D. R., ed., Geology of 

the Bingham mining district and northern Oquirrh 

Mountains: Utah Geol. Soc. Guidebook 16, p. 101-119.

Spurr, J. E., 1895, Economic geology of the Mercur minirg 

district, Utah: U.S. Geol. Survey 16th Ann. Rept., pt. 2, 

p. 374-376.

Steele, Grant, 1960, Pennsylvanian-Permian stratigraphy of 

east-central Nevada and adjacent Utah, in Geology of 

east-central Nevada: Intermountain Assoc. Petroleum 

Geologists Guidebook, llth Ann. Field Conf., 1960, p. 91- 

113, 8 pis., 1 correlation chart.

Stringham, Bronson, 1953, Granitization and hydrothermal 

alteration at Bingham, Utah: Geol. Soc. America Bull., 

v. 64, no. 8, p. 945-991.

Tooker, E. W., 1962, Clay minerals in rocks of the lower 

part of the Oquirrh Formation, Utah, in Bailey, S. W., 

ed., in Clays and clay minerals, v. 9 14th National Conference on Clays and Clay Minerals Proceedings: Ne-v 

York, Pergamon Press, p. 355-364.

Tooker, E. W., and Roberts, R. J., 1961, Stratigraphy of th«. 

north end of the Oquirrh Mountains, Utah, in Cool', 

D. R., ed., Geology of the Bingham mining district and 

northern Oquirrh Mountains: Utah Geol. Soc. Guidebook 16, p. 17-35.

_____1963, Comparison of Oquirrh Formation sections in 

the northern and central Oquirrh Mountains, Utah, in 

Geological Survey research, 1962: U.S. Geol. Survey 

Prof. Paper 450-E, p. E32-E36.

Welsh, J. E., and James, A. H., 1961, Pennsylvanian and 

Permian stratigraphy of the central Oquirrh Mountains, 

Utah, in Cook, D. R., ed., Geology of the Bingham miring district and northern Oquirrh Mountains: Utah Geo1 , 

Soc. Guidebook 16, p. 1-16.

