Volume VII-A
OCCURRENCE AND CHARACTERISTICS OF
GROUND WATER IN THE DENVER-JULESBURG BASIN
WYOMING
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Volume VII-A
OCCURRENCE AND CHARACTERISTICS OF
GROUND WATER IN THE DENVER-JULESBURG BASIN,
WYOMING
by
Robert D. Libra, Michael Collentine, and Kenneth R. Feathers
Project Manager
Craig Eisen
Water Resources Research Institute
University of Wyoming
Report to
U.S. Environmental Protection Agency
Contract Number G-008269-79
Project Officer
Paul Osborne
August 1981
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Introduction
This report presents the findings of a ground-water study of the
Denver-Julesburg basin in southeastern Wyoming. The study was funded by
the U.S. Environmental Protection Agency (EPA) for the Underground
Injection Control (UIC) program. The UIC is designed to protect sources
of usable ground water from possible contamination caused by underground
injection of liquid wastes and other fluids. This ground-water report
is one of seven prepared by the Wyoming Water Resources Research Insti-
tute for the EPA. These reports cover all of the state of Wyoming with
the exception of the Yellowstone National Park area in the northwestern
part of the state. The results of the study are primarily intended for
use by the EPA and Wyoming state agencies concerned with development and
preservation of the ground-water resources of the area.
The purpose of this report is to delineate, characterize, and
document ground-water occurrence, flow, quality, and use in the Denver-
Julesburg basin. The findings are based on available information; no
site-specific ground-water investigations were conducted during the
course of this study by the Wyoming Water Resources Research Institute
(WRRI). Specific work activities conducted by WRRI included (1) field
geologic reconnaissance of some parts of the study area and adjacent
areas; (2) collection, screening, and analyses of existing spring, water
well, and oil test well data; and (3) review of previous reports.
Water well, spring, and oil test well data were obtained from
records at the Wyoming State Engineer's Office, Wyoming Geological
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Survey, Wyoming Oil and Gas Conservation Commission, and from tabulated
data in previous reports.
iii
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TABLE OF CONTENTS
CHAPTER Page
I. SUMMARY OF FINDINGS 1
II. GEOGRAPHIC AND GEOLOGIC SETTING 7
PHYSIOGRAPHY 8
Topography 8
Surface Drainage 10
Climate 12
HUMAN GEOGRAPHY 12
Population Distribution 12
Land Use and Ownership 14
GEOLOGY 14
Stratigraphy 14
Structural Geology. ..." 18
Hydrostratigraphy 21
III. WATER USE 25
AGRICULTURAL WATER USE 29
Irrigation 29
Livestock 32
PUBLIC AND DOMESTIC WATER USE 32
Public Water Use 32
Domestic Water Use 33
INDUSTRIAL WATER USE 34
IV. AQUIFER PROPERTIES AND GROUND-WATER CIRCULATION .... 37
PALEOZOIC AQUIFER SYSTEM 38
Hydrologic Properties 45
Ground-Water Circulation 46
MES0Z0IC AQUIFERS 48
Hydrologic Properties 48
Ground-Water Circulation 50
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CHAPTER Page
LANCE/FOX HILLS AQUIFER 50
Hydrologic Properties 52
Ground-Water Circulation 54
TERTIARY AQUIFER SYSTEM 54
Hydrologic Properties 56
Permeability 56
Transmissivity 59
Specific Capacity and Well Yields 62
Ground-Water Circulation 65
Recharge 67
Discharge 67
QUATERNARY AQUIFERS 68
Hydrologic Properties 69
Permeability 69
Transmissivity 69
Specific Capacities and Well Yields 73
Ground-Water Circulation 73
V. WATER QUALITY 75
GENERAL WATER QUALITY 76
Paleozoic Aquifer System 76
Mesozoic Aquifers 77
Lance/Fox Hills Aquifer 79
Tertiary Aquifer System 81
Quaternary Aquifers 83
White River Aquifer 87
Arikaree and Ogallala Aquifers 87
DRINKING WATER STANDARDS 88
Primary Standards 88
Fluoride 88
Nitrate 90
Secondary Standards 90
Radionuclear Species 91
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CHAPTER Page
VI. REFERENCES 97
APPENDIX A: GROUND-WATER USE BY MUNICIPAL AND
NON-MUNICIPAL SYSTEMS AND BY INDUSTRY
IN THE DENVER-JULESBURG BASIN,
WYOMING A-l
APPENDIX B: LOCATION AND NUMBERING SYSTEM B-l
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LIST OF FIGURES
Figure Page
II-l Location map of the Denver-Julesburg basin 9
II-2 General geologic column, Denver-Julesburg basin,
Wyoming 16
II-3 Major structural features of the Denver-Julesburg
basin, Wyoming 17
II-4 Structural cross-sections, Denver-Julesburg
basin, Wyoming 19
II-5 Hydrostrigraphy of the Denver-Julesburg basin,
