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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
, fr
om s
ands
tone
and
fra
ctur
ed s
hale
. T
he f
orm
atio
n is
no
t co
nsid
ered
to
be a
goo
d so
urce
of
wat
er.
Not
kno
wn
to y
ield
wat
er t
o w
ells
in
Lar
amie
Cou
nty.
M
ay y
ield
sm
all q
uant
itie
s fr
om fr
actu
res
near
the
out
cr
op,
but
the
form
atio
ns a
re n
ot c
onsi
dere
d to
be
a po
tent
ial
sour
ce o
f wat
er.
Not
kno
wn
to y
ield
wat
er t
o w
ells
in
Lar
amie
Cou
nty
but
wou
ld p
roba
bly
yiel
d sm
all
to m
oder
ate
supp
lies.
T
wo
sam
ples
of
wat
er f
rom
the
Hor
se C
reek
oil
fiel
d w
ere
of th
e so
dium
chl
orid
e ty
pe a
nd c
onta
ined
sli
ghtl
y m
ore
than
20,
000
part
s pe
r m
illio
n di
ssol
ved
solid
s.
The
wat
er i
s pr
obab
ly o
f be
tter
qua
lity
nea
rer
the
outc
rop.
Not
kno
wn
to y
ield
wat
er t
o w
ells
in
the
coun
ty,
nor
is
it c
onsi
dere
d to
be
a po
tent
ial
sour
ce o
f w
ater
.
Not
kno
wn
to y
ield
wat
er t
o w
ells
in
the
coun
ty b
ut
mig
ht y
ield
sm
all
to m
oder
ate
supp
lies.
A
sam
ple
of
wat
er f
rom
the
Hor
se C
reek
oil
fiel
d w
as o
f the
sod
ium
bi
carb
onat
e ty
pe a
nd c
onta
ined
1,2
90 p
pm d
isso
lved
so
lids.
CO
TA
BL
E 1
. Sum
mary
of
stra
tigr
aphi
c u
nit
s an
d th
eir
wat
er-b
eari
ng c
hara
cter
isti
cs C
onti
nued
Era o 1 <s> 3 ft-l i a M
,D
Syst
em
Jura
ssic
Tri
assi
c
Perm
ian
§
g
03 fe
0 ~
^
[
Penn
sylv
ania
n
Serie
s
Upp
erJu
rass
ic
Low
erT
rias
sic
Subd
ivis
ion
Mor
riso
nFo
rmat
ion
Sun d
ance
Form
atio
n
Chu
gwat
erFo
rmat
ion
Goo
se E
ggFo
rmat
ion
Cas
per
Form
atio
n
Thi
ckne
ss(f
eet)
200-
230
40-1
00
430-
500
200-
250
800-
900
(?)
Phy
sica
l cha
ract
eris
tics
Var
iega
ted
shal
e, t
hin
sand
ston
e, a
ndlim
esto
ne b
eds.
Pre
dom
inan
tly
ligh
t-ta
n sa
ndst
one
and
gree
nish
san
dy s
hale
.
Red
dish
-ora
nge
silts
tone
an
d ve
ryfi
ne g
rain
ed s
ands
tone
.
Red
dish
sil
tsto
ne a
nd s
ands
tone
inte
r-st
ratif
ied
with
lim
esto
ne,
dolo
mite
,an
d gy
psum
.
Upp
er 6
00-7
00 f
eet
cons
ists
of
lim
est
one
and
sand
ston
e; l
ower
par
t is
redd
ish
to re
ddis
h-ye
llow
san
dsto
ne,
quar
tzit
e, a
nd a
rkos
e.
Pre
dom
inan
tly
gran
ite,
gn
eiss
, an
dsc
hist
.
Wat
er s
uppl
y
Not
kno
wn
to y
ield
wat
er t
o w
ells
in
the
coun
ty.
It i
sno
t co
nsid
ered
to
be a
pot
enti
al s
ourc
e of
wat
er.
