Geology and Ground-Water Resources of Laramie County Wyoming

GEOLOGICAL SURVEY WATER-SUPPLY PAPER 1834

Prepared in cooperation with the Jf^yoming State Engineer

VER RESOURCES

Geology and Ground-Water Resources of Laramie County WyomingBy MARLIN E. LOWRY and MARVIN A. CRIST

With a section onCHEMICAL QUALITY OF GROUND WATERAND OF SURFACE WATERBy JOHN R. TILSTRA

GEOLOGICAL SURVEY WATER-SUPPLY PAPER 1834

Prepared in cooperation with the Wyoming State Engineer

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1967

UNITED STATES DEPARTMENT OF THE INTERIOR

STEWART L. UDALL, Secretary

GEOLOGICAL SURVEY

William T. Pecora, Director

Library of Congress catalog-card No. GS66-309

For sale by the Superintendent of Documents, U.S. Government Printing Office Washington, D.C. 20402

CONTENTS

Page

Abstract__ __-__________-_______________-____--__--_--_--------- 1Introduction. _____________-__________-_________--__-__--_--------- 2

Purpose and scope of the investigation.__________________________ 2Location and extent of the area.______________________---------_ 3Well-numbering system._____________________________--_------- 3Previous investigations..________________________-_____-_--_---- 3Acknowledgments ____________-__________-________--__--_--_-_- 4Landforms and drainage___-___-__________-__-___-_---__-_---_-- 5Climate._______________________________--_--_____--__-_---__- 6

Geology...__-___--_-_--_----__---_--__---__-_--_---_--_--------_- 7Rocks of pre-Tertiary age.________________________--__---_--__- 7Rocks of Tertiary age._________________________________________ 13

White River Formation_________________-_-________-_-___-_ 13Arikaree Formation______________________________________ 13Ogallala Formation._______________________________________ 16

Rocks of Quaternary age_-__-----------_--__-----_------------- 18Alluvium. _ ______________-_________-___-_._______-_-----_- 18

Terrace deposits______________________-____---------- 19Flood-plain deposits.__________________________________ 20

Ground water_____________________________________________________ 20History of development-____________-_______-__--_____--__----- 20Principles of occurrence._______________________--____--_------_ 22Hydraulic properties of the principal aquifers.____________-----__- 24

White River Formation-____________-___-_________-__----__ 25Arikaree Formation.-_________________________-_-_---_--.-__ 28Ogallala Formation._______________________________________ 30

Pumping tests____________________-________----_--__- 30Idealized aquifer.__________________-___-__------_---_- 32

Alluvium_ ________________________________________________ 38The water table-______________________________________________ 39

Configuration. ____________________________________________ 39Fluctuation. ______________________________________________ 41

Recharge.____________________________________________________ 45Discharge. ___________________________________________________ 46Future development.__________________________________________ 48

Chemical quality of ground water and of surface water, by John R. Tilstra_ _ 50Chemical characteristics of water._______________________________ 50Classification of water use._____________________________________ 50

Domestic use_____________________________________________ 50Industrial use.____________________________________________ 51Irrigation_ _ _ ____________________________________________ 51

Quality of ground water________________________________________ 55Quality of surface water________________________________________ 57

Records of selected wells and springs_______________________________ 58References cited___________________________________________________ 69

nr

IV CONTENTS

ILLUSTRATIONS

Page PLATE 1. Geologic map.__________________-__-____--___----_-_ In pocket

2. Hydrologic map______________________--______------- In pocketFIGUEE 1. Index map showing areas described in this report and in earlier

ground-water reports on Laramie and nearby counties_____ 42. Diagram showing well-numbering system__________________ 53. Photograph showing fractured siltstone of the White River

Formation.___________________________-_-__----_-_--_ 144. Photograph showing a clastic dike in the White River For­

mation. _______________________-_-______-------_-_--- 155. Sections across Lodgepole Creek valley.___________________ 216. Graph showing sources of Cheyenne municipal water supply

and annual usage.________________-__-_-____---__----- 237. Photograph showing a pipe in White River Formation_______ 278. Graph showing specific capacity frequency of wells in the

Arikaree Formation,__________________________________ 299. Contour map and section showing decline of the piezometric

surface.-_______--______---______---_-__--_----_-_--_ 3310. Graph showing relation of water levels to pumpage in Cheyenne

well field_____________________________________________ 3411. Map showing polygon network used to estimate change in

ground-water storage________________________________ 3712. Map showing configuration of top of White River Formation

and saturated thickness of terrace deposits.._____________ 4013. Hydrograph showing water-level fluctuations in a well tapping

the Arikaree Formation______________________________ 4214. Hydrograph showing seasonal fluctuations of water levels in

areas of heavy pumping.______________________________ 4315. Hydrograph showing long-term trend of water levels in areas

of heavy pumping-___________________________________ 4416. Diagram showing classification of irrigation water___________ 56

TABLES

TABLE 1. Summary of stratigraphic units and their water-bearing charac­ teristics. ______________________________________________

2. Aquifer coefficients of the Ogallala Formation as determined from pumping tests_______-_-_____--_-____-_____-_______

3. Chemical analyses of ground water.________________________4. Chemical analyses of surface water.________________________

Page

315254

GEOLOGY AND GROUND-WATER RESOURCES OF LARAMIE COUNTY, WYOMING

By MARLIN E. LOWRY and MARVIN A. GRIST

ABSTRACT

Laramie County, an area of 2,709 square miles, is in the southeast corner of Wyoming. Rocks exposed there range in age from Precambrian to Recent. The most extensive aquifers in the county are the White River Formation of Oligocene age, which is as much as 500 feet thick and consists predominantly of siltstone; the Arikaree Formation of Miocene age, which consists of as much as 450 feet of very fine grained to fine-grained sandstone; and the Ogallala Formation of Miocene and Pliocene age, which consists of as much as 330 feet of gravel, sand, silt, and some cobbles and boulders. These formations are capable of yielding large supplies of water locally. Terrace deposits of Quater­ nary age yield moderate to large supplies of water in the southeastern and northeastern parts of the county.

In the Federal well field, large yields of water from the White River Forma­ tion are obtained from gravel lenses. In the eastern part of the county near Pine Bluffs, large yields are obtained from openings in the siltstone of the White River. Previous investigators reported that the large yields were ob­ tained in areas where the formation is fractured and fissured. The authors of this report believe that the large yields from siltstone in the White River Formation are from pipes, sometimes called natural tunnels, rather than from fractures or fissures.

Little is known about the water-bearing properties of the pre-Tertiary aqui­ fers in the county, but water derived from the pre-Tertiary formations would probably be of poor quality, except in the vicinity of the outcrop near the west­ ern edge of the county.

Precipitation is the principal source of recharge to the ground-water reser­ voirs. About 5 percent of the annual precipitation, or about 108,400 acre-feet per year, is estimated to be recharge. Only a small amount of additional re­ charge is from streams. The general movement of ground water is eastward, and the average gradient of the water table is about 40 feet per mile.

The total amount of ground water pumped from wells in Laramie County during 1964 is estimated to be 28,000 acre-feet; about 6,000 acre-feet was used for municipal and industrial supplies, about 17,000 acre-feet was used for irrigation in the Pine Bluffs-Carpenter area, and about 5,000 acre-feet was used for other purposes. The balance of the recharge (80,400 acre-feet) is estimated to be discharged by the following means: 20 percent by underflow, 20 percent by streamflow, and 60 percent by evapotranspiration.

The coefficient of transmissibility of the Ogallala Formation, determined by averaging data from 28 pumping tests made in the Cheyenne municipal well

2 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

field, is about 16,000 gallons per day per foot. However, this figure is an average of the more permeable zones, and the average coefficient of transmissibility of the Ogallala in the county is probably much less because of the heterogeneous character of the formation. A coefficient of transmissibility of 3,800 gallons per day per foot was calculated for the Ogallala, in the same vicinity that the pumping tests were made, by using a regional method of analysis. Although the average transmissibility of the Ogallala is considered to be low, large yields are obtained from gravel stringers and lenses in the formation. The maximum perennial yield from the Cheyenne well field is estimated to be about 1.6 billion gallons per year.

Moderate to large yields of water can be obtained in the north-central part of the county where the saturated thickness of the Arikaree Formation, or com­ bined Arikaree and Ogallala Formations, is 200 feet or more.

Ground water has been developed throughout the county, but development has been intensive only in the Cheyenne municipal well fields near Cheyenne and Federal and in the Pine Bluffs lowland. The water level has been lowered as much as 40 feet in the Cheyenne well field and somewhat less in the Federal well field.

Interference between wells occurs in the Pine Bluffs lowland during the summer, when pumping is at a maximum, and additional development will aggravate the interference. At the present rate of development, no permanent lowering of the water table is likely to occur in this area in the near future; however, a great amount of additional development could possibly cause perma­ nent lowering of the water table.

The chemical quality of water from the principal aquifers and streams is generally suitable for domestic, irrigation, and industrial uses. The water is predominantly of a calcium bicarbonate type and is very hard; its dissolved- solids concentration ranges from 167 to 688 parts per million. The chemical composition of water from the White River, Arikaree, and Ogallala Formations, and from the alluvium is generally similar, although small local differences are apparent within the formation. Comparison of older data with recent data indicates that water from the alluvium in the Pine Bluffs vicinity has increased in mineralization as a result of irrigation.

INTRODUCTION

PURPOSE AND SCOPE OF THE INVESTIGATION

Laramie County is one of the principal areas of ground-water development in the State, and many reports on ground-water condi­ tions in the area have been written. The purposes of this investigation were to consolidate and update existing data, to determine the effect of the development of ground water on the hydrology of the area, and to study the hydraulic properties of the aquifers in order to better understand the relation between aquifers and the extent to which additional water can be developed from them.

The investigation was started in the winter of 1964 as part of the program of the U.S. Geological Survey in cooperation with the Wyoming State Engineer. The ground-water study was under the supervision of E. D. Gordon, district geologist of the Ground Water

INTRODUCTION '6

Branch of the Geological Survey. The quality-of-water study was under the supervision of T. F. Hanly, district engineer of the Quality of Water Branch of the Geological Survey.

LOCATION AND EXTENT OF THE AREA

Laramie County occupies the southeast corner of Wyoming (fig. 1). Almost rectangular, it covers 2,709 square miles.

WELL-NUMBERING SYSTEM

Water wells, springs, and test holes cited in this report are numbered according to the Federal system of land subdivision (fig. 2). The first numeral of the number indicates the township, the second the range, and the third the section in which the well, spring, or test hole is lo­ cated. The lowercase letters following the section number indicate the position of the well in the section. The first letter denotes the quarter section, the second letter the quarter-quarter section, and the third letter the quarter-quarter-quarter section (10-acre tract). The sub­ divisions of a section are lettered a, b, c, and d in a counterclockwise direction, starting in the northeast quarter. If more than one well is listed in a 10-acre tract, consecutive numbers starting with 1 are added to the well numbers.

PREVIOUS INVESTIGATIONS

Darton, Blackwelder, and Siebenthal (1910) mapped in detail the geology of the western part of the county as far north as lat 41°30'. Newhouse and Hagner (1957) mapped the Precambrian rocks in the northern part of the county, and Denson and Banks (written commun., 1965) mapped the Tertiary formations throughout the county. Mas­ ter's theses by Gray (1946), Haun (1948), Brady (1949), Hammond (1949), and McGookey (1952) describe the geology along the east flank of the Laramie Range.

Several water-supply papers and circulars that cover parts of the area have been published by the U.S. Geological Survey. These are by Adams (1902), Meinzer (1917), Babcock and Rapp (1952), Rapp, Warner, and Morgan (1953), Babcock and Bjorklund (1956), and Bjorklund (1959). In addition, reports by Cady (1935), Theis (1941), Foley (1943), and Morgan (1946) have been placed on open file by the U.S. Geological Survey.

Other reports on ground-water conditions in the county include re­ ports by the Wyoming Geological Survey (Knight and Morgan, impub. data, 1936, 1937; Dockery, 1940) and reports by the U.S. De­ partment of Agriculture (Burleigh and others, 1938; U.S. Dept. Agriculture, 1940).

GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

106° 104°

42

KIMBALL l c CHEYENNE O

50 MILES

FIGURE 1. Areas described in this report and in earlier ground-water reports on Laramie and nearby counties. Numbers on map refer to U.S. Geological Survey reports listed below. Type of publication identified as follows: WSP, water-supply paper; Circ., circular.

1_ - . - WSP 943..- ______ Wenzel, L. K., Cady, R. C., and Waite, H. W____________ 19462_____________. Cire. 126............... Babcock, H.M., and Visher.F.N.---.__-- .--_-_____ 19513_.____._______ WSP 969...._._.__.____ Cady, R. C., and Scherer, O. J.....-_-_____.--__._______- 19464.............. Circ. 156............... Babcock, H. M., and Visher, F. N._...... . ..... 19525.............. WSP 1410.-.. . Bjorklund, L. J.. ... 19576.. . -. WSP 1791.-... Welder, G.E.,andWeeks,E.P 19657...-------- Circ. 163.--------. Rapp, J. R., and Babcock, H. M...________________ 1953o /WSP 1783-.-._____--___ Weeks, E.P 19648 . | Cire 70..______________ Littleton, B. T.... . .. 19509 .____._-__ WSP 1490-.. Babcock, H.M., and Morris, D. A.... -.- 196010 WSP 1377-__.-______.._ Rapp, J. R., Visher, F. N., and Littleton, R. T..._______ 195711 .___...-_.. Circ. 238-.. Visher, F. N., and Babcock, H. M..__________________ 195312 ________ Circ. 162... ......... Babcock, H. M., and Rapp, J. R 195213 WSP 1483--- - Bjorklund, L. J. 195914._.._._______ WSP 1140...___________ Rapp, J. R., Warner, D. A., and Morgan, A. M...- ... 195315...___.__-___ WSP 1367----- Babcock, H. M., and Bjorklund, L. J.,... ......... 195616... WSP 1809-L .____._. Weist, W. G., Jr..-- 196517 ------- Circ. 80.- Littleton, R.T.......................................... 1950

ACKNOWLEDGMENTS

The writers appreciate the cooperation of Pure Oil Co., Shell Oil Co., and local water-well drillers who furnished logs of holes drilled in

INTRODUCTION

T. 16 N.

RANGES, WEST 72 71 70 69 68 67 66 65 64 63 62 61 60

17

16

£ 15

0 14 z.</> ' 3a.x 12

1"O

2

1/

P

//

V/

/

o /

/

£ <Oor

z_l <Q.

O 7.K. Q.