Wyoming 23
III-l Estimated water use in the Denver-Julesburg
basin, Wyoming 28
IV-1 Potentiometric map of the Paleozoic aquifer
system, Denver-Julesburg basin, Wyoming 44
IV-2 Water table map of the Tertiary aquifer system,
Denver-Julesburg basin, Wyoming 66
V-l Major ion compositions of representative waters
of the Paleozoic aquifer system, Denver-Julesburg
basin, Wyoming 78
V-2 Major ion composition of representative waters from
Mesozoic aquifers, Denver-Julesburg basin,
Wyoming 80
V-3 Major ion composition of representative waters from
the Lance/Fox Hills aquifer, Denver-Julesburg
basin, Wyoming 82
V-4 Major ion composition of representative waters of
the White River aquifer, Tertiary aquifer system,
Denver-Julesburg basin, Wyoming 84
V-5 Major ion composition of representative waters of
the Arikaree and Ogallala aquifers, Tertiary
aquifer system, Denver-Julesburg basin, Wyoming ... 85
V-6 Major ion composition of representative waters of
the Quaternary aquifers, Denver-Julesburg basin,
Wyoming 86
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Figure Page
V-7 Locations of high fluoride and nitrate levels in
ground water, Denver-Julesburg basin, Wyoming .... 89
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LIST OF TABLES
Table Page
II-l Surface drainage systems in the Denver-Julesburg
basin, Wyoming 11
II-2 Population figures for counties and incorporated
areas, Denver-Julesburg basin, Wyoming 13
III-l Water use in the Denver-Julesburg basin, Wyoming. . . 27
III-2 Irrigation water use, Denver-Julesburg basin,
Wyoming 30
IV-1 Lithologic and hydrologic characteristics of
rock units in the Denver-Julesburg basin, Wyoming . . 39
IV-2 Hydrologic properties of the Paleozoic aquifer
system, Denver-Julesburg basin, Wyoming 47
IV-3 Hydrologic properties of Mesozoic aquifers,
Denver-Julesburg basin, Wyoming 49
IV-4 Yields of Mesozoic aquifers, Denver-Julesburg
basin, Wyoming 51
IV-5 Hydrologic properties of the Lance aquifer,
Denver-Julesburg basin, Wyoming 53
IV-6 Hydrologic properties of the White River aquifer,
Tertiary aquifer system, Denver-Julesburg basin,
Wyoming 57
IV-7 Hydrologic properties of the Ogallala aquifer,
Tertiary aquifer system, Denver-Julesburg basin,
Wyoming 60
IV-8 Hydrologic properties of the Arikaree aquifer,
Tertiary aquifer system, Denver-Julesburg basin,
Wyoming 63
IV-9 Hydrologic properties of Quaternary aquifers,
Denver-Julesburg basin, Wyoming 70
IV-10 Data sources for hydrologic properties 72
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Range of reported concentrations (mg/1) of chloride,
sulfate, and iron, by aquifer and county, Denver-
Julesburg basin, Wyoming
Reported analytical data for radiometric species
in ground water, Denver-Julesburg basin, Wyoming. . .
ix
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LIST OF PLATES*
Plate
1 Structure contour map on top of the Cloverly Formation, Denver-
Julesburg basin, Wyoming.
2 Permitted domestic wells in the Denver-Julesburg basin, Wyoming.
3 Total dissolved solids map of the Paleozoic aquifer system and
Precambrian rocks, Denver-Julesburg basin, Wyoming.
4 Total dissolved solids map of Mesozoic aquifers, Denver-Julesburg
basin, Wyoming.
5 Total dissolved solids map of the Lance/Fox Hills aquifer, Denver-
Julesburg basin, Wyoming.
6 Total dissolved solids map of the White River aquifer, Tertiary
aquifer system, Denver-Julesburg basin, Wyoming.
7 Total dissolved solids map of the Arikaree and Ogallala aquifers,
Tertiary aquifer System, Denver-Julesburg basin, Wyoming.
8 Total dissolved solids map of Quaternary aquifers, Denver-
Julesburg basin, Wyoming.
*Plates contained in Volume VII-B.
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I. SUMMARY OF FINDINGS
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I. SUMMARY OF FINDINGS
1. Identified as water-bearing zones within the Denver-Julesburg
basin are, in ascending stratigraphic order: (1) weathered surficial
zones in Precambrian rocks; (2) the Paleozoic aquifer system; (3)
several dispersed, permeable sandstone horizons within the predominantly
shale and siltstone Mesozoic sequence; (4) the Lance/Fox Hills aquifer;
(5) the Tertiary aquifer system; and (6) Quaternary alluvial aquifers.
The most productive units are members of the Paleozoic and Tertiary
aquifer systems, and Quaternary alluvial aquifers. These aquifers are
dependable sources for stock and domestic needs throughout the basin and
commonly yield sufficient quantities of water for irrigation, municipal,
and industrial use.