INDEX

Page

Arnnthocladia sp _____ ____ __ A54

Aranthopecten sp _____ __ _ 47

Adobe Rook _____________________ 14 

Age. Bingham Mine Formation ____ _ 55

Bingham Mine Formation, Clipper 

Ridge Member __________ 35, 53

Markham Peak Member, __ 38, 54 

Bimerfilcl Peaks

Formation _________ 8.'!, 51, 53 

('(tninia Zone _____________ 42

Krela Formation ____________ -48

Green Ravine Formation _____ /,2 

Kessler Canyon Formation ____ 48, 49

Lake Point Limestone ________ 14, ^5

Park City Formation, Grandeur

Member, _______________ 49

West Canyon Limestone ____ 27, 50 

Ameiira sp _____________^___ 47,52

Amplerizaplirentiii sp ______ 40, 41, 43,51

Amplextm sp _______________ 46,51

Amsden Formation _________ 41, 42

Anomplinlux sp _____________ 41

Antliracospirifer _______-_________ 45

occiiluus __________ 44, 45, 46, 51, 52

opimu* ___________ 45,46,47,52 

rocTtjimontanus ____ _,____ 44, 47, 51

sp ____________ 40, 43 

Antiqualonia ________ 41,42,45,48

coloradoensis _______ 25, 44, 47, 51

pernofloKa ________ _________ 40, 41

sp _____ 47, 53, 54 

Antler erogenic belt ____________ 57

Antler Peak, Nev _____________ 57

Antler Peak Limestone __________ 57 

Archimedes ___________________ 14,42,43

A returns Formation __________ 9, 50

Arrow Canyon Range __________ 55

Arthur fault __________________ 19 

Ascopora sp. A _____________ 46

sp. B __________________ 46,48 

sp ____ ________,_________ 52

Axtartella subquadrata __________ 49

sp ______________________,_ 54 

Atoka Formation _____________ 46

Aulopora sp ______________ 40,41

Ariculopecten sp __________ 41,49

B

Babj/lonite* _______________ 49

sp ______________ 49 

Rarboitria sp ________________ 45

Bates Canyon _______________ H, 14 

Bates syncline ___________,___ 14, 18 

Battle Conglomerate ___________ 57

Rai/lea sp _______________ 41, 43, 54 

ReecJieria boridens _______,44,49,52

sp ___________________ 41,43 

Relleroplton sp _______________ 43

Big Canyon ________________ 45, 48

Bingham Canyon ______________ 9

Bingham Mine Formation, Oquirrh

Group _______ 7, 9, 23, 33, 35, 50, 53

[Italic page numbers indicate major references]

Page

Bingham Mine Formation Continued 

Clipper Ridge Member, Oquirrh

Group ________ A23, 33,50, 53,55 

Markham Peak Member, Oquirrh

Group ______ 23, 33, 35, 50, 53, 55 

Bingham mining district ___ 4, 6, 7, 9, 33 

Bingham Quartzlte ______________ --- 6

Butterfleld Limestone member _ 6, 7 

Commercial Limestone member 6 

Highland Boy Limestone member 6 

Jordan Limestone member ________ 6

Lenox Limestone member 6 

Petro Limestone lentil ______ _ ____ 6

Phoenix Limestone lentil __ _ __ 6

Tilden Limestone lentil __ _ _ 6

Tampa Limestone member _ _ 6 

Bingham sequence _ _ __ _ 4, 7, 9, 11,

14, 18,21, 23,42, 45, 49, 50 

Bingham stock _ _ __ _ _ ___ 4

Bird Spring Formation __ __ _____ _ 55

Black Rock Canyon _________ 9,18,48 

Bloyd Formation, Trace Creek Shale

Member __ __ _______________ 46 

Borestux sp ____________________ _ __ 41

Bradiiina sp _______ ___ 53, 54, 67, 68 

Breathitt Formation, Kendrick Shale

Member _ ___ __ _ ____ _ ____ _ 46

Butterfleld Formation, Oquirrh

Group ___ __________ ____ 7, 27 ' 