I HX(/)

BASE LINE

Well 16-67-15ddd

R.67W. / Sec. 15

18

19

30

31

17

20

29

32

16

21

28

33

10

15

22

27

34 35

FIGUEE 2. Well-numbering system.

the area. Many well owners in Laramie County supplied information on their wells and gave permission for various measurements and tests. The writers are especially indebted to Mr. Kay Sherard, superintend­ ent of the Cheyenne Water Department, for his cooperation during the pumping tests in the municipal well fields; to Adolpho K. Hanke, trainee from Brazil, who assisted during the pumping tests; and to L. J. McGreevy, of the U.S. Geological Survey, whose 'assistance in this study is greatly appreciated.

LANDFOBMS AND DBAINAGE

Laramie County includes parts of the Southern Kocky Mountains and Great Plains physiographic provinces. The Laramie Range, which extends along the western edge of the county, is part of the

6 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

Southern Eocky Mountains. The mountain surface in many localities has been reduced to a relatively uniform plain that slopes gently east­ ward and is nearly smooth in gross appearance. The surface in other localities, however, is rough and irregular, and is broken by steep-sided valleys several hundred feet deep and by rugged mountain peaks.

North of Crow Creek, ridges of resistant sandstone and limestone form a line of foothills along the mountain front. South of Crow Creek, Tertiary deposits form a gradual slope from the mountains to the plains. This gradual slope, the "gangplank," is utilized by U.S. Highway 30 and the Union Pacific Railroad to gain access to the mountain uplands with the least possible grade.

The area east of the mountains lies in the High Plains section of the Great Plains physiographic province. The central part of the area is a high eastward-sloping surface underlain by Tertiary sediments. Gradients range from 100 feet per mile on the "gangplank" to 20 feet per mile near Albin, Wyo., at the eastern edge of the county. This surface has a gently rolling topography of only moderate relief and is marked by ephemeral and intermittent streams.

The high central area is nearly surrounded by escarpments. An escarpment extends northward from Granite Canyon along the east side of Federal and Chugwater Creek valleys; the Goshen Hole and related escarpments bound the north side of the area; and to the south, in Colorado, an escarpment that nearly parallels the Wyoming- Colorado State line extends eastward from the mountains. Two em- bayments extend into Wyoming from Colorado, one at Warrenton and a more extensive one in the Pine Bluffs-Carpenter area.

The county is drained by small eastward-flowing streams. Chug- water, Bear, and Horse Creeks are part of the North Platte Eiver drainage, and Lodgepole, Crow, and Lone Tree Creeks are part of the South Platte Eiver drainage. Horse and Chugwater Creeks are the only streams that are perennial throughout their course in the county. Crow Creek at one time was perennial from the mountains to the vicin­ ity of Arcola, Wyo. (Foley, 1943, p. 9; Babcock and Bjorklund, 1956, p. 8), but the channel through the city well field is now dry. Other streams in the area are intermittent, alternately gaining water from and losing water to the ground-water reservoir.

CLIMATE

The climate of the area is characterized by high evaporation, wide temperature range, cold winters, and low precipitation. Strong winds are frequent during the winter and spring. Summer temperatures are relatively cool; on only 8 percent of the days in an average year are temperatures in the nineties. January is the coldest month; on 13

GEOLOGY 7

percent of the days in an average January temperatures are zero or below. The growing season in Laramie County averages between 130 and 140 days; and, at Cheyenne, the mean precipitation from 1871 to 1964 was 14.67 inches, about 70 percent of which fell during the grow­ ing season.

GEOLOGY

Rocks ranging in age from Precambrian to Recent are present in Laramie County. The sedimentary rocks are predominantly shale with smaller amounts of sandstone, silt stone, and limestone. Physical characteristics, thickness, and water-bearing properties of the forma­ tions are summarized in table 1. The geologic map (pi. 1) was com­ piled principally from existing maps. Because of the small scale of the map and the relative unimportance of the older formations as aquifers, many formations have been mapped together.

BOCKS OF PRE-TERTIARY AGE

Pre-Tertiary rocks have not been considered to be major aquifers in Laramie County, because other supplies are generally more readily available. There is, however, increasing need for an understanding of the total water resources of the area. For this reason, information on water-bearing properties is given for formations for which well data are not available. Much of the following discussion is inferred from data obtained in nearby areas.

The oldest rocks in the area are of Precambrian age and are exposed in the Laramie Range in the western part of the county. They have been mapped in some detail by Darton, Blackwelder, and Siebenthal (1910), and more recently part of the area was mapped by Newhouse and Hagner (1957). The rocks are principally granite, gneiss, and schist. Of these the most widespread is granite, which is normally massive and coarse grained, although locally it may be either fine grained or porphyritic (Darton and others, 1910, p. 5). The granite is weathered to depths of as much as 40-50 feet (Darton. and others, 1910, p. 5), and it forms rounded hills. Where the granite is firm, weathering occurs principally along joints, and the rock has the appearance of stacks of rounded boulders.

Pre-Tertiary sedimentary rocks, which may have an aggregate thickness of as much as 12,000 feet, are exposed only in a narrow belt along the eastern mountain front, where the formations have been up­ turned and faulted. The dips of the beds range from 5° to vertical, and some beds are overturned. Anticlines east of the mountains cause reversals in dip in some areas. Horse Creek and Borie oil fields are on anticlines, and similar folds probably occur elsewhere.

TAB

LE 1

. Su

mm

ary

of s

trat

igra

phic

uni

ts a

nd t

heir

wat

er-b

eari

ng c

hara

cter

istic

s

Era Cenozo

ic

Syst

em

Qua

tern

ary

Ter

tiar

y

Seri

es

Rec

ent

?

Plei

stoc

ene

Plio

cene

Mio

cene

Olig

ocen

e

Sub

divi

sion

Floo

d-pl

ain

depo

sits

Ter

race

de

posi

ts

Oga

llala

F

orm

atio

n

Ari

kare

e F

orm

atio

n

Whi

te R

iver

F

orm

atio

n

Lan

ce

For

mat

ion

Thi

ckne

ss

(fee

t) 0-85

0-20

0

0-33

0

0-45

0

0-50

0

200-

1500

Phy

sica

l cha

ract

eris

tics

Len

ticu

lar

beds

of

fine

to v

ery

coar

se

sand

, gr

avel

, si

lt,

and

clay

; so

me

cobb

les

and

boul

ders

.

Len

ticu

lar

beds

of c

oars

e sa

nd,

grav

el,

silt,

fi

ne

sand

, an

d cl

ay;

som

e co

bble

s an

d bo

ulde

rs.

Het

erog

eneo

us

depo

sits

of

gr

avel

, sa

nd,

and

silt,

con

tain

ing

som

e co

b­

bles

and

bou

lder

s.

May

be

eith

er

un co

nsol

idat

ed o

r w

ell

cem

ente

d.

Loo

se

to

wel

l ce

men

ted

very

fi

ne

grai

ned

to f

ine-

grai

ned

gray

to w

hite

sa

ndst

one

and

silt,

con

tain

ing

hard

co

ncre

tiona

ry

zone

s.

May

be

a

coar

se c

hann

el c

ongl

omer

ate

at b

ase

in s

ome

area

s.

Pre

dom

inan

tly

a un

ifor

m

brit

tle

pink

ish-

brow

n si

ltsto

ne.

Con

tain

s be

ds o

f san

dsto

ne a

nd c

ongl

omer

ate,

pr

inci

pall

y ne

ar

the

mou

ntai

ns.

Bas

al p

art

of fo

rmat

ion

cont

ains

red

an

d gr

een

clay

wit

h co

nspi

cuou

s ir

on

stai

ning

.

Lig

ht-g

ray

to y

ello

w -b

row

n sa

nlst

one;

co

ntai

ns b

eds

of s

oft

shal

e an

d co

al.

Wat

er s

uppl

y

Yie

ld s

mal

l to

mod

erat

e su

pplie

s to

wel

ls.

Yie

ld l

arge

sup

plie

s to

som

e w

ells

.

Yie

lds

smal

l to

lar

ge s

uppl

ies

to w

ells

.

Yie

lds

smal

l to

mod

erat

e su

pplie

s to

mos

t w

ells

; la

rge

supp

lies

coul

d be

obt

aine

d un

der

opti

mum

con

ditio

ns.

Yie

lds

larg

e su

pplie

s fr

om c

ongl

omer

ate

and

open

ings

in

silts

tone

; ho

wev

er,

will

pr

obab

ly

yiel

d on

ly

smal

l su

pplie

s in

mos

t ar

eas.

Yie

lds

smal

l su

pplie

s.

Dee

per

wel

ls w

ould

pro

babl

y ob

tain

mod

erat

e yi

elds

; ho

wev

er,

the

wat

er m

ay b

e un

fit

for

som

e us

es.

00

Cre

tace

ous

Upp

er

Cre

tace

ous

Low

er

Cre

tace

ous

Fox

Hill

s Sa

ndst

one

Pie

rre

Shal

e

Nio

brar

a F

orm

atio

n

Fro

ntie

r F

orm

atio

n

Mow

ry S

hale

New

cast

le

Sand

ston

e

Skul

l C

reek

Sh

ale

Cle

verl

y F

orm

atio

n

250±

5700

±

325-

400

550-

600 80

75-1

00

70-1

50

100-

200

Med

ium

-gra

ined

gra

y to

yel

low

-bro

wn

fria

ble

silt

y sa

ndst

one

inte

rbed

ded

wit

h da

rk s

hale

.

Pre

dom

inan

tly

dark

-gra

y sh

ale

but

has

a th

ick

pers

ista

nt s

ands

tone

bed

ne

ar th

e m

iddl

e of

the

form

atio

n.

Lim

esto

ne a

nd c

alca

reou

s sh

ale.

Bla

ck a

nd g

ray

shal

e co

ntai

ning

thi

n sa

ndst

one

beds

.

Upp

er p

art

is d

ark-

gray

sili

ceou

s sh

ale

that

wea

ther

s li

ght

gray

; lo

wer

par

t is

dar

k-gr

ay s

hale

.

Coa

rse-

grai

ned

mas

sive

san

dsto

ne.

Dar

k-gr

ay f

issi

le s

hale

.

Flag

gy t

an s

ands

tone

, co

nglo

mer

ate,

qu

artz

ite,

silt

ston

e, a

nd s

hale

. O

ut­

crop

s co

nsis

t of

an

uppe

r an

d lo

wer

sa

ndst

one

sepa

rate

d by

sha

le.

Not

kno

wn

to y

ield

wat

er t

o w

ells

in

the

area

. Y

ield

s sm

all

to m

oder

ate

supp

lies

of w

ater

to

wel

ls s

outh

of

the

area

, in

C

olor

ado.

T

he w

ater

is

of t

he s

odiu

m

bica

rbon

ate

type

(B

abco

ck a

nd B

jork

lund

, 19

56).

Yie

lds

smal

l su

pplie

s of

wat

er,

gene

rally

poo

r in

qua

lity

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GEOLOGY 11

The oldest known sedimentary rocks in Laramie County are equiva­ lent to the Madison Limestone of Early and Late Mississippian age. The rocks, which consist of sandstone, siltstone, and limestone, are 45 feet thick at Farthing, Wyo., but wedge out near the Middle Fork of Crow Creek (Maughan, 1963, fig. 66.2). The formation is not differ­ entiated in this report but is included with beds assigned to the Casper Formation.

The Casper Formation of Pennsylvania!! and Permian age is di­ visible into two units. The lower unit, which correlates with the Fountain Formation of Pennsylvania!! and Permian age, consists of about 200 feet of reddish-yellow sandstone, quartzite, and arkose. The upper unit, which correlates with the Ingleside Formation of Permian age, consists of 600-700 feet of limestone. .The limestone forms the dominant hogback along much of the mountain front.

Overlying the Casper Formation is a red-bed sequence of Permian and Triassic age. As redefined by Maughan (1964), the Goose Egg Formation of Permian and Early Triassic age consists of about 200 feet of red beds interstratified with gypsum, limestone, and dolomite. The Chugwater Formation of Triassic age consists of about 500 feet of moderate-reddish-orange siltstone and very fine grained sandstone.

The Sundance and Morrison Formations, of Late Jurassic age, over­ lie the Chugwater Formation. They consist of about 300 feet of sand­ stone, greenish and variegated blue and olive-green shale, and thin beds of limestone. The rocks are generally soft and friable and weather to form slopes beneath the overlying Cleverly Formation.

Rocks of Early Cretaceous age include, in ascending order, the Cloverly Formation, Skull Creek Shale, Newcastle Sandstone, and Mowry Shale. The Cloverly Formation consists of two prominent sandstone units separated by soft shale. The thickness of the sand­ stone outcrops is highly variable locally. In sections measured by Lee (1927), the lower sand is 54 feet thick at Mill Creek and 25-45 feet thick at Chugwater Creek. The upper sandstone, at the same loca­ tions, is 12 and 30-40 feet thick, respectively. Where the sandstone outcrops are more resistant than adjacent strata, they form prominent ridges along the mountain front; elsewhere such surficial expression may be entirely absent.

The Skull Creek Shale consists of as much as 150 feet of dark soft fissile shale that often forms a narrow valley between steeply dipping strata of the underlying Cloverly Formation and the overlying New­ castle Sandstone. The Newcastle Sandstone is a coarse-grained mas­ sive sandstone that is as much as 100 feet thick, but the thickness varies considerably throughout the area. The overlying Mowry Shale

12 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

consists principally of dark-gray siliceous shale and is about 80 feet thick.

Rocks of Late Cretaceous age include, in ascending order, the Fron­ tier and Niobrara Formations, Pierre Shale, Fox Hills Sandstone, and Lance Formation. The Frontier Formation is about 600 feet thick and consists principally of nonresistant shale. The overlying Niobrara Formation is about 400 feet thick near the North Fork of Horse Creek (Darton, 1910, p. 9). The formation in that locality consists of light- orange calcareous shale and limestone, which are more resistant to erosion than adjacent formations.

Overlying the Niobrara Formation is the Pierre Shale, It is pres­ ent in large areas north of Crow Creek, where it is exposed in many stream valleys. Elsewhere the formation is generally concealed by overlying thin pediment and terrace deposits. The Pierre consists of more than 5,000 feet of interbedded shale, sandy shale, and lenticular sandstone. The Pierre becomes increasingly sandy in its upper part and grades upward into the Fox Hills Sandstone.

The Fox Hills Sandstone, which consists of gray to yellowish-brown sandstone beds interbedded with sandy shale, was mapped by Darton (1910) principally along Horse Creek and in the Crow Creek drainage. Bergstrom (1953) (correlated the rocks along Horse Creek with the Mesaverde Formation of the Laramie Basin, and the youngest Creta­ ceous unit shown in the county on the State geologic map (Love and others, 1955) is the Mesaverde Formation. The Mesaverde is equiva­ lent to a part of the Pierre Shale of this report. Fossils collected from SEi/t sec. 16, T. 14 N"., R. 69 W. (USGS Mesozoic loc. D4865) are Ostrea glabra Meek and Hayden. A few specimens have faint radial ribs, which are common on the very late forms of the species, and may be from Fox Hills or Lance strata (W. A. Cobban, written commun. 1965). Time was not available for detailed mapping, and consequently the Pierre and the younger Cretaceous strata are not differentiated on the geologic map (pi. 1).