Not
kno
wn
to y
ield
wat
er t
o w
ells
in t
he c
ount
y.
Sand
st
one
clas
sed
as a
pot
enti
al a
quif
er i
n A
lban
y C
ount
y(L
ittle
ton,
19
50,
p.
14)
prob
ably
has
sim
ilar
wat
er
bear
ing
char
acte
rist
ics
in L
aram
ie C
ount
y.
No
wel
ls k
now
n to
pen
etra
te t
hese
for
mat
ions
in
the
coun
ty.
Not
con
side
red
to b
e a
pote
ntia
l so
urce
of
wat
er.
Yie
lds
larg
e qu
anti
ties
of
wat
er t
o sp
ring
13-
69-8
dbb.
Wou
ld y
ield
mod
erat
e to
larg
e su
pplie
s to
wel
ls.
Will
yie
ld s
mal
l qu
anti
ties
of
wat
er f
rom
fra
ctur
es o
r w
eath
ered
zon
es a
t fav
orab
le l
ocat
ions
.
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
.A-*
Ter
race
dep
osits
50
75
' -,
5050'-
5000'-
49
50
'-
4900
'
Flo
od-p
lain
dep
osits
Ter
race
Allu
vium
Whi
te R
iver
For
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ion
Flo
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ts
Ter
race
de
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race
F
lood
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in \D
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- 5200' -
5150'
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Flo
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tsF
lood
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in
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sits
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5100'
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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
Bas
e fr
om W
yom
ing
Sta
te
Hig
hway
Dep
artm
ent
4
MIL
ES
H
ydro
geol
ogy
com
pile
d by
Mar
lin
E. L
owry
I
and
Mar
vin
A.
Cris
t, 1965
G § I I S3
FIG
URE
12.
Con
figu
rati
on o
f to
p of
Whi
te R
iver
For
mat
ion
(sol
id c
onto
urs)
an
d sa
tura
ted
thic
knes
s of
ter
race
depo
sits
(da
shed
con
tour
s).
Dot
s ar
e co
ntro
l po
ints
.
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
1UO1
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FIGURE 13. Water-level fluctuations in well tapping the Arikaree Formation.Recorded automatically.
p l-js52
O M»IS* <T>
5
DEPTH TO WATER, IN FEET BELOW LAND SURFACE£> O
AUGUST
SEPTEMBER
OCTOBER
NOVEMBER
DECEMBER
JANUARY
FEBRUARY
30i
i i
i i
r
50 -
l»
Well
13-6
0-3
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ine B
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Co
mp
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FIG
URE
15.
Lon
g-te
rm t
rend
of
wat
er l
evel
s in
are
as o
f he
avy
pum
ping
.
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),
TA
BL
E 3
. C
hem
ical
ana
lyse
s of
grou
nd w
ater
in
Lar
amie
Cou
nty,
Wyo
.
[Res
ults
in p
arts
per
mill
ion
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pt a
s in
dica
ted.
A
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by U
.S.
Geo
l. Su
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]
to
Loc
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epth
(f
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Dat
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co
llec
tion
Temperature
(°F)
Silica
(SiOa)
Total
iron
(Fe)
Calcium
(Ca)
Magnesium
(Mg)
Sodium
(Na)
Potassium
(K)
Bicarbonate
(HCOs)
Carbonate
(CDs)
6 s -S
<2
"3 03
Chloride (Cl)
Fluoride
(F)
Nitrate
(N0»)
Boron
(B)
Dissolved
solids (resid
ue at
180°C)
Hardness as CaCOs
Noncarbonate
hard ness
as CaCOa
Specific
conductance (microm
hos at 25°C
)
W a
Sodium-adsorption- ratio
(SAR
)Residual-sodium
- carbonate (RSC)
[IIOHO 'iooioao ^
Lan
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1
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-70
4 71
35-
1-6
2 5-
1-6
252
58
13 120.