Butterfleld Limestone member,

Bingham Quartzite __ ___ ______ 6, 7 

Butterfleld Peaks _________ ______ 27 

Butterfleld Peaks Formation,

Oquirrh Group ______ 7, 23, 24, 27, 50 

Biiftonia sp _ _ __ _ __ _ _ _ __ _ ___ 40

C

CancrineUa sp ___________ _ 47,49, 

C'aninia ____________ 10,33,37,40,41,

excentricn _ __ ____ _ __ _ _ __ 40,

tieradcnsis _ _ __ ____ ___ 40,

sp ________________ __ 43,46, 

Caninia Zone ___________ 11,40,41, 

Carbon Ridge Formation __________ 55,

Carlin Canyon ___ _______ _ __ ___

f'arlinin _ ___ _ ___ _____ __ ___ _ ___ _____

(liabolicrt _ _______________ __ 42,

pfiiUipai _ ______________ _____ 42,

Cedar Fort Member,

Oquirrh Formation _ __ _ _ _____

Chaetetes 4. ____________ 18,31,47, 

sp __ i.i ____________________ 46,

Chainman Shale _ _ ____ _ _ __ _ __

Cliainodictyon _ _ ___ __ _ ; _ _ ____

sp ___ _ ___________ ______ ,

CliaeicUa _ __ _ ____ _ ___ _ __ _ _ -_j._

sp _____________________ 4'8, 

Charleston-Nebo thrust plate u_ 

Chesterfield Range, Idaho _ __ __ _ _ -

Cfionetinella _ _ ____________________

nlata ____________________ 46,47,

si> ______________________ 

CladocJioniin sp __________________ _ _

Clrtdodtis sp __ _ _ ___ _ __ __ _ _ _ __

Clark County, Nev. ____ ___ _ _ ___

54

42

41

41

52

42

57

57

44

43

43

7

51

52

42

52

52

54

54

2

42

48

54

53

54

41

55

Page

Cleiothyrdina __ A41, 42, 47 

orbicularis ________ 44, 45, 46, 51, 54

siiblameUosa _____ 43

sp. A ___ 40 

sp _________________ 40,42,52 

Climacammina _ _ 69 

sp _________________ 53, 6T, 69 

Clinker Formation _ 9 

Clipper Peak ________- 38 

Clipper Ridge _______ 33 

Clipper Ridge Member, 

Bingham Mine Formation, 

Oquirrh Group ____ 23, 33, 50, 53, 55 

(*oeloconiis sp _______ 54 

Colpites sp _______- 43 

Commercial Limestone .member,

Bingham Quartzite _ _ 6 

Commercial marker bed , 33 

Composita _ __________________ 59

elongata ____________________ 52

orata ____________ __________ 46, 52

subtilita ______________ 47,48,49,52

sp ____________ 41,43,44,45 51 

Confusion Range __ 21, 42, 44, 45, 48, 48, 55 

Conger Mountain _____ ___ 42

Conical Hill ________ 57 

Conocardium sp 54 

Coon Canyon _________---__- --- 21

Coon Canyon syncline 21 

Coon Peak ________ 14, 18, 21 

Copper Gulch ________ -_- ____ 54

Correlation, Bingham Mine Formation _ 55 

Butterfield Peaks

Formation __________ 51, 52, 53 

Caninia Zone _______ ___ 42 

Brda Formation _________ 18. 48 

Green Ravine Formation . 4% 

Kessler Canyon Formation _ 21, 48 49 

Lake Point Limestone 14. 45 

Mississippian-Pennsylvanian

boundary 44 

Oquirrh Group 38 

Park City Formation,

Grandeur Member 49, 50 

West Canyon Limestone .. ______ 50

Coyote syncline ___ 14. 18 

Crurithijris planiconvexa _ 47, 48 54 

sp ___________________ 40,43 

Curry Formation ____ 9, 35 

Curry Peak sequence _ 3, 4, 9 

Cllpricardella gp ___ - 41 

Cypricardinia, sp _____ .___ 49, 51 

Cyrtorostra sp _ _ 49 

Cystodlctya ______________<-_, __ 41, 51

Jineatn ________ _ 41

sp. A ______________-__- 40 

sp. B ___________ , 40

D

crassa __________________ 46

sp ____________ 45, 48, 49,52^54

nesmoinesia _ __.______ _ 48 

ingrata ____±._ ___- '__ _^_i 46 

muricatina _______ 17, 47, 48, 51, 52
A74 INDEX

Page

Diamond Creek Formation A9, 57 

Diamond Creek Sandstone 9, 38 

Diamond Peak ___ 57 

Diamond Peak Formation ____ 57 

Diaphragmiis ________- ___- 42

cestriensis __ - 40,42

n. sp ___ 44

Diploporaria ___________________ 52

sp ___________________ 46, 52 

Ditomopyge sp 54

Donaldina sp ________________ 49 

Doughnut Formation _______ 11, 14, 42 

Douglass, R. C.,