The Lance Formation, which overlies the Fox Hills, may be as much as 1,500 feet thick in the western part of the county, but it was beveled by erosion before deposition of the White River Formation and is only about 200 feet thick in the northeastern part. Exposures in Colorado were described by Babcock and Bjorklund (1956, p. 12) as light-gray to yellowish-brown sandstone and gray to bluish-gray soft shale and clay containing lenses of crossbedded sandstone and beds of coal. Sandstone concretions, which are cemented by limonite or calcium car­ bonate, occur throughout much of the formation. Beds of calcareous shale, coal, and sandstone are abundant in the lower part of the formation.

GEOLOGY 13

ROCKS OF TERTIARY AGE

WHITE RIVER FORMATION

The White River Formation of Oligocene age has been given group rank in nearby areas and divided into the Chadron and Brule Forma­ tions. In this report the Chadron and Brule are not differentiated. The White River overlies the truncated edges of older rocks, and it is as much as 500 feet thick. It is of remarkably uniform composition throughout Laramie County and adjacent areas, consisting predomi­ nantly of massive brittle argillaceous siltstone containing a few beds of sandstone, conglomerate, and volcanic ash. The siltstone is pinkish gray on fresh exposures. Near the base of the formation, red and green shale and coarse channel deposits are present. Denson and Berg- endahl (1961, p. C170) described the White River Formation in southeastern Wyoming and adjacent areas as follows:

In general, these rocks consist of 65 to 85 percent silt and 5 to 25 percent very fine grained sand imbedded in a matrix of clay-size particles. The silt and very fine grained sand fractions consist of glass shards and angular to subrounded fragments of quartz, potassium feldspar (microcline and orthoelase), plagioclase, and small amounts of detrital minerals. The clay-size fraction consists of montmorillonitic clay, clay size carbonate flakes, and fine volcanic ash.

Where the White River Formation has been extensively fractured, weathered outcrops often appear as assemblages of loose blocks that are only inches in size, but the fractures are less pronounced on fresh exposures. (See fig. 3.) The smooth, nearly vertical walls of the White River Formation are the result of weathering along clastic dikes similar to the one shown in figure 4.

The clastic dikes observed during the investigation are composed of material derived mainly from the White River Formation. All are nearly vertical, and they have no apparent preferred orientation. The dikes range from a fraction of an inch to 11/2 feet in width, and many can be traced on the surface for several hundred feet.

ARIKAREE FORMATION

The Arikaree Formation of Miocene age is generally homogeneous and is considered to be a single hydrologic unit.

The formation is predominantly a very fine grained to fine-grained massive sandstone that contains beds of siltstone, layers of hard con­ cretionary sandstone, and thin beds of volcanic ash. A basal con­ glomerate is present in many localities.

The following logs of test holes illustrate the composition of the formation. The terminology used is that of the driller with minor modifications by the authors.

14 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

FIGURE 3. Fractured siltstone of the White River Formation, sec. 2, T. 14 N., R. 69 W. Fractures are much more pronounced on weathered surfaces, right and left background, than on freshly exposed surfaces, center.

Test hole (partial log) 19-67-5cddThick­ ness (feet)

Arikaree Formation:Siltstone, clayey, sandy, organic, calcareous, brown._______ 2. 5Sandstone, medium- to coarse-grained, trace of silt and clay,

gravelly, micaceous, grayish-brown,___________________ 5. 5Sandstone, fine- to coarse-grained, silty, clayey, micaceous,

grayish-brown_____________________________________ 4. 5Conglomerate, well-cemented, brown and mottled grayish-

brown; consists of J£-l in. subrounded igneous rock peb­ bles in a calcareous silstone matrix____________________ 9. 5

White River Formation.

Depth (feet)

2. 5

12. 5

22

GEOLOGY 15

FIGTJEE 4. Clastic dike in the White River Formation, NW% sec. 9, T. 12 N.,R. 63 W.

hole (partial log) 16-63-SOaaaThick­ ness Depth (feet) (feet)

Ogallala Formation:Siltstone, sandy, clayey, reddish-brown_________________ 9. 5 97

Arikaree Formation:Sandstone, fine- to medium-grained, gravelly, tan; contains

trace of silt_____-________--_-__--____--_-_---------- 19 116Siltstone, sandy, gravelly, tan___________________-___--__ 2 118Siltstone and fine-grained sandstone, tan_________________ 5. 5 123. 5Siltstone, massive, shaly, micaceous, moderately cemented,

brown. Bottom 1 ft well cemented____^_____________ 7 130. 5Sandstone, fine-grained, silty, pale-reddish-brown-_________ 36. 5 167

16 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

Test hole (partial log) 16-63-30aaa -ContinuedThick­ ness Depth

(feet) (feet) Ogallala Formation Continued

Sandstone, fine- to coarse-grained, well-cemented, calcareous,dark-brown_ ________________________________________ 5 172

Siltstone, well-cemented, calcareous, gray_______________ 2. 5 174. 5Sandstone, fine-grained, silty, reddish-brown______________ 17 191. 5Sandstone, fine-grained, well-cemented, calcareous, brown. _ 2. 5 194 Siltstone, sandy, reddish-brown_________________________ 7 211Sandstone, fine-grained, silty, well-cemented, calcareous,

grayish-brown_____________________________________ 11. 5 222. 5Sandstone, fine-grained, silty, brown_____________________ 22. 5 245Sandstone, fine-grained, brown; contains trace of silt_______ 26 271Sandstone, fine- to medium-grained, very dense, brown;

contains trace of silt, sandstone lenses________-__-___-__ 11. 5 282. 5Sandstone, fine-grained, thin-bedded, well-cemented, cal­

careous, grayish-brown_______________________________ 15. 5 298Sandstone, fine-grained, brown; contains trace of silt_______ 27 325Sand, fine, silty, slightly cemented, tan_________________ 19 344Sand, fine, silty, tan; calcareous in part__________________ 10 354Sand, fine to medium, brown; contains trace of silt________ 11 365Sand, fine, brown; contains trace of silt_________________ 35 400

Erosion has removed the Arikaree in the southern and western parts of the county. The formation thickens rapidly to the north and north­ east and it is about 500 feet thick along the Goshen Hole escarpment.

Numerous white resistant ledges occur in outcrops of the Arikaree Formation, in sharp contrast with outcrops of the less resistant overlying Ogallala Formation.

OGALLALA FORMATION

The Ogallala Formation of Miocene and Pliocene age unconform- ably overlies rocks that range from Miocene to Precambrian in age. The Ogallala consists of lenticular beds of sand and gravel deposited by braided streams and of silt, clay, and thin limestone beds deposited in temporary lakes. The gravel in the Ogallala was derived from the mountains to the west and consists mainly of quartz, quartzite, feldspar, gneiss, and schist.

The following logs of test holes show the heterogeneous character of the material and the change from predominantly coarse material near the mountains to finer material in the eastern part of the county. The terminology used is that of the driller with minor modification by the authors.

GEOLOGY 17

Test hole 17-68-28bcaThick­ ness (feet)

Depth (feet)

Ogallala Formation:Clay, sandy, slightly organic, brown_____________________ 3 3Sand, fine to coarse, gravelly, slightly cemented, calcareous,

grayish-brown______________________________________ 6 9Conglomerate; consists of angular to subangular pebbles of

granitic rocks in a tan silty sandstone matrix; poorly ce­ mented in upper part, last 3 ft moderately cemented____ 21 30

Conglomerate; consists of 50-60 percent angular to sub- angular pink and gray pebbles of granitic rocks in a tan calcareous fine-grained sandstone matrix; slightly porous, moderately cemented, hard___________________________ 34 64

Conglomerate; consists of 60-80 percent pebbles of graniticrocks in a fine-grained calcareous sandstone matrix,___ 11 75

Conglomerate; consists of 60-80 percent angular to sub- angular pink and gray pebbles of granitic rocks in a tan calcareous fine-grained sandstone matrix, slightly porous, moderately hard. Occasional pebbles of buff very hard limestone from 101 to 109 ft. Occasional thin zones with sandy limestone matrix from 109 to 113 ft____________ 41 116

Sandstone, medium- to coarse-grained, moderately cement­ ed, calcareous, conglomeratic, hard, pink and tan______ 5 121

Conglomerate; consists of 60-80 percent angular to sub- angular pink and gray pebbles of granitic rocks in a cal­ careous medium-grained sandstone matrix, slightly porous, hard to very hard___ ________________________________ 9 130

Test hole (partial log) 16-63-SOaaaThick­ ness Depth (feet) (feet)

Ogallala Formation:Sand, fine to medium, clayey, slightly organic, brown__-___ 3 3 Sand, fine to coarse, very dense, tan; contains trace of silt and

gravel______________________________________________ 6 9Gravel, fine to coarse, sandy, silty, tan___________________ 9 18Sand, fine to coarse, silty, gravelly, pale-reddish-brown_____ 9 37Silt and fine sand, clayey, brown________________________ 6 43Clay, silty, reddish-brown; contains trace of sand________ 9. 5 52. 5Sand, fine to medium, tan; contains trace of silt_._________ 11.5 64Sand, fine to coarse, silty, pale-reddish-brown-____________ 13 77Silt, sandy, micaceous, tan-brown; contains trace of clay___ 8 85 Sand, fine to medium, pale-reddish-brown; contains trace of

silt-_______________________________________________ 2.5 87.5Silt, sandy, clayey, reddish-brown. ______________________ 9. 5 97

Arikaree Formation.

18 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

Test well 16-60~3bbb J- DepthOgallala Formation: (feet) (feet)

Sand, fine to medium, silty, slightly organic, dark-brown- _ _ 1. 5 1.5 Sand, fine to coarse, gravelly, brown, contains trace of silt__ 16. 5 18 Sandstone, fine-grained, well-cemented, calcareous, light-

brown____________________________________________ 7 25Sand, fine to medium, silty, brown; contains occasional

cemented nodules____________________________________ 6 31Sandstone, fine-grained, well-cemented, calcareous, reddish-

brown___-----_-----___________________-________-__- 4 35Sand, fine, silty, brown; contains occasional cemented

nodules___________________________________________ 2 37Sandstone, fine-grained, well-cemented, calcareous, reddish-

brown______________________________________________ 4. 5 41. 5Silt, sandy, calcareous, reddish-brown____________-___--_- 6. 5 48Sandstone, fine-grained, massive, slightly cemented, silty,

reddish-brown_____ __________________________________ 10. 5 58. 5Sand, fine, silty, brown_________________________________ 6.5 65Sand, fine to coarse, tan; contains trace of silt and gravel-__ 13 78 Sand, fine to coarse, gravelly, tan; contains trace of silt____ 6 84Sand, fine to coarse, tan; contains trace of silt and fine graveL 14 98 Sand, medium to coarse, and fine gravel, silty, reddish-brown_ 10 108 Sand, fine, silty, reddish-brown__________________________ 12 120

Arikaree Formation:Sandstone, fine, silty, grayish-brown- ____________________ 10 130

The Ogallala is thickest in the western part of Laramie County, where 330 feet of the formation has been logged. It thins eastward to the State line, where 150 feet is exposed near Pine Bluffs (Rapp and others, 1953). The thickness elsewhere in the eastern part of the county is much less, and the exposure near Pine Bluffs is probably about the maximum thickness of Ogallala present near the Wyoming- Nebraska border.

Some resistant beds in the Ogallala, such as the one capping the es­ carpment at Pine Bluffs, are cemented by calcium carbonate. The topography where the Ogallala is exposed, however, generally con­ sists of rounded hills and shallow valleys.

ROCKS OF QUATERNARY AGE

ALdLTJVITJM

Alluvium underlies terraces and flood plains throughout the county. It consists of lenticular beds of poorly sorted clay, silt, sand, gravel, and boulders that were derived from all the older rocks in the area. The coarse fraction is predominantly igneous rock derived from Ter­ tiary formations and from Precambrian rocks of the Laramie Range. Thick deposits of alluvium are known only in areas immediately underlain by the White River Formation.

GEOLOGY 19

Logs of many wells show little difference between the composition of alluvium derived from the White River Formation and the White River Formation in place. Many of the reported fractured or porous zones in the White River are probably permeable alluvial deposits. Babcock and Bjorklund (1956, p. 14) stated that "In some places, a zone of loose material is present at the top of the formation [White River] where it is protected by a cover of younger deposits. This zone, which is as much as 15 feet thick, contains rounded pebbles of siltstone derived from the Brule Formation."

McLaughlin (1948, p. 12) noted that along Lodgepole Creek in Nebraska the "porous" zone in the White River was confined to the valley and did not extend beneath the bordering uplands. He stated (p. 13) : "During the test drilling done by the town of Julesburg [Colo.], it was found that the 'porous' zone consists of moderately well rounded pebbles of reworked Brule clay [White River], the pebbles ranging in diameter from less than half an inch to more than 2 inches. Inasmuch as the so-called 'porous' zone is actually a deposit of coarse gravel that is confined to the zone underlying the alluvium, it perhaps should be considered a part of the alluvium."

The difficulty in distinguishing between the alluvium and the for­ mation from which it was derived, whether White River or Ogallala, is probably why Bjorklund (1959, p. 15) found that the alluvium of Lodgepole Creek valley between the Wyoming State line and Chap- pell, Nebr., is relatively thin, averaging about 25 feet, whereas Rapp, Warner, and Morgan (1953, p. 47) stated that the alluvium along Lodgepole Creek in Wyoming is generally thin but is as much as 85 feet thick at some places.

TERRACE DEPOSITS

Terraces are widely distributed in the county but are generally topographically high and drained of water. The only terraces shown on the geologic map (pi. 1), however, are those in the Pine Bluffs low­ land in the southeast corner of Laramie County and along Horse Creek in the northeast corner of the county. These are the areas where terraces are underlain by significant thicknesses of saturated alluvium.

Pine Bluffs loivland. Terraces in the Pine Bluffs lowland have been discussed in detail by Rapp, Warner, and Morgan (1953), who divided them into older and younger terrace deposits. The older ter­ races include the surfaces that extend from about 4 miles south of the Colorado State line (Weist, 1965) in Rs. 61 and 62 W. northward to the valley of Lodgepole Creek. This terrace is a nearly continuous surface in Wyoming, cut only by Muddy Creek and its tributaries and

20 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

Crow Creek. A generalized map of the saturated thickness of the alluvium underlying the main part of the terrace is shown in figure 12.