10
.11
3.2
3.2
1.0 .5
270
247
592
560
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2732 28
31 6.9
2.8
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688
625
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100 0
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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
3-_
.do
Ju
ne
1945
Oct
. 19
64O
ct.
1957
July
19
61A
pr.
19
64Ja
n.
1965
Mar
. 19
62O
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1964
May
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1964
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d
1963
1955
1948
1940
1961
1964
1936
1935
1964
1964
1964
1964
1935
1964
1964
1964
1954
1952
1952
1939
1962
(?)
1956
Dep
th
of w
ell
(fee
t) 75 220 90 150
222
185
155 85 300+
/IOQ
300
170
485
170 26 168
185
182
172
300
171
185
190
190
175
205
158
500 91 187
Dia
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of w
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(inc
hes) 5 8 6 5 6 5 8 5 10 5 6 6 8 10 10 8 8 8 8 8 8 8 12 3 5 5 3 8 5 10 10 9 3 10
Geo
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S S S S S S S In S p S S N D,I
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Alt
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land
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mea
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a le
vel
(fee
t) 5,92
55,
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5,87
05,
850
5,92
05
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96,
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350
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553
Dis
tanc
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wat
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belo
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nd
surf
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(fee
t)
41.2
01
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Alt
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wat
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leve
l ab
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mea
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a le
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(fee
t) 5,88
45
794
5,79
65,
735
5,72
85,
803
5,77
75,
985
5,87
55,
920
5,99
96,
026
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5
6,33
2
6,18
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250
6,25
36,
247
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5
6,25
5
6,26
56,
272
6,38
96,
274
6,22
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305
6,22
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Dat
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m
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re
men
t
Apr
. 19
64 d
o _
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d
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-
d
o
Mar
. 19
63A
pr.
1964
Mar
. 19
57A
pr.
1964
June
196
1
July
19
64
Apr
. 19
64
Dec
19
64
d
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d
o ...
d
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May
196
4D
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1964
d
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Sept
. 19
64A
pr.
1964
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1963
d
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Sept
. 19
63A
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1964
Rem
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rrM
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1944
1944
1947
1920
1932
1959
1959
1959
1950
1953
1900
1962
~~~I
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1961
1962
1934
1962
1960
1917
1955
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1959
1938
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1910
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1945
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1938
(?)
1912
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1900
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202
255
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June
196
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1963
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19
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May
196
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May
196
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1961
Ju
ly
1962
Apr
. 19
64
Oct
. 19
64
Mar
. 19
60
Jan.
19
65
Nov
. 19
48
Feb.
19
64
1959
A
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1964
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1963
July
196
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d
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(7)
1960
1964
1916
(?)
1945
1956
1960
1917
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1945
1960
1962
1900
1930
(7)
1955
1963
1933
IQK
d.
1956
1956
1955
1955
1955
1934
1955
1955
1956
Dep
th
of w
ell
(fee
t)
122
IRd.
240
125
131
122
152
139
170
170
194
240
580
320
296 74 400
250
275
115 99 98 180(
7)
311(
7)31
0(7)
225
229
274 12 341
332
175
212
266
Dia
met
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of w
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(inc
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Alt
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land
su
rfac
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ove
mea
n se
a le
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(fee
t) 6,72
05,
680
5,78
05,
780
5,84
05,
860
5,88
95,
930
5,92
55,
962
6,01
05,
950
5,97
06,
098
6,02
56,
062
6,19
26,
210
6,21
56,
130
6,01
06,
146
6,01
76,
385
6,43
86,
328
6,33
36,
270
6,24
96,
302
6,16
8
6,31
56,
315
6,44
06,
274
6.33
0
Dis
tanc
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belo
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surf
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t)
103.
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110
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Alt
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e of
wat
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leve
l ab
ove
mea
n se
a le
vel
(fee
t) 5,61
65,
591
5,67
05,
670
5,70
95,
728
5,75
65,
787
5,81
35,
805
5.87
25
7Q4.