fusulinid identifications _________ 66 

Dry Canyon _ _______ _______ 35 

Dyoros sp _________ _____ _ 49

B

East Tintic Mountains ________ 38, 42 

Echinaria sp ________________ 47

Echinoconchus ______________ 45

rodeoensis ________________ 40

sp. A ___________________ 51

sp _ __ _ ________ 44 

ElliotteUa _________________________ 50

sp. A ______________________ 51

Ely Limestone _______ 9, 44, 45, 55, 57 

Ely mining district _____________ 55 

EnaUopora sp ________________ 43 

EoUssochonetes sp __________ 46, 52 

Eotrochtis sp ________________ 43 

Erda Formation,

Oquirrh Group _____ 9, 11, H, 33, 39, 

46, 49, 50,51,52, 53

Erldopora sp ________________ 43

Euphemites n. sp ______________ 49

sp __ ______ 43, 47, 54

Eureka mining district, Nev _______ 55

F

Fenestella _________________________ 41

austini archimediformis _________ 54

serratula __________________ 46

(Cervella) cruciformis ___________ 54

(Polyporella) sp ____________ 54 

sp 40, 43, 46, 51, 52, 53 

Ferguson Springs Formation ______ 55 

Ferguson Springs Mountain, Nev ____ 55 

Fistulipora sp ________________ 51 

Fleataria ________________ 45, 66

sp. A _______________ 42, 43, 50 

sp. B __________________ 44, 51 

sp ___________ 40,42, 45, 47,52 

Fossils, Big Canyon ____________ 45 

Bingham Mine Formation,

Clipper Ridge Member ____ 35, 53 

Markham Peak

Member _____ 36, 38, 53, 54 

Butterfleld Peaks

Formation _______ 33, 51, 52, 53 

Caninia Zone ______________ 41 

Confusion Range __________ 21 

Erda Formation ___ 16, IS, 46, 47, 48 

Kessler Canyon Formation _ 21, 48, 49 

Lake Point Limestone ______ 13, 14 

Park City Formation,

Grandeur member _______ 23, 49 

post-CflM/Hi'a Zone _ ________ 42

preservation _____ _ 39

West Canyon Limestone ___ 26, 50 

Fourmile Canyon _____________ 23 

Fusulina _______________________ 48, 52

sp ____________ 48, 51, 52, 67, 68 

FusulineUa __________________ 47, 51

sp _________________ 52, 67, 68 

Fusulinid collecting localities ______ 66

Page

6

Garfleld fault __________ A18, 22 

Geologic setting _____ 2 

Glabrocing ulum sp ____ 49 

Gold Hill region, Utah _______ 55 

Goniasma sp _____________ 47 

Gosseletina sp _________ _ 41 

Grandaitrispina sp _______ 49 

Grandeur Member,

Park City Formation __ 9,10.27,40,49

Granite Mountain, Utah __________ 42

Great Basin _____ 2, 7, 42, 44, 47, 55, 57

Great Blue Limestone ________ 6, 11, 42

Long Trail Shale Member ______ 42

Paymaster Member _________ 42

Green Ravine _______________ 10, 14

Green Ravine Formation __ 9, 10, 11, .39, 40

H

Hall Canyon Member,

Oquirrh Formation ____________ 7 

HedereUa sp _____________ 45, 51, 52 

Heteralosia sp ____________ 40, 49 

Highland Boy Limestone member,

Bingham Quartzite ___ 6 

Hitatedia mormoni ________ 47, 54

sp _______________ 40,44,49,51 

Hystriculina __________ __ 48

sp _______________ 46

Ichthyorachi* ___________________ 48

sp _________________ 40,47,52 

Inflatia ____________________________ 42

sp. A __________________ 42, 43 

sp. B __________________ 42,43 

n. sp _________ _ 44 

sp __________________ 40, 47 

Introduction __________________ 1

Jordan Limestone member,

Bingham Quartzite ___________ 6 

Jordan marker bed __________ 7, 27, 33 

Juresania _____________________ 47

sp ___________________ 44, 52

K

K zone, Monroe Canyon Limestone ___ 42 

Kaibab Limestone _____________ 49 

KanttaneUa _______________ 69

sp _______________ 53, 69 

Keiidrick Shale Member,

Breathitt Formation __ 46 

Kessler anticline _______ 10, 11, 14, IS 

Kessler Canyon _________ _ 9, IS. 54 

Kessler Canyon Formation,

Oquirrh Group ___ 9, 11, 14, 18 22, 38. 