The alluvium underlying one of the younger terraces along Lodge- pole Creek was found to be 107 feet thick during a test drilling pro­ gram in 1943. Drilling during this program provided data incor­ porated in the geologic sections shown in figure 5. The thickness of the alluvium underlying the other younger terraces is not known, mainly because of the difficulty in recognizing the White River For­ mation in the logs available. However, the level to which erosion occurs in tributaries is accordant with that in the main stream Lodgepole Creek. Therefore, thick deposits of alluvium probably underlie the other younger terraces as well.

Horse Creek. The terrace along Horse Creek in the northeast corner of the county is only about 8 miles long and, in most places, less than 1 mile wide. The alluvium underlying the terrace was deposited in a former course of Horse Creek, and the terrace surface is 40-60 feet above the present (1965) level of Horse Creek. Little is known about the thickness of the deposits. Well 18-62-12acd penetrated 65 feet of saturated terrace deposits, and test drilling would probably locate com­ parable thicknesses in other parts of the deposits.

FLOOD-PLAIN DEPOSITS

Most of the streams and dry washes are underlain by flood-plain deposits, but only the deposits along the major drainages are shown on plate 1. In most of the tributary valleys and some reaches of Horse and Lodgepole Creeks, the alluvium is very thin. In many of the tributary valleys, the alluvium may be above the water table. The thickest flood-plain deposits are in the Pine Bluffs lowland, where they are as much as 85 feet thick; known thicknesses elsewhere are less than 50 feet.

GROUND WATER

HISTOBY OF DEVELOPMENT

Cheyenne and Pine Bluffs were established in conjunction with the building of the Union Pacific Railroad in 1867. Other than the rail­ road, there was little economic development in Laramie County until 1875. Cattle raising was the principal industry from 1875 to about 1893.

In 1909 farmers began to move into the eastern part of the county after methods had been developed for producing dryland crops. The communities of Burns and Carpenter were established at about this time. Since 1930 the rural population has decreased, but the county has experienced a rapid growth in population that is primarily attribut­ able to the expansion of Cheyenne and its suburbs. The population of

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5150'

-i

5100'

5050' -

5000'

From

Rap

p an

d ot

hers

(19

53)

VERT

ICAL

EXA

GGER

ATIO

N X

40

FIG

URE

5. S

ecti

ons

acro

ss

Lod

gepo

le C

reek

val

ley,

lo

okin

g up

stre

am.

(Loc

atio

n of

sec

tion

s sh

own

on p

i. 1.

)

22 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

Laramie County in 1960 was 60,149, with a'bout 87 percent of the people residing in the Cheyenne area.

Use of ground water for irrigation was started in the Pine Bluffs- Carpenter area during the drought years of the middle 1930's and by 1942 about 75 irrigation wells were in use. The number of wells in­ creased to about 125 by the end of 1946, and by 1950 an estimated 210 wells were in operation (Rapp and others, 1953, p. 30). As of October 1964, there were 'about 220 irrigation wells in the Pine Bluffs-Car­ penter area. However, many of these wells are not pumped every year. Nearly all the large wolls in this area are equipped with elec­ tric motors, and records of the Rural Electric Co. at Pine Bluffs showed that 148 wells were in operation during 1964. A few wells were pumped during the year with some other type of power. Use of ground water for irrigation in this area has increased from an esti­ mated 1,500 acre-feet in 1936 to an estimated 17,000 acre-feet in 1964.

The municipal water supply for Cheyenne (1960 population, 43,505) is about one-third ground water and about two-thirds surface water. The ground water is obtained from 44 wells in the municipal well fields west and northwest of Cheyenne, and from 2 collection galleries in the alluvium of Crow Creek, one in sec. 20, T. 14 N., R. 67 W., and another in sec. 27, T. 14 N., R. 67 W. Part of the surface water is obtained from the headwaters of Crow Creek, and since January 1964 an addi­ tional amount has been piped from Douglas Creek in the Medicine Bow Mountains about 50 miles west of Laramie County. The amount of water used annually by Cheyenne since 1941 is shown in figure 6. In­ cluded in the total is water supplied to F. E. Warren Air Force Base, the Frontier Gasoline Refinery, and the Union Pacific Railroad. In 1964, these three consumers used about 22 percent of the total water pumped to Cheyenne. A fertilizer plant that moved to the vicinity of Cheyenne in 1964 is expected to pump about 100 million gallons of ground water per year.

PRINCIPLES OF OCCURRENCE

Meinzer (1923a), Wenzel (1942), and several others have fully dis­ cussed the principles of the occurrence and movement of ground water. Only a few definitions and principles will be discussed in this report.

Porous rocks contain interstices, which are open spaces that form the receptacles for ground water. The size of the interstices in a sedi­ mentary rock depends on the size of the particles, the degree of sorting, and the amount of compaction and cementation. Hard massive forma­ tions may have voids that result from deformation or solution that occurred after the rocks were laid down. Interconnected interstices form the conduits through which water may move in the rocks.

GROUND WATER 23

FIGUEE 6. Sources of Cheyenne municipal water supply and annual usage.

Permeability is the property of a porous material that permits it to transmit water through its interstices under a hydraulic gradient. In the more permeable rocks, such as deposits of unconsolidated sand and gravel, the interstices are relatively large and will permit free move­ ment of water. Rocks such as claystone, siltstone, and fine sandstone are less permeable, so movement through them is much slower. Kocks that are capable of yielding recoverable quantities of water to wells are called aquifers.

The water table has been defined by Meinzer (1923b, p. 22) as "the upper surface of a zone of saturation except where that surface is formed by an impermeable body." The zone of saturation is that zone in which permeable rocks are generally saturated with water under hydrostatic pressure. The water table, which is not a flat surface, has irregularities related to those of the land surface, although smoother. It is not stationary; instead it fluctuates as water is added to or re­ moved from the underground reservoir.

24 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

An artesian aquifer is one in which water will rise in a well to some level higher than the top of the aquifer. For this to occur, a relatively impermeable rock must overlie the aquifer and confine the water under pressure.

The piezometric surface of an aquifer is an imaginary surface that everywhere coincides with the static level of the water in the aquifer. It is the surface to which the water from a given aquifer will rise under its full head. If the piezometric surface is above the land surface, water in wells that penetrate the aquifer will flow. The piezometric surface is also irregular, but its irregularities may not be comparable to those of the land surface.

HYDRAULIC PROPERTIES OF THE PRINCIPAL AQUIFERS

The ability of an aquifer to transmit water and to yield water to wells depends on its hydraulic properties. The gross rate of movement of the water is proportional to the hydraulic gradient and to the perme­ ability of the aquifer. The hydraulic gradient of an aquifer at a given place is the rate of change of pressure head per unit of distance at that place in that direction (Meinzer, 1923b, p. 38). Generally, for horizon­ tal aquifers the hydraulic gradient is expressed as the ratio of the differ­ ence in static water level between two points to the horizontal distance between them.

The field coefficient of permeability, P, is a measure of the material's capacity to transmit water. It is defined as the rate of flow of water in gallons per day through a cross-sectional are'a of 1 square foot under a hydraulic gradient of 100 percent at the prevailing water temperature and is expressed in gallons per day per square foot. The coefficient of transmissibility, T, is the rate of flow of water, in gallons per day, at the prevailing temperature through a vertical strip of the aquifer 1 foot wide extending the full saturated thickness of the aquifer under a hydraulic gradient of 100 percent. The coefficient of transmissibility is equal to the average field coefficient of permeability times the satu­ rated thickness of the aquifer and is expressed in gallons per day per foot.

The specific capacity of a well is the yield per unit of drawdown of the water level in the well and is generally expressed in gallons per minute per foot of drawdown. It is not a constant; it may decrease with increased pumping rates because of partial dewatering of the aquifer. The specific capacity will also decrease with time if the well is pumped continuously because the drawdown increases as the cone of influence of the well expands.

The coefficient of storage, $, of an aquifer is the volume of water released from or taken into storage per unit surface area of the aquifer

GROUND WATER 25

per unit change in the component head normal to the surface. In unconfined aquifers the coefficient of storage is approximately equal to the specific yield, which is the quantity of water that a given satu­ rated volume of the aquifer will yield by gravity drainage. The specific yield is the ratio of the volume of water given up by gravity drainage to the total volume of the aquifer that is drained.

WHITE RIVER FORMATION

The White River Formation yields small to large supplies of water to wells in Laramie County. Large yields,1 over 350 gpm (gallons per minute), are obtained only in the Federal well field and in the Pine Bluffs lowland; however, well 19-66-lTcda near Bear Creek and well 18-62-15ddb near Horse Creek are exceptions.

Logs of wells in the Federal well field show that the large yields of water are obtained from gravel channels in the White River Forma­ tion. These deposits are apparently limited to the lower part of the formation. No large gravel channels have been found in the upper part of the White River exposed along the escarpment between Granite and Federal. Two pumping tests were made in the Federal well field. However, conditions in the aquifer do not approximate those assumed in the available mathematical derivation of theoretical aquifer re­ sponse, and coefficients of transmissibility and storage could not be computed. Specific capacities, which are available from 7 of the 10 Cheyenne municipal wells which tap the White River Formation, range from 2.8 to 8.1 gpm per foot of drawdown. More than half of the test wells drilled in the area by the city were abandoned because of low yields; therefore, these specific capacities are probably the larg­ est that might be expected in the area.

The White River Formation is reportedly the principal aquifer in the Pine Bluffs lowland. Yields of the irrigation wells are as much as 2,000 gpm; the reported specific capacity of one well is 257 gpm per foot of drawdown. Because of the difficulty in differentiating the White River that is in place from that which has been reworked and deposited as alluvium, many of the wells reported to be in the White River may be in alluvium.

Siltstone of the White River Formation is not sufficiently permeable to yield significant quantities of water to wells. Three samples of siltstone from Goshen County were tested in the U.S. Geological Sur­ vey's Hydrologic Laboratory, Denver, Colo., in order to determine their coefficients of permeability. The results ranged from "too small to be measured accurately" to 0.2 gpd per sq ft (gallons per day per

1 In this report 3 yield categories are used. The range of yields in each category is as follows:. Small, 0-50 gpm; moderate, 50-350 gpm; and large, more than 350 gpm.

26 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

square foot) (Kapp and others, 1957). The permeability of the silt- stone in Laramie County is probably very similar. Large yields of water from the White Kiver Formation have been attributed to joints, fissures, and fractures formed after deposition of the formation. Babcock and Bjorklund (1956, p. 14) described the formation as follows:

Surficially, the Brule Formation [White River] is cut by systems of joints. The joints are either horizontal (along bedding planes) or vertical and, although they are most prominently developed where the formation is exposed, they occur also at the top of the formation where the Brule [White River] is mantled by younger stream deposits. In some places, nearly vertical fractures, or fissures, penetrate to unknown depths within the formation and possibly penetrate com­ pletely through it. Surface traces of these fractures, some of which are at least 1 foot wide and 1 mile long, are seen easily on aerial photographs, but they are difficult to detect and follow on the ground.2

Other investigators have similarly described the White Eiver.It is assumed that the vertical fractures (or fissures) in outcrops

referred to in previous reports are clastic dikes such as shown in figure 4. Because these dikes are often truncated within the White River Formation and the filling material is generally similar to the surround­ ing formation, it is doubtful whether they are sufficiently permeable to yield even moderate quantities of water to wells.

Fractures undoubtedly transmit water to many small-yield wells that tap the White Eiver Formation. However, fracturing alone does not adequately explain the large variation in permeability that occurs within a few tens of feet a battery of wells connected below the water level is often drilled to locate permeable sites or explain the concen­ tration of large-yield wells in areas underlain by alluvium. Permea­ bility resulting from fractures, such as those shown in figure 3, would not vary significantly in short distances. Furthermore, if fractures were the- principal cause of zones of large permeability, it would be expected that large-yield wells would be closely related to faulting; however, only one such well is known to the authors. Welder and Weeks (1965, p. 49) reported that the relatively large yield of a well (29-69-33bac) in the Horseshoe Creek valley, Platto County, Wyo., may be the result of increased permeability near the Elkhorn fault.

Piping, which is the process by which subterranean channels form as a consequence of the movement of water in relatively insoluble and incoherent clastic rocks, occurs in the White River (fig. 7) and is wide­ spread in alluvium derived from the formation. Piping occurs where there are large hydraulic head differences in short distances, an ex­ ample of which is the "gully-wall" type of piping so widespread in the

- The authors of this report believe that the features previously identified on aerial photographs as fractures are traces of animal and vehicle trails.

GROUND WATER

FIGURE 7. Pipe in White River Formation, sec. 15, T. 15 N., R. 69 W.

Western States (Parker, 1963, p. 104). Parker (1963, p. 106) listed the conditions necessary for piping to occur as follows: (1) Sufficient water to saturate some part of the soil or bedrock above base level,(2) hydraulic head to move the water through a subterranean route,(3) presence of a permeable erosible soil or bedrock above base level, and (4) an outlet for flow. Parker listed siltstone, volcanic ash, and swelling clays as materials favorable to piping. Some of the permea­ bility in the White Eiver Formation is very likely the result of piping.

Conditions related to piping have been described in part of the White River in Scot'ts Bluff County, Nebr., by Wenzel, Cady, and Waite (1946, p. 85), who stated, "The Brule is eroded very easily and, hence, in irrigated parts of the county, the openings have been en­ larged by circulation through them. Thus, the permeability of the formation is probably greater in those areas than it is where the source of ground water is precipitation."

In the Pine Bluffs lowland, an erosion surface with a local relief of 100 feet formed on the White River before deposition of the alluvium, and conditions were created that were suitable for the formation of pipes. The position of the pipes may have been controlled by frac­ tures or other zones of weakness in the formation; however, pipes, not

28 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

fractures, are believed to be the cause of increased permeability in areas where large yields are obtained. The large-yield wells near Horse Creek (18-62-15ddb) and Bear Creek (19-66-17cda) may be in areas of increased permeability resulting from piping near the streams. However, well 19-66-17cda may derive part of its water from alluvium.

ARIKAREE FORMATION

Previous investigators have not considered the Arikaree Formation to be a source of large supplies of water in Laramie County; however, the Arikaree is believed to contribute a large part of the yield of sev­ eral irrigation wells in the county. Although the permeability of the formation is generally low, the saturated thickness of the formation is great enough in the central part of the county that sufficiently deep wells yield large quantities of water.

Because the Ogallala Formation consists, in part, of reworked mate­ rial from the Arikaree Formation, it is difficult to distinguish the con­ tact between the two formations in many wells. Where the forma­ tions are so similar in appearance that they are not easily distin­ guished, the water-bearing properties of the Ogallala and of the Arikaree are similar enough that the two formations may be considered as a hydrologic unit.