5,75
85,
767
5,80
65,
801
5,96
86,
023
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9
5,93
06,
071
5,87
56,
264
6,30
56,
274
6,27
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6,26
4
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6,30
26,
312
6,27
06.
273
Dat
e Of
m
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men
t
Aug
. 19
63...d
o.
A n
r 1
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.
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196
3A
ug
. 19
63Ju
ly 1
963
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o
Nov
. 19
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ly
1963
Aug
. 19
63_
__
do
---.
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n.
1964
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19
63
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. 19
63A
pr.
1955
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r IQ
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Mar
. 19
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Feb
. 19
64A
pr.
1964
Mar
. 19
64..
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Rem
arks
T71,
K37
5
D15
0R,
Ca
D60
0RT
50,
K37
5T
55,
K40
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65,
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52.5
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360
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375
T55
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365
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d.
TT
°.Q
^
T69
, K
390
T57
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360
T58
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335
T60
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378
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5M
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to
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d.--
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d..
14
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24
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McD
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l.
Har
old
Me W
illia
ms.
.. -
-do . ..
. .d
o .. ..
1955
1955
1955
1955
1940
1955
1934
1940
1940
1956
1945
1940
1943
1945
1941
1963
1917
1963
1960
1946
1954
1959
1959
1961
1960
1913
(?)
1900
(?)
1900
1912
(?)
1910
(?)
1962
196
1
1955
1941
1941
1941
190
151
163
208
250
ocn
286
334
368
215
220
250
110
307
235
190
230
235
230
184
152
194 10 16 10 156 12 125 95 315
318
240
175
137 57 75 145
113
115
109 98 160
270 48 65 10'J
12 12 12 12 10 12 10 10 12 1 <;
10 10 6 10 10 10 10 10 10 10 12 12 12 80 24(?
)
30 16 36 7 7 16 4 5 6 4 4 4 6 14 18 5 5 5
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P N P P P P P P P P P P N S P P P P P N P P P S S S S D,S
S I S D,I
nD
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I I N S S N S D,S
D,S
D,S
I I I S S D,
S
6,25
86,
277
6,31
66,
344
6,39
36,
328
6,31
86,
375
6,38
36,
398
6,44
56,
483
6,54
56,
490
6,63
46,
469
6,52
46,
550
6,51
76,
512
6,40
96,
365
6,42
86,
600
6,58
06,
538
6,49
06,
529
6,73
05,
155
5,11
25,
096
5,08
25,
285
5,30
85,
603
5,47
05,
382
5,43
05,
512
5,58
55,
623
5,55
05,
480
5,68
0
5,79
55,
710
5,67
95,
655
9.82
39.3
869
.09
79.1
759
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33.7
8
52.0
0 24
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57.5
281
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124.
9191
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178.
31
68.7
6 10
6.81
12
2. 2
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8.81
50.0
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46.6
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1.78
6 30
7.65
55
74
58
47
73
90
12
8. 4
0 49
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50.0
4 12
3. 8
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100
100 86 25
.56
96.3
2
173.
51
28
45 14
6,26
76,
277
6,27
5 6,
314
6,26
8 6,
284
6,33
1 6,
374
6,38
76,
401
6,42
06,
399
6,45
6 6,
400
6,41
7 6,
428
6,40
8
6,35
9 6,
328
6,38
16,
597
6,55
4 6,
536
6,48
4 6,
499
6,72
2 5,
100
5,03
8 5,
038
5,03
5 5,
212
5,21
8 5,
475
5,42
0 5,
332
5,30
6 5,
413
5,48
5 5,
523
5,46
45.
454
5, 5
84
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21
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034
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41
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64
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. 19
64
Mar
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64
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o .
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o .
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o .
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pr.
1964
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Mar
. 19
64
Dec
. 19
64
Apr
. 19
64
Apr
. 19
64
d
o .
.