39, 47, 50, 54, 55

Kessler Peak ____________ 10, 11, 14 

Kirkman Formation ___ 9 

Kirkman Limestone ___ 9 

Knightites (Retispira) sp _____ 43, 54 

Kochiproductus ___ 48, 54 

peruvianmt __________ 48,49,54

Kozlowftkia _______ 51

haydenensis _____ 46, 47, 48, 51, 52, 53

splendens __ 54 

sp ____________ 47

Krotoria wallaciana _____ 49

sp _____ 54

Page

Laeridentalium sp _ A43 

Lake Point __ _ 11, 14 

Lake Point Limestone, Oquirrh

Group _____ 9, 10, 11, 16, 26, 39, 42, 50 

Lake Point Ridge ____ 11, 14 

Lake Point thrust fault ________ 14 

Lark _______________ 38,53,54,55 

Last Chance stock 4 

Left Hand Fork of Middle Cannon ___ 27 

Lelorltynchuis carboniferum __________ 40

Lenox Limestone member,

Bingham Quartzite ___________ 6

Lept-agonia sp __________________ 40

Lewiston Peak _______,____ 7, 23, 24 

Lewiston Peak Member,

Oquirrh Formation ____________ 7 

Limipecten sp _________________ 51 

Lincoln County. Nev. _ ________ 55 

Li no pro duct us _______ ______ 45, 59

nodosus _____________ 45,46,50,51

prattenianus ________________ 47, 52

sp. A _________________ 44, 51

sp. B _____________________ 44

sp ____________ 46,48,52,53,54

LiosoteUa __________________________ 49

sp. A _____________ ___ 49 

Lissoclionetes sp _____ _ 49 

Lithology, Bingham Mine Formation,

Clipper Ridge Member _____ 33 

Bingham Mine Formation,

Markham Peak Member ___ 35 

Butterfield Peaks Formation ___ 28 

Erda Formation _ _____ 14, 16

Green Ravine Formation ___ _ 10 

Lake Point Limestone ______ 11, 12 

Kessler Canyon Formation __ 18, 19 

Park City Formation,

Grandeur member _________ 22

West Canyon Limestone _______ 24

Lithophagus sp ___ _ ________ 41

Litltoxtrotion ________________ 36 

8telcki _____________________ 40, 41

Little Valley __________________ 21 

Little Valley syncline ___________ 21 

Little Valley Wash ______________ 18 

Long Ridge anticline _______ 23, 27, 33 

Long Trail Shale Member,

Grout Blue Limestone _______ 42 

LophophyUidium. sp _ 43

M

Magoffln Beds _____________ 46 

Manning Canyon _____________ 23 

Manning Canyon Shale _ 7, 9, 11, 14, 23,

27, 42, 45, 50

Maple Formation, Oquirrb Grcup __ 7,27 

Markham Peak ____ _ _____ 35, 38

M;irkham Peak Member, 

Bingham Mine Formation, 

Oqtiirrh Group ___ 23, 33, S5, 50, 53, 55 

Martinia sp ___ _ 40 

Matlieropora _ 52 

sp ________ __ 52 

Mendmv Canyon Member,

Oquirrh Formation _ 7 

Meekella striatocostata ______________ 46

Meekospira sp ___________ 43, 49, 54

Megafaunal collecting localities 57

Megafossils, Bingham Mine Fcrmation,

Clipper Ridge Member 35, 53

Butterfield Peaks Formation __ 51, 52

Erda Formation ___ __ 46, 47, 48

Kessler Canyon Formatter 48
INDEX A 75

Page

Mcgafossils Continued 

Park City Formation,

Grandeur Member _ A49

West Canyon Limestone _ 51

Megousia _______________ 49

sp. A _________ _ 49

Mercur mining district _ 5, 6 

Mesolobus __________________ 48

eiiampygus _____________________ 47

Michelinia sp _______________ 54

Microfossils, Bingham Mine Formation, 

Clipper Ridge Member _______ 35, 53 

Bingham Mine Formation,

Markham Peak Member __ 38, 53, 54

Butterfleld Peaks Formation _ 51, 52