The yields of wells 16-65-3bbb and 16-65-3cca, open to both the Ogallala and Arikaree Formations, are reported to be in excess of 300 gpm. Specific capacities of these two wells were reported to be 4.5 and 7.4 gpm per foot of drawdown, respectively. Well 17-63-6dc, which taps only the Arikaree, has a reported specific capacity of 3.6 gpm per foot of drawdown with a pumping level 92 feet below land surface.

Data from wells producing from the Arikaree, or Arikaree and Ogallala, have been used to prepare a specific capacity frequency graph. Specific capacities per foot of penetration were plotted against the percentage of wells, as shown in figure 8. The Arikaree is fairly homogeneous over a large area; therefore, data from Arika­ ree wells in Platte County were used to support the data obtained from Arikaree wells in Laramie County. By fitting a straight line to the plotted data, the specific capacity is shown to average 0.016 gpm per foot of penetration in the Arikaree.

Small yields can be obtained at most locations where the Arikaree is saturated. However, based on existing data, the chances are good of obtaining large yields from wells in areas where at least 200 feet of saturated material overlies the White River Formation, as shown on plate 2. Pumping lifts would probably range from 100 to 300 feet.

GROUND WATER 29

SPECIFIC CAPACITY PER FOOT OF PENETRATION, IN GALLONS

PER MINUTE PER FOOT OF DRAWDOWN

o p o o c 3 b b b i-3 O i-- Ol

- Ol

^\\

N

0\

\

* \0 0

1 » »x 0

o

\X

EXPLANATION

o Data obtained from wells

in Platte County

Data obtained from wells in Laramie Cour

!

x. ,^"\v\\

10 20 30 40 50 6C

PERCENTAGE OF WELLS

80 90 95 98

FIGURE 8. Specific capacity frequency of wells in the Arikaree Formation, in Platte and Laramie Counties.

An example of using these data for predicting yields of wells is illustrated as follows. In an area where 200 feet of saturated ma­ terial can be penetrated, the specific capacity would probably be greater than 3.2 (0.016 X 200) gpm per foot of drawdown in 50 percent of the wells.

To obtain maximum yields with minimum lift, wells should be drilled completely through the Ogallala and Arikaree Formations and should be finished so that as much of the aquifer as possible contributes water to the well.

226-450 O - 67 - 2

30 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

OGAL.LALA FORMATION

PUMPING TESTS

The Ogallala Formation is the most extensively developed aquifer in Laramie County. The area of largest ground-water withdrawal from the Ogallala is in the Cheyenne well field, about 6 miles west of Cheyenne. Of 36 municipal wells drilled in this area, 35 are con­ sidered to obtain water primarily from the Ogallala.

Theis (1941, p. 15) analyzed pumping tests at six of the wells in the Cheyenne well field in 1940. In 1942, Foley (1943, p. 69) made a pumping test at one of the same wells as Theis and obtained similar results. Pumping tests were made on four more wells in the period 1942-46 (Morgan, 1946, p. 21). D. A. Morris made 12 pumping tests when the Cheyenne well field was expanded in 1955 and 1956; 5 pumping tests were made in 1964: 3 in the Cheyenne well field, 1 at an industrial plant, and 1 at a privately owTned irrigation well. These tests were analyzed by the Theis nonequilibrium formula (Jacob, 1950, p. 368) and the Theis recovery formula (Theis, 1935).

Results of all the pumping tests are shown in table 2. The wide range of the coefficients of transmissibility is expected, owing to the heterogeneity of the Ogallala Formation. Theis (1941, p. 15) stated, "The recovery curves of 'all the wells, except the Eddy well [14-68- 23ddc] showed anomalies that are doubtless to be ascribed to irregu­ larities of the aquifer." One of the basic assumptions made in ana­ lyzing aquifer tests is that the aquifer is homogeneous and isotropic. However, the water-bearing beds in the Ogallala consist of lenses, stringers, and irregular masses of sand and gravel which are inter.- bedded with silt and clay. Two of the pumping tests made in 1964 were continued for 7 days to determine if, with a longer pumping period, the Ogallala would respond as a homogeneous aquifer. The indicated boundary conditions showed that even prolonged pumping tests were not reliable for computing the aquifer characteristics of the formation. Although the data obtained from the individual pumping tests are not significant by themselves, they can be used for comparison of the aquifers within the formation tapped by the different wells and add to the geologic knowledge of the aquifers. Morgan (1946, p. 12) noted that, in the older parts of the Cheyenne well field, the wells appear to tap two or more locally separate lenses, or groups of lenses, of sand and gravel. Wells that are in a belt ex­ tending from wells 13-68-4acd and 13-68-4dcc northeast to well 14- 68-25dda mutually interfere but do not appreciably affect other wells.

Adjacent to this belt, four other wells, 14-68-26bdd, 14-68-26cbc, 14-68-27dcc, and 14-68-34abb, appear to be in a separate lens, and apparently there is slight hydrologic connection between these two

GROUND WATER 31

TABLE 2. Aquifer coefficients of the Ogallala Formation as determined from pump­ ing tests

Date

1940 1940.-. _ ---- 1940 1940 1940 1940 1948 1945 1945 ------1945 1945 May 1956. - -

Do

Do-Do

October 1955...February 1956..

October 1956. ..1956 March 1964.....

February 1964..

Do

August 1964 September 1964

Location of pumped well

14-68-25bcb--.

27dcc 26cbc_ 23ddc--_26bdd 26cbc _ .

13-68-14bbb I4cbd.--

14-68-33dcc

14-67-24acb 14-68-13dad- . .14-67-18cbd...

14-68-14ada--_

24bdd 13acb .14dcd-_.

14-67-18ddc...

19bbd 7ccb _ .

14-68-13ccd-__-26cbc... .

24ddd

36acc ....

15-67-2dba--_16bca ....

Name

Eddy 1 -

Elkar 7 .

King 4--

Bell5_._-Bell 6-

Bell 7.. Bell 8-. Bell 10.. ..Bell 11-. -Bell 12.- -

Bell 14.- -

Bell 15- -Bell 16-.-Belll7_ BaUey 3...

HappyJack 2.

Coeffi­ cient

of trans- missi- bility (gpd

per ft)

16, 75016,40017,00026, 9004,7501,065

24,95431, 70023,39234,31612, 2781,670

10, 8246,900

13, 600

7,20032, 000

6,20023,00019,20031, 000

4,30016, 400

3,0005,580

27,00026,40028, 200

138,300

2 5, 300

15, 000

39, 200

1,730

1,835

1,870

Coefficient of

storage

5.6 X 10-"

5.9 X 10-5

1.8 X 10-"

3. 11X10-*

1. 95X10-*

7. 85XHH

1. 4X10-*

4.95X10-5

6. 74X10-3

3. 19X10-3

Specific capac­

ity (gpm per

foot of draw­ down)

2.94.7

14.05.5

15.3

1.5

1.5

13.55.2

.3

Length of test

hr min

145 404646

4825 5046732424

1212

27 207

24 55168168168168

168

4

4

232 3055 4055 40

55 40

55 40

Remarks

Observation well1,700 ft west of pumped well.

Observation well2,140 ft north of pumped well.

Observation well1,320 ft west of pumped well.

Do.

Observation well1,730 ft west of pumped well.

Observation well2,950 ft east of pumped well.

Observation well2,000 ft west of pumped well.

Observation well1,981 ft southeast of pumped well.

Observation well835 ft west of pumped well.

Observation well1,200 ft south­ west of pumped well.

1 Coefficients of transmissibility and storage were calculated from early test data. At least 4 boundary conditions were indicated; therefore, interpretation is doubtful. The coefficient of transmissibility will probably range from 4,900 to 38,300 gpd per ft (gallons per day per foot), and the coefficient of storage will probably range from 3.04X10~5 to 1.95X10-*.

2 Aquifer characteristics calculated from the first 24 hours of data; later data indicate boundary conditions.

226-450 O - 67 - 3

32 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

groups of wells. Two other wells, 13-68-14bbb and 13-68-14cbd, ap­ pear to tap a lens isolated from the two previously mentioned groups of wells. Morgan also stated that wells 14-68-23ddc and 14-68-24dd may be in another separate lens. This was verified in 1964 by the au­ thors during a 7-day pumping test of well 14~68-24ddd. In addition, the well yielded water from the same zone as 14-67-30abb and 14-68- 24bdd, but the water level in well 14-68-25dda was not affected. Mor­ gan (1946, p. 12) stated, "The alignment of the various identified beds suggests that the mass of sand and gravel furnishing water to the well field is part of an alluvial fan built up by Lone Tree Creek with the apex of the fan near the mouth of Lone Tree Canyon where the stream emerges from the mountains."

IDEALIZED AQUIFER

The Ogallala Formation in the vicinity of the Cheyenne well field has been represented as an idealized aquifer for the purpose of esti­ mating a coefficient of transmissibility that might be representative of the formation. Figure 9 shows the depression in the piezometric surface caused by pumping in the Cheyenne well field. The contours represent the drawdown of the piezometric surface during the period 1942-64. The zero contour represents the boundary of the area in­ fluenced by pumping in 1964. Section A-A' in figure 9 shows a marked change in gradient from 1942 to 1964, but the direction of ground-water movement continues to be from west to east.

Pickup of ground water in Crow Creek between Silver Crown and Cheyenne was reported to be 4,324,000 gpd (13.27 acre-feet per day) in November 1942 (Morgan, 1946, p. 30). However, during the pe­ riod 1961-64, Crow Creek was dry between Silver Crown and the eastern edge of the Cheyenne well field. Also, progressive drying of the higher springs has caused an eastward movement of the spring line (pi. 2). The ground water formerly discharged to the surface is now being diverted to the well field, and near-equilibrium condi­ tions have been established in the aquifer.

Water-level fluctuations and annual pumpage in the Cheyenne well field are graphed in figure 10. The hydrograph was compiled from the monthly average nonpumping water levels in the wells and is believed to be representative of the average water-level trend in the Cheyenne well field.

The water level declined only slightly during the years 1945-49 and 1961-64. It is assumed that the recharge-discharge relation in the area had reached near equilibrium during these periods. Therefore, the depression shown in figure 9 is assumed to be almost entirely the result of the increased pumping rate between the two periods. The

GROUND WATER 33

Base from Wyoming State Highway Department

6200' -

6100'

Hydrology by Marvin A. Grist, 1965

A'

DATUM IS MEAN SEA LEVEL

FIGUBE 9. Area affected by pumping and changes in the piezometric surface, 1942-64, in Cheyenne well field.

0

z <

/> 200 h

~-|

400

< <

600

Q. O§ u

- 80

° ~

Q- ° 1000 -

1200 -

1400

1600

1800 h

58

z3

62_

j£

66

> =

5 70

UJ

V)

^Q

7

4

£l <

7

8

< ^

82

uj 3

86C5

uj

< C

D 90

cc uj

94

CO O

FIG

UK

E 10. R

elat

ion o

f w

ater

lev

els

to a

nn

ual

pum

page

in

Che

yenn

e w

ell

fiel

d.

Pum

page

fro

m c

olle

ctio

n ga

ller

ies

not

incl

uded

.

GROUND WATER 35

difference between the average yearly pumping rates during the two periods of equilibrium is considered to be the average yearly inflow to the area of depression. This is about 1,800 acre-feet per year or a minimum inflow of about 27,000 acre-feet from 1950 to 1964, inclusive.

The total amount of water pumped from the area from 1950 to 1964 is estimated to be about 31,000 acre-feet. Subtracting the inflow from the amount pumped indicates 4,000 acre-feet of water was re­ moved from storage within the area. The volume of the aquifer dewatered is estimated from figure 9 to be 22.3 billion cubic feet. This was determined by multiplying the planimetered area between the contours by the estimated average thickness of the dewatered zone within each area. A specific yield of about 0.7 percent was calculated by dividing the amount of water removed from storage by the volume of the aquifer dewatered.

The Theissen-mean method (Theissen, 1911) was used to estimate the changes in saturated volume within the area. In this method a system of polygons is constructed around each well in which water- level measurements are made. It is assumed that the change in water level observed in a well is the change in water level throughout the area of the polygon surrounding that well and that the change in saturated volume can be attributed mainly to ground-water inflow into the area and does not reflect solely the recovery of the wells from a pumped- down condition. The polygon network used for the determination of the change in saturated volume is shown in figure 11. The changes in saturated volume were calculated by multiplying the change in water level by the area of the polygon. Water-level changes were measured January 28 and February 28,1964, because during the inter­ vening period the least number of wells was pumped. Interference occurs between many of the wells in the Cheyenne well field; however, computation of the change in saturated volume during February 1964 would probably be more reliable because less water was pumped dur­ ing that month than during any other that year. If a well was pump­ ing during Februray, the change in water level was estimated from the change in water levels observed during the months of November and December 1963.

If a part of the area shown in figure 11 is considered to be an aquifer bounded on one side by a fully penetrating stream and on the other side by a parallel ground-water divide, both of infinite length, and if it is assumed that the aquifer is regionally homogeneous and iso- tropic, then the coefficient of transmissibility for the area can be calcu­ lated using the equation of the steady-state profile (Jacob, 1943, p. 566) :

36 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

, _(a?W\ /2x tf\ flQ-\~2T~)\a a2)

whereW= constant rate of recharge to the water table. Recharge

to the area of depression between Crow Creek and the water-table divide is assumed to be approximately equal to the yearly inflow to that area.

a = distance from the stream to the ground-water divide. x = distance from the stream to a point where the altitude of

the water table is measured.AO altitude of the water table at point x, with respect to the

mean stream level.

If the altitude of the water table with respect to the mean stream level is measured at the ground-water divide, then x~a, and the foregoing equation becomes

The planimetered area of the polygons between the ground-water divide and Crow Creek was multiplied by the respective change in water level of each polygon to obtain the increase in saturated volume. During February 1964, the saturated volume increased about 16,900 acre-feet. The change in saturated volume multiplied by the specific yield of 0.7 percent is about 118 acre-feet. This is the estimated quantity returned to storage during February in the part of the area between the ground-water divide and Crow Creek. Assuming that the inflow is constant, the yearly inflow to this part of the area is estimated to be about 1,400 acre- feet.

The coefficient of transmissibility calculated with the above equation is about 3,800 gpd per ft. This is somewhat lower than the average coefficient of transmissibility of 16,000 gpd per ft determined from pumping tests. It is realized that many assumptions were based on meager data and that possibly some error may be induced by assuming that steady-state conditions exist during any one month. However, the coefficient of transmissibility (3,800 gpd per ft) calculated by the regional method appears to be a reasonable value for the formation. It would be expected to be lower than an average coefficient of trans­ missibility determined from pumping tests made on wells producing principally from highly permeable gravel zones. The large-yield wells were located by drilling many test holes and therefore are located in areas of relatively high permeability.