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o _
Nov
. 19
63
Aug
. 19
63
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o.
Ja
n.
1960
S
ept.
1946
S
ept.
1963
N
ov.
1954
N
ov.
1947
A
pr.
1960
A
ug.
1959
M
ay 1
961
May
196
0 D
ec.
1963
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ay 1
964
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d
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Dec
. 19
63
d
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May
196
2 N
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1964
Oct
. 19
64
Aug.
1963
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o......
.
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Ca
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Cur
tis
Mil
ler
------
Yea
r dr
iUed
1930
(?)
1955
1958
1963
1910
(7)
1910
1953
1910
(7)
1910
(7)
1956
1961
1960
1942
1954
1954
1954
1954
1954
1954
1911
1912
(7)
1911
(7)
1960
1910
(7)
1890
1962
1911
(7)
Dep
th
of w
ell
(fee
t) 28 42 135
110
100 81 139
260
216
114
117
189
203
182
181
191
190
300
260
430 90 182
351
223
236
294
130
238
312
180
206
220
160
169
235
245
235(
7)
Dia
met
er
of w
ell
(inc
hes)
16 4 3 5 5 6 5 6 6 5 6 16 6 6 6 6 10 12 12 24 12 6 12 12 5 4 5 5 6 6 5
Geo
logi
c so
urce
Qfp
----
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____
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----
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o___
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r_.
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Use
of
wat
er
S s S s s s s s s s D,
SD
, S
S s s s s I s s D S s s p p p p p s p p s N N S N S S S
Alt
itud
e of
land
su
rfac
e ab
ove
mea
n se
a le
vel
(fee
t) 5, 67
9
5,77
55,
705
5,85
85,
820
5,96
26,
032
5,98
35,
848
6,12
56,
151
6,06
5
6,41
06,
480
6,76
66,
612
6,74
56,
841
6,78
56,
668
6,61
66,
642
6,79
46,
680
6,59
55,
350
5,45
25,
410
5,40
55,
450
5,50
05,
600
5.51
2
Dis
tance
to
wat
er
bel
ow
lan
d
surf
ace
(fee
t) 16.7
022
.28
112.
07
70.5
985 43
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87.6
182 19
9. 0
317
6 74.1
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166.
05
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86
161.
9972
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87
169.
33
93.2
022
0.00
160 33
.82
56.4
5
33.9
613
.83
36.6
742
.22
65.9
618
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165.
9120
0.00
194.
87
125
154.
54
166.
17
200
222.
24
Alt
itud
e of
wat
er
leve
l ab
ove
mea
n se
a le
vel
(fee
t) 5, 66
25,
688
5,72
35,
704
5,62
0
5,77
05,
738
5.83
75,
826
5,83
35,
807
5,77
4
5,95
96,
018
5,90
36,
168
6,27
06,
311
6,54
66,
452
6,71
16,
785
6,72
96,
634
6,60
26,
605
6,75
26,
614
6,57
65,
184
5,25
2
5,28
05,
295
5,33
45,
400
5.29
0
Dat
e of
m
easu
re
men
t
Aug
. 19
63
July
196
3A
ug.
1963
...d
o
Aug
. 19
64 d
o
Ju
ly 1
963
d
o
...d
o .
d
o
__. d
o
___do
do .
Jan.
196
5Ju
ly 1
963
Apr
. 19
64
Aug
. 19
63
Aug
. 19
63O
ct.
1960
Aug
. 19
63M
ar.
1964
d
o
... d
o ....
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o.......
...d
o .
Dec
. 19
63M
ar.
1964
... d
o..
....
_Se
pt.
1964
... d
o..
....
_ d
o
._
Mar
. 19
64S
ept.
1964
Sent
. 19
64
Rem
arks
T66,
K40
5T
57.5
, K
420
T54
, K
410
T54
, K
355
T56
, K
395
T57
, K
360
T55
, K
380
T57
, K
345
T63
, K
320
T69
, K
345
T56
.5,
K26
5D
15R
, D
D15
T54
, K
340
DIO
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Ca
D45
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123
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b. ---
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C.