Erda Formation _______ 46, 47, 48

Kessler Canyon Formation ___ 48, 49

Midas thrust fault ____ 2, 4, 7, 9, 23, 35

Middle Canyon ______________ 27, 33

MiUerella _______________________ 27, 50

sp _______________ 53, 69 

Mills Junction syncline __________ 14 

Mount Raymond sequence __ 11, 14, 18, 21 

Multitfiecopora ________________ 41,47,51

n. sp _____________ 40

sp. A _________________ 46, 52

sp. B ____________________ 46

sp ______________ 46

Multithecopora zone __________ 47, 51

Myalina sp ___________ 47, 51

N

Naticopsis (Naticopsis) sp _________ 54 

sp ___________________ 41,43

Neilsonia ______________________ 48

sp ___________________ 41, 47 

Nelson Peak _______________ 11, 14 

Neochonetes granulifer ________ 47, 48, 54

Neophricodothyris sp. A _________ 49 

Neospirifer ________________________ 51

cameratus __________________ 44, 45

coJoradoensis ______ 46, 47, 48, 51, 52

sp ___________________ 47, 54 

North Oquirrh thrust fault __ 2, 3, 9, 11,

14, 18, 22

Nttcleospira sp _______________ 41 

Nucttlopsis (Nuculanella) sp ______ 49

O

Occidental fault ______________ 35 

Omphalotrochus ______________ 48, 54

obtvsispira __________ 54

wolfcampensis ____________ 48, 54, 55

assemblage, Bingham Mine

Formation ___ 54, 55 

Kessler Canyon

Formation _______ 48, 54 

Ophir anticline _______________ 23 

Ophir Canyon ________________ 23 

Ophir mining district _______ 4,11, 23 

Oquirrh Formation __ 2, 5, 6, 7, 9, 11, 14,

18, 23, 50, 55

Cedar Fort Member __________ 7 

Hall Canyon Member ________ 7 

Lewiston Peak Member _______ 7 

Meadow Canyon Member ______ 7 

Pole Canyon Member ________ 7 

Sandy Oquirrh member 7 

West Canyon Limestone

Member ______________ 7, 23 

Oquirrh Group ___ 2, 7, 9, 10, 11, 22, 23,

39, 45, 46, 50

Bingham Mine Formation _ 7, 9, 23, 

33, 35, 50, 53

Clipper Ridge Member _ 23, S3, 

50, 53,55

Page

Oquirrah Group Continued

Bingham Mine Formation Continued

Markham Peak Member __ A23, 33, 

35, 50, 53, 55

biostratigraphy ________ 38 

Butterfleld Formation ______ 7, 27 

Butterfleld Peaks Formation __ 7, 23,

24, 27, 50

Erda Formation ___ 9, 11, Ik, 33, 39, 

46, 49, 50, 51, 52, 53

Kessler Canyon Formation _ 9, 11, 14,

18, 22, 38, 39, £7, 50, 54, 55

Lake Point Limestone __ 9,10,11,16,

26, 39, 42, 50

Maple Formation __________ 7,27

West Canyon Limestone _ 7, 23, 27,

44, 45, 46, 50

White Pine Formation ______ 7, 27 

Orbiculoidea _______________________ 22

sp ______________________ 52 

Orthonema soc.oroense ____________ 49

Orthotetes occidentaUs _ 40

sp ___________________ 43,51

Orygmopliylhim _____ 13, 42, 44, 45, 62, 65

sp ___________________ 43

Ovatia sp. A _____________ 40,42, 43

sp. B _______________ 40,43

Paladin sp ______________ 43,44, 51 

Paleostylus (Pseudotsygopleura) sp __ 41

sp ____________________ 43 

Parallelodon politiis ___ 49

sp _ ___ 47 

Park City Formation _______ 9, 21

Grandeur Member 9, 10, 21, 40, £9 

Parnell marker bed 33 

Paymaster Member,

Great Blue Limestone _ 42 

Penniculauris __________ 49

bassi ____________________ 49

Penniretepora ______ 41

sp __________ 40, 46, 47, 52, 53, 54 