GROUND WATER 37

Approximate water-table divide of infinite- strip aquifer EXPLANATION

Observation well

Base from Wyoming State Highway Department

Hydrology by Marvin A. Grist, 1965

FIGURE 11. Polygon network used to estimate change in ground-water storage in vicinity of Cheyenne well field.

The steady-state profile method was used to determine an average coefficient of transmissibility of about 3,800 gpd per ft in the vicinity of the Cheyenne well field where 27 of the 28 pumping tests were made. Considering 3,800 gpd per ft as a conservative estimate of the average coefficient of transmissibility in the Cheyenne well field, a strip of the aquifer 10 miles wide is capable of transmitting 830 million gallons per year under a hydraulic gradient of 60 feet per mile. Pumpage at this rate should not lower the water table below its present level. An estimated 100 feet of saturation exists below the present draw­ down. Assuming that the gradient of 60 feet per mile and the cal­ culated premeability of 0.86 gpd per sq ft remain constant, an addi­ tional 830 million gallons per year could be pumped from a 10-mile- wide strip of aquifer by lowering the water table 50 feet. Intercep­ tion of this additional water would reduce the amount of discharge

38 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

from springs east of the well field, and the spring line would migrate farther eastward. Maximum yield from the Cheyenne well field is estimated to be about 1.6 billion gallons per year, which is probably a conservative estimate. This value approximates the maximum yield of 1.8 billion gallons per year estimated by a consulting firm in 1950, although the areas and permeabilities used in the methods of calcula­ tion were considerably different.

At least three irrigation wells east of Cheyenne and two north of Cheyenne are believed to derive water principally from the Ogallala Formation. Reported yields range from 150 to about 1,000 gpm. Un­ doubtedly, such yields can be obtained only from sand and gravel lenses because the indicated average coefficient of transmissibility of the Ogallala is small. Stock and domestic wells yielding as much as 50 gpm can probably be drilled in the Ogallala ait most locations, ex­ cept in the eastern part of Laramie County near the Nebraska border and near the edge of escarpments where the formation is drained.

Conclusions. Coefficients of transmissibility for the Ogallala For­ mation, determined by 28 pumping tests, ranged from 1,730 to 38,300 gpd per ft and averaged about 16,000' gpd per ft. All the tests except one were made using moderate- to large-yield wells that produce from sand and gravel stringers and lenses. The average coefficient of trans­ missibility as stated above, may be too high if applied to all the Ogal­ lala in Laramie County, because only a very small percentage of the wells drilled in this formation penetrates the highly productive zones.

It is believed that the coefficient of transmissibility determined by the regional method is 'better than the average obtained from pumping tests for the Ogallala in Laramie County for the reasons listed below.1. Data obtained from pumping tests in the Ogallala are difficult to

interpret, and the results of the interpretation may be misleading.2. All but one of the pumping tests were made at large-capacity wells

completed in sand and gravel lenses. Many unsuccessful test holes were drilled to find the highly productive zones.

3. The assumption that the aquifer is regionally homogeneous and iso- tropic is more valid than similar assumptions made to permit use of pumping-test data to determine aquifer characteristics in the Ogallala. Local heterogeneity was revealed by pumping tests made by Theis (1941, p. 15) and by the T-day tests made by the authors in 1964.

ALLUVIUM

The lithologic characteristics of the alluvium are similar throughout Laramie County, and the permeability of the alluvium is of the same order as that of the older terrace deposits. The Pine Bluffs lowland is the principal area where the alluvium will yield large supplies of

GROUND WATER 39

water to wells. In most other areas the alluvium is thin and may not be saturated. Large yields have been obtained from wells in the ter­ race deposits along Horse Creek and from collection galleries in the flood-plain deposits of Crow Creek. A yield of 450 gpm has been ob­ tained from well 13-70-15cba in wet years. This well probably pro­ duces from both alluvium and weathered granite.

Aquifer characteristics of the older terrace deposits near Carpenter, Wyo., determined from three pumping tests, are shown in the follow­ ing table.

Location ofpumped well

12-62-2bcb-_______

3bcc._ ......22abb __-_-_

Distance ofobservation well

from pumped well

Coefficientof trans-

missibility(gpd per ft)

105, 000146, 000

53, 30059, 00044,800

Coefficientof storage

5. 43X10-2

4. 65X10-3

Specificcapacity

(gpm per ftof draw­down)

58.0

37.413.9

Length oftest

hr min97 1597 15

7 3584 1584 15

Date oftest

1964April 29.

Do.April 28.May 21.

Do.

The saturated thickness of the terrace deposits in the three wells tested ranges from about 33 feet at well 12-62-2bcb to about 85 feet at well 12-62-22abb. The coefficient of permeability ranges from 3,180 to 694 gpd per sq ft, respectively. Figure 12 is a generalized satu­ rated-thickness map of the terrace deposits in the vicinity of Carpenter, Wyo. Many large-yield irrigation wells in the area tap more than 40 feet of saturated material, and at least seven wells, with reported yields of 400-700 gpm, penetrate 30-40 feet of saturated material. Addi­ tional large-yield wells tapping more than 30 feet of saturated mate­ rial could possibly be developed within the area.

THE WATER TABLE

CONFIGURATION

Plate 2 is a contour map of the piezometric surface in Laramie County showing the location of wells and springs used for control in drawing the contours. Pertinent data regarding most of the wells and springs are given in the section "Records of Selected Wells and Springs"; data on some wells have been published previously and are therefore omitted. Most of the water-level measurements were made during 1963 and 1964. In some areas, control was supplemented by older measurements that were assumed to be representative of that area.

Hydraulic connection between the Tertiary formations is sufficient to permit contouring a common water table. On the western edge of

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GROUND WATER 41

the county the piezometric surface has been extended, particularly in the southwestern corner, to include the water level in pre-Tertiary rocks where there was control.

Ground water moves in the general direction of the slope of the piezometric surface, and the rate of movement is dependent on the slope (hydraulic gradient) and the permeability of the aquifer. The slope of the piezometric surface averages 'about 40 feet per mile, but it is considerably different in some areas in Laramie County owing to the difference in permeability, thickness of the water-bearing materials, and amount of water moving through the beds.

Drainage systems influence the configuration of the water table. This is particularly noticeable along Chugwater Creek, Horse Creek, and the upper reaches of Crow Creek. The contour lines along Crow Creek (pi. 2) show the stream is effluent (receives water from the for­ mation) west of Cheyenne and is influent (discharges water to the formations) in the lower reaches. Pumping in the Cheyenne well field has lowered the water table so that Crow Creek is dry between Silver Crown and sec. 18, T. 14 K, E. 67 W. This, however, has not changed the regional drainage pattern of ground water in this area. The change in the piezometric surface due to pumping (discussed in section on hydraulic properties of the Ogallala Formation) in the Cheyenne well field was less than 50 feet; therefore, because the contour interval of plate 2 is 50 feet, the map does not reflect the influence of pumping.

East of Cheyenne, Crow Creek is perennial nearly to Carpenter except when the flow is diverted for irrigation. Surface flow ceases in sec. 36, T. 13 N., K. 63 W., where all the flow seeps into the terrace deposits. Chugwater and Horse Creeks are effluent streams and are the only perennial streams crossing the county; all Others are inter­ mittent.

The water level in the terrace deposit north of Horse Creek in T. 18 N., Ks. 61 and 62 W., is higher than that in the adjacent White River Formation because of recharge received from surface-water irrigation. Some of the water may percolate downward to contribute recharge to the White Eiver Formation.

FLUCTUATION

Fluctuations of the water level in an aquifer are attributed mainly to recharge and discharge. Only the more significant water-level trends in Laramie County are discussed in this report. Additional information is available in other ground-water reports on various parts of the area and in the annual water-level reports of the Geologi­ cal Survey.

42 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

A graph of the water level in well 18-66-31ccc, which taps the Ari- karee Formation, is shown in figure 13. The water-level fluctuations in this well are slight; they are caused by changes in atmospheric pres­ sure. Barometric-pressure readings at the Cheyenne Airport, taken at the same time as the water-level measurements for November and December, are shown for comparison in figure 13. The magnitude of water-level fluctuations measured in several wells during the investiga­ tion suggests that barometric pressure was the cause of fluctuation.

Although 1964 was one of the driest years of record in Laramie County, lack of recharge did not cause a decline in water levels in the Tertiary formations, except perhaps for the White River Formation in the Pine Bluffs lowland. Water levels in most of the Tertiary formations are probably sensitive only to long-term trends in precipitation.

Graphs of water levels in well 14-67-18ddc, in the Cheyenne well field, and well 14-60-5bcb, in the Pine Bluffs lowland (fig. 14), show the effect of seasonal pumping. The slow recovery of the water level in well 14-60-5bcb in the latter part of 1964 might seem to indicate lack of recharge among other things; however, most of the recharge occurs in the spring, and the slow recovery is mostly the result of pumping late in the year.

Long-term water levels in the Cheyenne well field and the Pine Bluffs lowland are shown graphically in figure 15. No significant change in water levels for the period of record has occurred in the Pine Bluffs area. In the Cheyenne well field, there was an initial decline with a subsequent leveling off at a point where recharge and natural and artificial discharge reached a new equilibrium. The zero

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GROUND WATER 45

contour in figure 9 shows the extent of the area in which the Cheyenne well field influenced the water level in 1964. Water levels in the Federal well field, which are not included in the averages shown in figure 15, declined greatly the first year of pumping. However, in subsequent years, levels fluctuated less, and the water now recovers to nearly the same level each winter.

RECHARGE

Precipitation. Morgan (1946, p. 19) estimated the recharge from precipitation to be about 0.83 inch per year in the vicinity of Cheyenne, Wyo., or about 5.5 percent of the average annual precipitation. Kapp, Warner, and Morgan (1953, p. 22) used the same estimate for the Egbert-Pine Bluffs-Carpenter area. Assuming that recharge from precipitation in Laramie County is'about 5 percent of the aver­ age annual precipitation and that the average annual precipitation is about 15 inches, the annual recharge from this source in Laramie County (2,709 sq. mi.) would be about 108,400 acre-feet.

/Streams. Recharge to the ground-water reservoir is also contri­ buted by streams that head in the mountains west of the county line. Stream discharge is usually maximum during April, May, and June because of spring runoff. Seepage runs (measurement of gain or loss of streamflow) were made during May and June 1964 on six streams that flow over sedimentary rocks of pre-Tertiary age in the western part of the county. Data in the following table show that these rocks are capable of accepting recharge from the six streams at the rate of at least 5.46 cfs (cubic feet per second). The rate of seepage is prob­ ably greater when surface runoff occurs. Evapotranspiration losses combined losses due to evaporation from land and water surfaces and transpiration by plants are included in the seepage figure. However, these losses are probably small because the distance between the points of measurement of streamflow is short (about half a mile) and the vegetation is sparse.

Date of measurement

1984

May 27. .... .

Do. ..Do. .....

June 16 .........June 18 __ ....

Total... .

Stream

Discharge upstream

from outcrop of pre-Tertiary

sedimentary rocks (cfs)

15.50

.062.021.331.98

Discharge downstream from outcrop

of pre-Tertiary sedimentary rocks (cfs)

12.5900.32.95

1.79

Recharge to pre-Tertiary sedimentary rocks (cfs)

2.91.22.06

1.70.38.19

5.46

Records of Laramie County Water Commissioner.

46 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

Foley (1943, p. 51) estimated recharge to the Ogallala Formation of Tertiary age from Duck, Goose, and Lone Tree Creeks to be about 2.5 million gallons per day (3.87 cfs). Rapp, Warner, and Morgan (1953, p. 20) estimated that streamflow annually contributes 8,000 acre-feet (11.05 cfs) of recharge to aquifers in the Egbert-Pine Bluffs lowland and the Carpenter area.

DISCHARGE

Ground water in Laramie County is discharged by flow into streams, seeps, and springs; by evapotranspiration; and by pumping wells. Some also leaves the county as underflow.

/Seeps and springs. Many seeps and springs in the Ogallala For­ mation in the western part of the county supplement surface flow in the tributaries to Crow and Lone Tree Creeks. Lines drawn through the eastern boundary of these seeps and springs, as they existed in 1942 and as they currently exist, are shown on plate 2. Morgan (1946, p. 14) related the spring line to the approximate eastern boundary of an area underlain by an appreciable thickness of permeable water-bearing beds. Eastward movement of water in the more permeable beds is impeded where these beds lens out and, eventually, some of this water discharges at the surface as seeps and springs. The eastward migra­ tion of the spring line between 1942 and 1964 is attributed to a de­ crease in the amount of water moving through the beds because of pumping in the Cheyenne well field. Even though the more perme­ able beds lens out, the permeability of adjacent rocks is great enough to transmit this lesser amount of water farther east before the perme­ ability is reduced to such an extent that the formation cannot transmit all the water.

Foley (1943, p. 51) also noted that seeps and springs occur along the escarpment south of the Colorado-Wyoming State line and in some of the valleys that cut back into the escarpment. These are con­ tact seeps 'and springs occurring near the base of the Ogallala Formation. Several contact springs occur near the Ogallala-Arikaree contact on the south side of Horse Creek. Springs that occur near the contact of these two formations in the south half of T. 14 N"., R. 62 W., are the beginning of perennial flow in Muddy Creek. A few springs occur in the Pine Bluffs lowland at the contact between the White River Formation and the overlying terrace deposits.

A large spring in sec. 8, T. 13 K, R. 69 W., yielding nearly 2 cfs from the Casper Formation was developed by the Union Pacific Rail­ road to supply water for steam engines. Since the use of steam engines has been discontinued by the railroad, only enough water is pumped from the spring for domestic supplies at Granite and Harri-

GROUND WATER 47

man, Wyo. Most of the discharge flows into the South Fork of South Crow Creek and is diverted for irrigation. The aquifer from which the spring issues is probably recharged by seepage from streams, principally Lone Tree Creek which flow across the Casper outcrop.

Streams. The average annual discharge of Lodgepole Creek is 13 cfs, or about 9,410 acre-feet per year, for the 32 years of record at a gaging station near Bushnell, Nebr., about 10 miles east of Pine Bluffs. Eapp, Warner, and Morgan (1953, p. 26) estimated the underflow at the gaging station to be 1.5 cfs. Total discharge from the area above the gaging station, therefore, averages 14.5 cfs, or nearly 10,500 acre- feet per year.

The contour lines on plate 2 show that the other streams, partic­ ularly Horse and Chugwater Creeks, obtain part of their flow from ground-water discharge.

Underflmv. Underflow from the county through the Tertiary and younger rocks is predominantly through flood-plain deposits under­ lying the principal streams and through terrace deposits in the Pine Bluffs-Carpenter area. The only other area where much water probably leaves as underflow is in the north-central part of the county, where there is as much as 200 feet of saturated Arikaree Formation (pi. 2). No data are available on movement of water through pre- Tertiary formations.