Dav
is -
_-_
1912
(?)
1914
(?)
1962
1910
(?)
1913
(?)
1913
(?)
1912
1912
(?)
1915
(?)
1960
1910
1940
1948
1958
1958
1959
1947
1911
(7)
1961
1950
1911
1958
1958
238
192
..99 245 86 113
165
220
135
(?)
185
175
120 90 235
210
206
200
513
638
198
215
165
202
162
265
240
192
230
219
229
197
210
220
242
233
217
156
459
473
270
260
320
6(?)
16 6 4 6 4 6 3 4 4 4 6 3 4 3 10 10 5 6 6 5 4 4 5 5 4 4 5 4 3 6 5 3 5 6 5 10 10 6 3 5 4 6
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N S S I S N
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5,53
05,
574
5,45
0 5,
482
5,51
8 5,
495
5,43
35,
675
5,55
5 5,
660
5,70
5 5,
628
5,56
0 5,
768
5,81
8 5,
872
5,83
0 5,
800
5,80
0 5,
840
5,88
7 5,
895
6,00
3 5,
940
6,03
3 5,
931
6,21
2 6,
092
6,14
2 6,
138
6,13
8 6,
263
6,15
36,
138
6,10
96,
128
6,12
06,
393
6,35
3 6,
493
6,41
06,
274
6,43
1 6,
547
6,53
86,
520
6,53
56,
691
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37,
049
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22
81.5
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200
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11
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5,30
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414
5,36
8 5,
317
5,44
3 5,
398
5,33
15,
475
5,43
5 5,
496
5,55
5 5,
536
5,49
2 5,
559
5,57
7 5,
697
5,65
0 5,
615
5,63
2 5,
655
5,73
4 5,
733
5,82
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782
5,88
8 5,
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6,08
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5,95
2 5,
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5,95
8 6,
117
5,94
85,
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5,90
95,
953
5,94
06,
237
6,21
3 6,
281
6,23
26,
152
6,29
5 6,
410
6,41
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313
6,43
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1937
1922
1911
1911
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1931
1912
1912
(?)
1910
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1963
1913
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1900
1910
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1951
1962
1912
(?)
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Dep
th
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(fee
t) 28 263 85 100
285(
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020
019
226
028
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025
521
328
020
027
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Alt
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(fee
t) 6,55
2
6,87
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681
6,71
55,
362
5,39
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355
5,31
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285
5.29
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55,
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496
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55,
550
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183.
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4828
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Alt
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wat
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leve
l ab
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mea
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(fee
t) 6,54
5
6,69
16,
657
6,69
35.
080
5,10
55,
115
51
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5,10
35,
102
5,15
35,
169
5,23
95,
264
5,17
05,
248
5,24
85,
299
5,32
75,
320
5,30
25,
320
5,35
5
5.30
05,
389
5,35
45,
421
5,38
35,
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5,42
65,
539
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1914
1959
1945
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1942
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1930
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1954
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1961
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6,50
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1958
1946
1940
1938
1960
1960
1963
1939
1959
1950
1920
(7)
1915
1915
(?)
1949
1949
1939
1939
Dep
th
of w
ell
(fee
t)
100
200
160
100
165
KC
116 84 219
14<;
153
130
one 60 115 81 132
137 48 145
1 A
K
175 26 22 190 72 22
Dia
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Alt
itu
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abov
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55,
320
5,03
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5,30
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5,64
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05,
930
5,92
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6,06
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125
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5,97
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Dis
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wat
er
belo
w l
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surf
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(fee
t) 67.7
276
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10
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44.9
8
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Alt
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l ab
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mea
n se
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(fee
t) 5,12
2A
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5,18
1
4,99
2
5,19
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GEOLOGY, GROUND WATER, LARAMIE COUNTY, WYO. 69
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o