Pennsylvanian, Middle Pennsylvanian

unconformity _ 21, 55

Mississippian. Pennsylvanian

boundary 44 

Pentremites n. sp _ 44 

Peruvispira _______ 48, 54

sp __________ 54 

Petro Limestone lentil,

Bingham Quartzite 6 

Phoenix Limestone lentil,

Bingham Quartzite 6 

Phricodothyris perplexa _______ 47, 52, 54

Platyceras sp 47 

Pleurotomariacea sp 43 

Pole Canyon Member,

Oquirrh Formation 7 

Pole Canyon syncline 27 

Polidevcia sp _ 49 

Polypora ___ 41

andina _______ 54

sp ______ 40, 43, 46, 51, 52, 53, 54 

Polyporella sp __ 43,46 

PortlocMella sp ______ 41 

Post-Caninia Zone __ H. 40, 42 

Pre-Caninia Zone H> 40 

Prismopora __________ 17, 31, 48, 52, 53

triangulata ______ -- 47, 48

sp __-______ - - 47, 52 

Profusulinella ______ 17,47,48,51,66

Profusulinella-Chaetetes faunizone 47 

Promarginifera n. sp 40,41 

Promytilus sp ____ 41 

Provo Canyon ______ 45, 50

Pseudofusulinella ___________ A66

Sp __________________ 38 70 

Pseiidosdiwagerina ________________ 38

Psilocamara sp 40 

Ptylopora sp ___ 54 

Pugnoides quinqueplecis __________ 44,51

Punctosplrifer TcentucUensis _______ 47,48

transversus ____ 40, 44. 45

sp _________ 44, 54

B

Ramiporalia sp ___ 4 , 54 

Rayonnoceras excentricum ___________ 41

Reference section, Butterfleld

Peaks Formation ___ 27, 31, 50, 51. 52

Park City Formation,

Grandeur member 22

West Canyon Limestone,

at Soldier Canyon _ 23, 24, 25, 2T, 50

at West Canyon 23, 24, 25,

27, 50

Retaria sp ____ 4f, 54 

Reticulariina ____ 42

campestris __ 40, 41, 42, 44, 45, 46 51

sp ______ 54 

Reticycloceras sp ____ 43 

Rhabdomeson ___________ 46", 52

sp ____________________ 47, 52 

RMneoderma pealeana _ 41

sp _________________ 43 

Rhipidomella carbonaria ___________ 48

nevadensis _____ 13,14,42,43,44,45

Zone ___________ 14, 42, 45

RJiombocladia ________________ 52

sp ____________ 46,47,52,53,54 

Rhombopora sp ________________ 47 

Rhomboporella sp _____________ 54 

RJiombotrypella sp ________ 46, 47, 52 

RJiynchopora taylori ________________ 49

sp _________________ 46, 47, 54 

Riepe Spring Limestone __________ 55 

Road Canyon Formation __________ 49 

Rocky Mountains _______________ 42 

Rogers Canyon S, 14 

Rogers Canyon sequence _ 3, 9,26, 33 38,

39, 53, 55

Round Valley Limestone _______ J* 14 

Rugoclostus ___________ 14, 26, 42, 4F, 50

semistriatus __________ 43, 44, 4ff, 51

sp _____________ 46,47

Zone ____________14, 26, 42, 4F, 50 

Ruaosochonetes ____________________ 42

pseudoliratus ___________________ 43

sp 40

8

Salt River Range, Wyo ___________ 42 

Sandy Oquirrh member,

Oquirrh Formation ____________ 7

Schell Creek Range, Nev _________ 55

Schizophoria resupinoides _________ 43

texana _________________ 43

sp ______ 40, 43, 51

Schuchertella ________________ 42

sp. A __________________ 43

sp ___________________ 40

Schwayerina ______ _ _______ 38

Scoloconcha sp _ 43 

Septopora sp _________ _ 47, 52, 54 

Settlement Canyon __________ 27,38 

Slnuatina sp _________________ 54 

Soldier Canyon ______ 23, 27, 39, 4«J, 50 

Soldier Creek ________________ 50 

South Mountain __ 3, 5, 7, 9, 33, 38, &*, 55
A76 INDEX

Page