Wells. Most large-yield wells are in the Cheyenne and Federal well fields, and in the irrigation area near Pine Bluffs and Carpenter. There are probably not more than 20 large-yield wells elsewThere. However, small-yield wells can generally be developed throughout the county.

Records show that about 4,576 acre-feet of water was pumped from all the Cheyenne municipal wells in 1964. The amount of water pumped in 1964 by other municipalities and communities was esti­ mated to be as follows:

Estimatedgroundwater

pumped,1964

Community (acre-feet)

Fox Farm!________________________.___-____--__-- 466Orchard Valley I ------ - ----- --- 492Burns._________________________________------_--- 98Albin________ _________ --__ -- --- ---- 58Pine BluflFs_____---_--__-------_.----------------- 381

Total..-_-______-__---_------_------------- 1, 495i Adjacent to Cheyenne.

An estimated 17,000 acre-feet of water was pumped for irrigation in the Pine Bluffs-Carpenter area in 1964. All other uses of ground water in the county (including irrigation outside the Pine Bluffs-

48 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

Carpenter area) probably do not exceed 5,000 acre-feet per year. Total ground-water discharge from wells in Laramie County was estimated to be about 28,000 acre-feet in 1964.

Evapotranspiration. Estimates of soil-moisture losses by evapo- transpiration in Wyoming have been computed by the U.S. Depart­ ment of Commerce and the U.S. Department of Agriculture. At Cheyenne and Pine Bluffs, estimated evapotranspiration losses range from 9.0 to 10.3 inches per year, assuming a 2-inch available-water capacity for annual 32°F and 28°F frost-free seasons, respectively; and from 9.5 to 12.1 inches per year, assuming a 6-inch available-water capacity for annual 32° F and 28° F frost-free seasons, respectively. The frost-free season is the average number of days between the last occurrence of this temperature in the spring and the first occurrence in the fall. Available water capacity, stated as inches of water, is the difference between the amount of water remaining in the soil after the soil has been saturated and allowed to drain freely, and the amount of water left in the soil when plants growing in that soil first show permanent wilting.

The estimates given above are soil moisture losses due to evapotrans­ piration and do not necessarily reflect direct loss of ground water. However, water lost to the atmosphere cannot contribute to ground- water recharge. In areas where the water table is near the land sur­ face, much ground water is lost by evapotranspiration. Evapotrans­ piration losses in such areas were estimated to range from 17.1 to 18.8 inches per year at Cheyenne and from 18.0 to 20.2 inches per year at Pine Bluffs, for annual 32°F and 28°F frost-free seasons, respectfully.

Summary. Eecharge to the ground-water reservoir in Laramie County is derived principally from precipitation and is estimated to be about 108,400 acre-feet per year. Streams contribute only a small additional amount of recharge, perhaps about 5,000 acre-feet per year. Yearly discharge of ground water by pumpage in Laramie County is estimated to be about 28,000 acre-feet. The balance of the recharge leaves the county by other means an estimated 20 percent by stream- flow, 20 percent by underflow, and 60 percent by evapotranspiration.

FUTITBE DEVELOPMENT

Ground water is extensively developed in Laramie County, but con­ centrated development is limited to three areas Cheyenne well field, Federal well field, and the Pine Bluffs lowland. Additional supplies of water can be developed in most areas, but the potential for large yields is limited and exploratory drilling may be required.

GROUND WATER 49

Precambrian rocks of the Laramie Kange will yield adequate sup­ plies for domestic and stock use in many places if "well sites are selected carefully. Small yields may also be obtained from the Mesozoic formations, which are at or near the surface along the mountain front and in the northwestern part of the area. Large yields might be obtained from the Casper Formation at economical drilling depths in some areas near the mountains.

The White Kiver Formation will probably yield small quantities of water to wells nearly everywhere in Laramie County and large yields are possible in some areas, particularly where pipes have formed (see p. 27) and where the formation contains gravel deposits in which wells can be completed.

The Arikaree Formation, which has not been developed extensively in Laramie County, will yield large supplies of water to wells in places. The formation is comparatively homogeneous and is the most predictable aquifer in the area. Although data are meager, yields from the formation can probably be predicted fairly accurately by the combined use of the saturated thickness map (pi. 2) and the probabil­ ity curve (fig. 8). Unless wells in the Arikaree are properly con­ structed, loose fine sand may enter them.

Small to large supplies of water can be developed from the Ogallala Formation. The formation's average transmissibility is low, but its sand and gravel lenses will yield large quantities of water. One of the best areas for developing large supplies of water is where a maximum saturated thickness of both Ogallala and Arikaree Formations is present. To obtain maximum yields, with minimum pumping lift, wells should be drilled completely through both formations.

The alluvium will yield small supplies of water in much of the area, and it may be the best source of water in, and near, the moun­ tains. Large supplies can probably be developed from alluvium under­ lying the flood plains of some streams and from the terrace along the lower part of Horse Creek. Intensive development of ground water in the Pme Bluifs area causes considerable interference between wells during the irrigation season. However, water levels are not permanently lowered and generally recover to about the same level each spring. Many of the wells are marginal producers because of the small amount of saturated gravel. During summer, water levels decline so much that some wells can be pumped only intermittently or at a reduced discharge. Further development would aggravate this situation. Similar interference and reduced yields will occur wher­ ever there is large ground-water development in areas of small sat­ urated thickness.

50 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

CHEMICAL QUALITY OF GROUND WATER AND OF SURFACE WATER

By JOHN R. TILSTKA

CHEMICAL CHABACTEEISTICS OF WATEE

The amount and type of chemical constituents in water are generally determined by the solubility and physical properties of the materials in contact with the water, the duration of contact, the temperature of the water, and the pressure under which it is confined. The most abun­ dant chemical constituents in ground water and surface water are generally sodium, calcium, magnesium, bicarbonate, sulfate, chloride, and silica. However, iron, manganese, postassium, fluoride, and nitrate are commonly present in trace amounts.

Chemical-quality data collected during 1960-64 are given in tables 3 and 4. Most of the recent samples are from the Cheyenne municipal well field and from wells in the Carpenter-Pine Bluffs area. (See pi. 2.) In addition, about 100 older analyses, some of which have been published by the U.S. Geological Survey, supplement the new data.

Concentrations of chemical constituents are expressed as parts per million. One part per million is the unit weight of a constituent in a million unit weights of water. Specific conductance and sodium-ab­ sorption-ratio (SAR) are used in evaluating water for irrigation use. The specific conductance of water is a measure of its ability to conduct an electric current and is directly proportional to dissolved-solids con­ tent (salinity). Sodium-absorption-ratio expresses the amount of exchangeable sodium in water.

CLASSIFICATION OF WATER USE

DOMESTIC USE

Water for domestic use should not have objectionable taste, odor, or color, and should not contain excessive amounts of biological and chemical constituents that may be physiologically harmful. The U.S. Geological Survey generally uses the U.S. Public Health Service standards for interstate common carriers (U.S. Public Health Service, 1962) as a guide for evaluating the suitability of domestic supplies. The following table lists the chemical constituents that commonly occur in water and gives the recommended limit for a public supply.

Maximum permissible

concentration Constituent (ppm)

Iron (Fe)_-__-____-________.______________________ 0. 3Fluoride (F)______________________________________ ' 1. 5Nitrate (NO3)__ _-.__-_.--___...___---____-__-.-__ 45Sulfate (SO4)_- -------_---_------_----------__--- 250Chloride (Cl) ______-___-_____________.___-----____ 250Dissolved solids.___-_______________-_____----___-_ 500

1 Estimated maximum for Laramie County (U.S. Pub. Health Ser., 1962).

CHEMICAL QUALITY OF WATER 51

Hardness is a property of water that causes soap to form an insoluble curd. Several chemical constituents cause hardness, but the degree of hardness for most water can be estimated from the concentration of alkaline earths, such as calcium and magnesium. The U.S. Geological Survey uses adjective ratings to describe hardness attributed to CaCO3 . Thus, soft water contains 0-60 ppin; moderately hard, 61-120 ppm; hard, 121-180 ppm; and very hard, more than 180 ppm.

Concentration ranges for some of the principal aquifers are com­ pared with the U.S. Public Health Service standards in the following table.

Concentrations, in parts per million

Constituent

Iron __ .._ ________Fluoride _ ___ ___

Sulfate. -_ Chloride-- .Dissolved soilds. _____

White River Formation

0.00- 1.1.4 - .9

1. 0 - 133. 8 - 742. 5 - 13

208 -42498 -264

12

Arikaree Formation

0.03- 0.14.6 - .7

8. 7 - 2612 - 273. 9 - 16

286 -330

3

Ogallala Formation

0.02- 5.8.3 - .9

1. 6 - 16.3-30

1. 0 - 17167 -308125 -219

13

Alluvium

0.00- 0.19.6- 1.0

5. 8 - 1716 - 65

5. 4 - 27260 -486152 -317

5

U.S. Public Health Service

standards

0.31.5

45250250500

INDUSTRIAL USB

Water-quality requirements for industrial use depend on the type of industry and the specific use of the water. For example, quality requirements of water used for coolant purposes will differ signifi­ cantly from requirements for food and beverage manufacture. Gen­ erally, if the water is soft and satisfies the U.S. Public Health Service, standards, it will also be satisfactory for most industrial uses.

IRRIGATION

The amount and type of chemical constituents should be considered in appraising water for irrigation use. However, water quality is not the only criterion in determing whether land should be irrigated climate, soil drainage, soil and crop types, and water management may affect agricultural productivity to a greater extent.

According to the U.S. Salinity Laboratory Staff (1954), the chem­ ical characteristics most important in the appraisal of irrigation sup­ plies are: (1) Total concentration of dissolved minerals or salts; (2) sodium concentration and relative proportion of sodium to other ca­ tions; (3) concentrations of boron and other elements that may be toxic; and (4) under some conditions, the bicarbonate and carbonate concentrations as related to the calcium and magnesium concentra­ tions (residual-sodium-carbonate),

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31 6.9

2.8

2.0

0.0 .0

688

625

12

100 0

1,10

0 1,

010

8.5

8.6

34

3410

.06

§

8.98

g M SJ

W

hite

Riv

er F

orm

atio

n

13-6

0-18

dda

2.....

13

-63-3

3cb

b-_

13

-69-

16cb

d s_

. ...

17da

a3...

..

14~6

0-28

bbb2

____

15

-60

-34

bcb

34

dac_

_ _

_34bdb

15

-69-6

ada_

...

21dc

c.._

18-6

2-9b

dc__

. _

100

315

555 93

315

318

182

223

312

6-26

-64

6-26

-64

4-21

-61

6-9

-61

8

-7-6

4

7-7

-64

5- 2

-62

5- 2

-62

8-11

-64

8-11

-64

8-11

-64

6-27

-«4

51 40

45

53

53

52

52

49

49

46

58

58

55

52

59

58

61

23

27

58

0.03 .00

.29

.02

.00

.00

1.1 .26

.01

.05

.06

35

47

81

40

24

32

49

30

50

8.9

6.2

15 8.8

9.2

12

16 6.8

7.8

48 11 24

12

2 1 16

47

18

41

S 5.

3 4.

5 3.

4 9 2

3.2

3.1

5.5

218

172

152

172

290

154

160

151

249

219

206

288

0 0 0 0 0 0 0 0 0 0 0 0

74

12

20 as 44

16

14

12

13

16

17

62

6.5

2.5

13 9.3

5.7

6.7

3.6

7.4

5.6

0.4 .4

.6

.5

.7

.6

.6

.6

.9

8.8

6.0

13

12 6.6

8.5

3.2

1.0

2.5

0.24

.1

6

.05

.04

.04

396

260

240

208

390

234

234

232

257

252

274

424

194

156

124

143

264

136 98

128

187

103

157

232

15

15 0 2 26

10 0 4 0 0 0 0

600

367

326

307

594

333

313

320

419

399

385

608

8.0

7.8

7.3

7.4

7.7

7.5

7.7

7.6

7.9

7.7

7.6

7.5

1.5 .4

.7

.2

.6

.4

1.3 .5

.5

2.0 .6

1.2

ro.o

o C

.00

g

.01

&

.00

g.00

S

.00

.66

n

.91

O

.34

cl

1.53

g

.24

3

08

1.4

Ari

kare

e F

orm

atio

n ^ J

14~

62-7

dbb_

14-6

4-2

8baa

. -

17-«

0-20

abb_

_-

6-26

-64

6-26

-64

6-27

-64

49

460.

14

.03

21

5140

14

12

16 9

4.4

3.0

208

218

184

\ 0

27

12

19

16 3.9

0.7 .6

26 8.7

0.58

.0

333

0 28

6 29

4

216

185

170

45 6 19

476

389

408

7.8

7.8

7.4

0.4 .2

.5

O

0.00

.0

0 .0

0

Ogallala For

mati

on

13-64-23aaa.--

23daa._ _

13-6

7-16

bcc-

--

13-68-4a

dC-.

-

14-6

7-18

cbd-

-

14-6

8-14cad.--

23ddc

27dcc.--._.

16-6

5-3b

bb<-

-.-

Qppn 4

16-68-2daa.

300

338

185

255

225

163

250

250

194

513

638

459

473

5- 2-62

5- 2-62

8-10-64

8-11-64

8-11

-64

8-11

-64

8-11-64

8-11-64

8-11

-64

6-8-61

10-2

8-60

4-14-61

9-8-60

54

56

51

51

51

50

50

52

54

40 40

40

57

65

27

24

27

40

28

30

20

51

52

23

24

0.03

5.8 .07

.05

.04

.02

.06

.07

.15

1.3

1.4 .34

.09

54

44

34

47

53

67

45

47

41

51

46

43

44

13

11

22 6.7

6.8

13 5.5

5.0

5.5

6.6

7.8

5.5

6.1

9 14

9.0

5.0

9.1

9.4

4.4

5.9

5.0 2.

6 7 8.

7

3.1

1.7

3.9

3.7

2.0

2.1

1.7

8 0 8 5

218

182

172

167

184

240

157

169

149

182

176

162

164

0 0 0 0 0 0 0 0 0 0 0 0 0

11

15

18 8.0

19

30 6.5

6.0

6.0 .3

4.8

8.0

8.5

6.4

6.2

17 2.6

3.8

6.0

2.8

2.5

1.6

2.1

2.7

1.5

1.0

0.4 .6

.5

.4

.7

.9

.4

.4

.6

.5

.3

.8

.8

8.4

16 8.3

6.9

5.7

1.6

7.0

6.8

3.9

7.5

7.6

1.8

8.3

0.07

.0

2 .06

.05

.02

.03

.02

286

281

241

201

214

308

191

189

167

218

223

175

181

186,

15

6 175

145

160

219

135

138

125

154

147

130

135

7 7 34 8 9 22 6 0 3 5 3 0 1

407

379

386

302

354

452

281

294

262

314

311

278

292

7.4

7.5

7.7

7.7

7.6

7.9

7.4

7.6

7.8

7.5

7.5

7.9

7.4

0.3 .5

.3

.2

.3

.3

.2

.2

.2

.1

.2

.3

.3

0.00

.00

.00

.00

.00

.00

.00

.01

.00

.00

.00

.06

.00

Allu

vium

12-6

2-2b

cb. ..

.13

-62-

29cc

c2...

_-14-6

0-1

0ac

c _ ..

.ll

bcc--

.

104 80

6-26

-64

6-26

-64

6-26

-64

8- 7

-64

6-22

-64

52 53

46 53 50 >?fi

0.04 .19

.07

.00

.02

46 48 109 53

9.0

12 11 is

14 13 30 45 77

5.2

4 S

8.9

10

183

190

320

403

348

0 0 0 0 0

16 16 65 43 65

5.4

6 9

16 27 11

00

1.0

1.0 .6

12 17 5.8

8.0

0.08 .05

.41 94

.

260

276

322

486

474

152

170

297

317

208

2 14 35 0 0

364

389

674

774

697

7 S

7 S

7.9

7.5

7 S

0.5 .4 1.1

2.3

0 0( .ra Of .2"

1 Wat

er is

pri

ncip

ally

from

Lan

ce F

orm

atio

n, a

lthou

gh s

ome

is fr

om W

hite

Riv

er F

orm

atio

n.2 P

roba

bly

repr

esen

ts w

ater

from

the

over

lyin

g al

luvi

um.

3 Wat

er is

pri

ncip

ally

from

Whi

te R

iver

For

mat

ion,

alth

ough

som

e is

from

Lan

ce F

orm

atio

n.4 M

ixtu

re o

f wat

er fr

om O

galla

la a

nd A

rika

ree

Form

atio

ns.

Cn

CO

TA

BL

E 4.

Ch

emic

al

analy

ses

of

surf

ace

wat

er i

n L

ara

mie

County

, W

yo.

[Res

ults

in p

arts

per

mill

ion

exce

pt a

s in

dica

ted.

A

naly

ses

by U

.S.

Geo

l. Su

rvey

]

Loc

atio

n of

sa

mpl

ing

site

Cro

w C

reek

nea

r Si

lver

Cro

wn

(14-

68-1

9a)-

~

Bel

ow H

eref

ord

Ran

ch R

eser

voir

1

(13-

66-1

c)-

--

Sout

h F

ork

Lod

ge-

pole

Cre

ek n

ear

Fed

eral

(15-

69-3

C)-

H

orse

Cre

ek:

Nea

r H

orse

Cre

ek,

Wyo

. (1

7-69

-30C

)

Nea

r H

orse

C

reek

oil

fiel

d (1

7-68

-21a

)-

Nea

r U

.S.

Hig

hway

87

(17-

67-l

c)- -

Nea

r M

erid

en

At

Gos

hen

Cou

nty

line

(1

8 6

1-l

b)

--

Chu

gwat

er C

reek

ne

ar F

arth

ing

(19

70-3

5a) -

-----

Bea

r C

reek

nea

r L

a G

rang

e, G

oshe

n C

ount

y (1

9-61

-6C

).

Estimated

discharge (cfs

)

<1 2

<1 2 3 1 3 5 5 3

.5

Silica

(Si02) 19 45

17

H o M i i

0.33

.08

.04

.04

.14

Calcium

(Ca)

118 44

140

Magnesium

(Mg)

32 9.7

33

I"a a ' § 02

1 K

100 11 32 9O 9Q 14 40

35 «O

g 'o PH 3.6

7.0

2.7

Bicarbonate

(HCOa)

258 79

264

329

260

303

192

258

302

271

Carbonate

(COs) 0 39

0 0 0 0 0 0 0 0

Sulfate

(SO4) 17

96

15

207

105 91

19 23

295 17

Chloride

(Cl)

3.5

5.5

5.1

Fluoride

(F)

1.4 .8

.4

Nitrate

(NOs)

0.3

1.4 .2

Boron

(B)

0.09 .1

9

.18

Dis

solv

ed

solid

s

Residue

at 180°

C

(ppm

)

288

522

272

584

398

402

232

290

694

300

Tons per

acre-

foot

0.39

.71

.37

.79

.54

.55

.32

.39

.94

.41

Hardness as CaCOs

205

164

212

427

266

285

150

150

486

114

Noncarbonate hard­ ness as CaCO

s 0 34 0

157 53 37 0 0

238 0

Percent

sodium 14

57

10

14

19 18

17 35

13 54

Sodium-adsorption- ratio

(SAR

)

0.5

3.4 .3 .7

.8 .7

.5 1.4 .7

2.5

Specific

conductance (micromh

os at

25°

C) 443

803

435

860

601

634

348

453

975

449

W P. 8.0

9.5

8.0

8.1

8.0

8.1

7.4

8.2

8.0

8.2

Residual-sodium- carbona

te (RSC

)

0.13

.00

.09

.00

.00

.00

.15

1.23

.00

2.16

o » §

CHEMICAL QUALITY OF WATER 55

The U.S. Salinity Laboratory classifies irrigation water according to its salinity and sodium hazard (fig. 16). Nearly all the water samples collected during this study are of medium-salinity and low-sodium hazard classification (C2-S1). Medium-salinity water (C2) can be used if a moderate amount of leachinng occurs. Plants that have mod- crate salt tolerance can generally be grown without special practices for salinity control. Low-sodium water (Si) can be used for irri­ gation on almost all soils with little danger of development of harmful levels of exchangeable sodium.

E-esidual-sodium-carbonate (RSC) and boron concentrations are not sufficiently high to cause adverse soil conditions or affect crop yield. This does not imply that levels of RSC or boron are particu­ larly low, but rather that drainage in the developed and potential agricultural areas is generally adequate to accommodate present levels.

QUALITY OF GROUND WATER

Chemical composition must be considered when ground-water sup­ plies for various uses are evaluated. Most analyses in table 3 are of water from formations and localities where large supplies occur. The chemical quality of this water is suitable for domestic, stock, and irrigation use; however, softening is desirable if the water is used for laundering.

Few data on the chemical composition of water from pre-Tertiary rocks are available. The Casper Formation, near the outcrop in the western part of the county, is known to produce water of suitable quality for domestic and irrigation use. Previous U.S.* Geological Survey investigations in areas adjacent to Laramie County indicate that water from the Lance and Fox Hills Formations is inferior for most uses.

The chemical composition of water from Tertiary and Quaternary rocks does not differ appreciably from one formation or locality to another. Most analyses (table 3) represent water from a single for­ mation, whereas a few represent water from two or more formations. For example, several of the wells tapping the White Eiver Formation in the Carpenter-Pine Bluffs area probably also derive some water from the alluvium. However, the extent to which this mixing occurs cannot be determined owing to the similarity in chemical composition of water from these formations.

Irrigation tends to deteriorate the quality of water in two ways: (1) Much of the water applied in irrigation is lost by evaporation from the land surface and by plant transpiration, causing some solutes (salts) to remain on the land surface and in the plant-root zone. Subsequent applications of water leach these solutes out of the soil by

56 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

100 2 345678 1000 2 34 5000

30

28

26

24

22

I 20os 18cc z

8 14

|l2 a

10

8

6

4

2

C1-S4

C1-S3

C1-S2

C1-S1

iiIIr TI

C2-S4

C2-S3

C2-S2

C2-S1

C3-S4

C3-S3

C3-S2

C3-S1

r^ \ v

C4-S4

C4-S3

C4-S2

C4-S1

100 250 750 2250CONDUCTIVITY, IN MICROMHOS PER CENTIMETER

(EC xlO 6 ) AT 25°C_________1

LOW MEDIUM HIGH VERY HIGH

SALINITY HAZARD

EXPLANATION

Ogallala Formation Lance Formation Arikaree Formation

Alluvium White River Formation Surface water (streams)

FIGUBE 16. Classification of irrigation water.

RECORDS OF SELECTED WELLS AND SPRINGS 57

seepage and increase mineralization of the ground water. (2) Some animal and chemical fertilizers applied to the land surface are leached into the aquifer, also increasing the mineralization and possibly con­ taminating the water in the aquifer to the extent that it may no longer be suitable for domestic supplies.

Water from two wells in the Cheyenne municipal well field 'and two wells in the Carpenter-Pine Bluffs area, analyzed in 1947, was re­ analyzed in 1964 to determine if quality had deteriorated. The data indicate very little change in chemical composition of water from the Cheyenne well field 'and the Carpenter area; however, water from an irrigation well (14-60-1 Ibcc), about half a mile northeast of Pine Bluffs, showed 'an increase in dissolved solids from 302 ppm (1947) to 486 ppm (1964).

Water from some of the irrigation wells in the Carpenter-Pine Bluffs area has relatively high (about 10 ppm) concentrations of ni­ trate, which are probably due to pollution from chemical and organic fertilizers.

QUALITY OF SURFACE WATER

Chemical composition of surface waiter in Laramie County is largely influenced by ground-water inflow and seepage, and by irrigation use. Although the quality of the water is generally suitable for irrigation use, streamflow during the irrigation season is sufficient only for lim­ ited irrigation on the stream flood plains.

Analyses of water from the principal streams (table 4) indicate a relatively wide range in chemical composition, not only from one stream to another but also along the reach of a particular stream. Horse Creek was sampled at five sites during June 23-27, 1964, and, although concentrations of principal constituents differed from place to place, all the water sampled was of a calcium bicarbonate type.

The chemical composition of streams is affected by runoff from snowmelt and rainfall, but these effects are generally of short duration. During high runoff, the streams are generally less mineralized than during base-flow conditions. Chemical composition is also influenced by return flow from irrigated areas.

58 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

RECORDS OF SELECTED WELLS AND SPRINGS

Location: See description of well-numbering system (p. 3).Depth of well: Depths are given in feet below land-surface datum.Geologic source: p-Cr, Precambrian rocks; P pc, Casper Formation;

Kl, Lance Formation; Twr, White Eiver Formation; To, Arikaree Formation; To, Ogallala Formation; Qf, terrace deposits; Qfp, flood- plain deposits.

Use of water: D, domestic; I, irrigation; In, industrial; N", none; P, public; S, stock.

Depth to water: Measured depths to water level are given in feet and hundredths; reported depths are given in feet.

Eemarks: Oa, sample collected for chemical analysis; D, discharge in gallons per minute (M, measured; R, reported) ; DD, drawdown in feet while discharging at preceding rate (measured drawdowns are given in feet and tenths; reported and estimated drawdowns are given in feet); B3d, battery of three wells (or number given) ; T, temperature in degrees Fahrenheit; K, specific conductance (micromhos at 25°C).

Loc

atio

n

2bcb

--~

- ---

2d

bc_

_

lOab

aL--

-- -

22ab

b-_

12-6

3-5d

hc_ .

12-6

4-2a

dd-

2bcb.

4ct)c

lldaa

.-_ ..

.

12-6

8-lla

ab- ---

--1

2-6

9-7

bbb -

17bcd .

..

.

30bc

c

13-6

1-5

baa

.-

3lc

bb

~

~O

Qrt

rtrt

O

13-6

3-10

ccb --- -

O

CrtQ

Q

13

-64

-10

ica.

--

19ca

c

30da

a. _

----

--_

Ow

ner

or t

enan

t

Ted

Mea

d

- .d

o..

... ..

....

..

-- d

o

- ------

.... . d

o -

- - ------

d

o - -

---.d

o--- ..

.......d

o--

----

- .....

....

.do

- -

_

-do ....

Dol

an C

attl

e C

o. _

__

J. A

. W

ald

en

__

__-_

do

Wvo

. H

eref

ord

Ran

ch

Yea

r dr

iUed

1963

1 Q

4.C

1Q

«O

1950

1947

IQR

Q

1 Q

19

1945

1941

1945

1961

1962

1962

1909

1959

1958

1958

Dep

th

of w

ell

(fee

t)

102

104

104

105

105 85 125

220

185 74 70 197

265

208 85 80 100 85 100 93 80

>10

410

3 80 100

175

115

120

150

300

338

160

Dia

met

er

of w

ell

(inc

hes)

16 36 18 18 18 18 18 6 6 6 6 5 8 6 8 18 18 20 18 18 32 18 6 20 5 4 10 10 8

Geo

logi

c so

urce

Qt

...

Qt ..

..

Qt.-

...

Ot

Qt -

Ot

To(T

)_

To

...-

---

To____ _

_T

o_

--. _

_T

o. -_

-.-

-T

o..

. _

.-

To.. _

_

-

Qt.

._ -

Qt-

----

---

Qt.

-- -

To

. .-.

-_-_

To--

----

-

To

.--.

-

To(?). -

To(?

)

To

Use

of

wat

er

I I I I I I I I S S S S S S S S I I I I I I I N I D D,

SI S S S S D

, In

D,

InS

Alt

itud

e of

land

su

rfac

e ab

ove

mea

n se

a le

vel

(fee

t) 5,34

55,

358

5,34

35,

361

5,35

85,

335

5,34

05,

325

5,51

05,

640

5,61

85,

692

5,67

06,

179

6,25

06,

294

6,33

57,

259

5,12

5

5,13

55,

141

5,17

85,

186

5,26

05,

184

5,32

55,

347

5,43

55,

581

5,48

05,

478

5,74

05,

762

5,82

85,

672

5,69

65,

838

Dis

tanc

e to

wat

er

belo

w la

nd

surf

ace

(fee

t) 59 70.3

555

.44

70.3

572

.34

53.6

118 40

.07

56.1

811

4. 4

839

.41

33.2

715

0 57.7

220

8.31

188.

73

59.7

740 38

.41

29 32 35.9

219

.49

30 57.0

864 56 76

.99

58 87.6

210

5. 2

910

7. 9

470 98 146.

24

Alt

itud

e of

wat

er

leve

l ab

ove

mea

n se

a le

vel

(fee

t) 5,28

65,

288

5,28

85,

291

5,28

65,

281

5,32

25,

285

5,45

45,

526

5,57

95,

659

5,52

06,

121

6,04

26,

105

6,33

57,

199

5,08

5

5,09

75,

112

5,14

65,

150

5,24

05,

154

5,26

85,

283

5,37

95,

504

5,42

2

5,65

25,

657

5,72

05,

602

5,59

85,

692

Dat

e of

m

easu

re­

men

t

Jan

. 19

63M

ay

1964

__ d

o .....

Ap

r.

1964

Oct

. 19

64 -do

Aug.

1959

May

196

4D

ec.

1964

Ap

r.

1964

__ d

o .....

-do

-A

pr.

19

61A

pr.

19

64-_

dO

----

-__

--d

o-

S

ept.

196

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GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO. 69

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70 GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO.

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REFERENCES CITED 71

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