Spirifer __________________ A59 

'brazerianus ________ 40, 42, 43

Spirorbis sp _____ ___ 40, 46, 54 

Rpiroscala sp __-_ ___ 41 

Spring Canyon _ _ _ 35 

Spring Mountain, Nev _________ 55

Spruce Mountain, Nev ______ _ - 55

StegoeoeUa sp _____________ 41,43 

Stenopliragmidium sp ______-__ 40 

Sterostylus sp ________________ 46 

Stockton mining district ______ _ 4 

Straparolus (Amphiscapha) sp ______ 44 

Strathearn Formation 57 

Stratigraphic terminology, recommended 

change 5

Stratigraphy, revised Upper Paleozoic 9 

Streblopteria sp ___ 49 

StreWotrypa sp ___ 46, 52 

Strobeus ,sp _____ _ 43 

Strophostylus sp ___ 43, 54 

Sulcatopinna sp _ 43 

 Syringopora __ _ 33 

multattenuata _________-_ _ 53

Tabulipora ______________________ 41, 48

sp. A ____________________ 46

sp. B ___________________ 46

sp ______________ 40, 43, 51, 52

TJiamnisQUs sp _____-_________ 40

Thickness, Bingham Mine Formation __ 33

Bingham Mine Formation. Clipper 

' - Ridge Member _______ 33, 34, 35

Page

Thickness Continued

Bingham Mine Formation Continued

Markham Peak Member _ A33, 35, 

36, 37, 38

Butterfield Peaks Formation __ 27, 28,

29, 30, 31, 32, 33

Caninia Zone ________________ 41

Erda Formation _____ 14, 16, 17, 18 

Green Ravine Formation _____10, 11

Kessler Canyon Formation _ 19, 20, 21 

Lake Point Limestone __ 11, 12, 13, 45 

Park City Formation, Grandeur

member, _____________ 22,23 

West Canyon Limestone __ 24, 25, 26 

Tilden Limestone lentil, Bingham

Quartzite ___________________ 6 

Timanodictya ___________________ 49

sp ___________________ 49

Timpanogos sequence _ 9, 14, 18, 21, 45, 55 

Tomera Formation _____________ 57

Tooele Valley ________________ 55 

Trace Creek Shale Member, Bloyd

Formation _________________ 46

Traverse Mountains ____________ 5

Trepospira (Trepospira) sp ________ 43 

Triticites _____________ 35, 38, 48, 49, 53,

54, 67, 68, 69, 70

sp _______ 38, 53, 66, 67, 68, 69, 70 

Type section, Bingham Mine

Formation _____ _ 33, 55 

Bingham Mine Formation, Clipper 

Ridge Member __________33, 53 

Markham Peak Member __ 36, 37,

55 

Bingham sequence _ 9

Page

Type section Continued

Butterfield Peaks Formation __ 28,

50,51

Erda Formation ________ A14, 16 

Green Ravine Formation _ 10 

Kessler Canyon Formation A18, 19 

Lake Point Limestone ______ 11. 12 

Oquirrh Group ___________ _ 9 

Rogers Canyon sequence 9

U

Uddenitfs _________________________ 48

T'ddenites Zone ___________________ 48

W

Waagenoconcha _____________________ 48

Wasatch Range ______ 2, 7, 9, 11, 18, 21, 

22, 42, 45, 50, 55

Weber Quartzite ______ 9, 18 

WedekindeUina __________________ 48, 67

sp __________________ 52, 67 

WellereUa sp __________ - 49 

West Canyon ________ 7, 2?, 24, 27, 50 

West Canyon Limestone, Oquirrh

Group ________ 7, 23, 27, 44, 45, 46, 50 

West Canyon Limestone Member,

Oquirrh Formation _______ 7,23 

White Pine Formation, Oquirrh

Group ________-___ - 7,27 

Wilkingia sp _______________ 51 

Worthenia sp ___________ _ 49

Yampa Limestone member, Ringham

Quartzite ___________________ 6 

York-Phoenix marker bed _________ 33

U.S. GOVERNMENT PRINTING OFFICE: 1970O-384-354