2. Ground-water movement within the Paleozoic aquifer system is
away from outcrop recharge areas located along uplifted basin margins.
Ground-water circulation within other pre-Tertiary aquifers is unknown,
but is considered similar to flow within the Paleozoic aquifer system
due to similarities in geographic extent and structural setting.
Ground-water movement within the Tertiary aquifer system is
topographically controlled, from elevated areas along the western and
northern basin margins towards lowlands to the east.
3. Available data indicate that the Tertiary aquifer system,
consisting of the White River Group, Arikaree, and Ogallala formations,
regionally produces the largest quantities of good quality water within
the basin. This system is extensively developed for irrigation use,
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with lesser withdrawals for municipal, industrial, domestic, and stock
water supplies.
Coarse-grained lenses and channel deposits within the Ogallala
Formation and zones of secondary permeability within the White River
Group have the greatest water-producing capabilities within the Tertiary
aquifer system. Yields over 1,000 gpm are common and transmissivities
in excess of 500,000 gpd/ft are reported. The Arikaree Formation is the
thickest unit within this system, has generally low permeabilities but
large saturated thicknesses. Commonly, yields and transmissivities from
this areally extensive unit are several hundred gpm and 10,000-30,000
gpd/ft, respectively.
Water from the Tertiary aquifer system generally contains less than
500 mg/1 TDS. Calcium and bicarbonate are the dominant ions in
solution. Some White River aquifer waters contain over 500 mg/1 TDS,
and are sodium enriched. High nitrate and uranium concentrations exist
locally.
4. Where present, Quaternary flood plain and terrace aquifers,
composed primarily of coarse sand and gravel deposits, are dependable
large-scale ground-water sources within the basin. These aquifers
supply large amounts of generally good quality water for irrigation,
with lesser withdrawals for municipal, domestic, and stock water
supplies. Well yields are commonly 500 to 1,000 gpm, and transmissivity
estimates often exceed 100,000 gpd/ft. Where thick saturated deposits
of coarse materials are present, yields and transmissivities in excess
of 3,000 gpm and 1,500,000 gpd/ft, respectively, are reported.
Quaternary aquifer waters generally contain less than 500 mg/1 TDS.
Calcium and bicarbonate are the primary constituents of waters
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containing less than 500 mg/1 TDS, with higher TDS concentrations
related to sodium and sulfate enrichment. Objectionable levels of
nitrate are present locally.
5. The Paleozoic aquifer system, consisting of the Flathead
Sandstone, Guernsey, Casper, and Hartville formations, represents a
potentially important, though largely undeveloped, source of good quality
ground water. Current withdrawals are mainly for stock and domestic
supplies from relatively few wells.
Permeable sandstones and fractured carbonate rocks within the
Casper and equivalent Hartville formations represent the major
water-producing zones of the Paleozoic aquifer system. Undeformed
sandstones have yields and transmissivities to 80 gpm and 10,000 gpd/ft,
respectively. Sparse data from fractured carbonates indicate yields in
excess of 750 gpm.
Near outcrop, Paleozoic waters contain TDS concentrations of less
than 500 mg/1, with calcium and bicarbonate the dominant ions in
solution. Deep basin chemical data are lacking. High fluoride
concentrations are present in the far northeastern part of the basin.
6. Sandstones within the Upper Cretaceous Lance/Fox Hills aquifer
are mainly developed for domestic and stock water supplies where they
crop out in the east-central part of the basin. Sandstones within this
unit are fine-grained, and generally of low permeability. Most reported
yields are less than 25 gpm, but locally reach 100 gpm. Transmissivity
estimates vary from 400 to 5,000 gpd/ft. Higher yields may be possible
from wells penetrating large thicknesses of the aquifer.
TDS concentrations in Lance/Fox Hills aquifer waters vary from less
than 250 to over 4,000 mg/1, with TDS levels greater than 1,000 mg/1
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limited to outcrop areas. Sodium and bicarbonate are the dominant ions
in solution. High fluoride concentrations are present locally.
Where exposed or near the surface, dispersed Mesozoic sandstones
provide adequate yields for stock and domestic use. Yields rarely
exceed 25 gpm. Sparse hydrologic data indicate generally low
transmissivities.
Sparse chemical data indicate generally poor water quality for
these units. Total dissolved solids levels below 1,000 mg/1 are limited
to near-outcrop waters, with deep basin waters containing over 15,000
mg/1 TDS. Major ion composition varies from sodium-bicarbonate sulfate
to sodium-chloride with increasing salinity.
Weathered zones in Precambrian granites are developed for domestic
and stock use along the western basin boundary. Yields are generally
less than 25 gpm. Dissolved solids concentrations are less than 500
mg/1. Major ion compositions are not reported.
7. Species which exceed U.S. Environmental Protection Agency
primary drinking water standards include fluoride in Lance/Fox Hills
aquifer waters and nitrite in waters from Quaternary aquifers and the
Tertiary aquifer system. High nitrates are related to areas of human
habitation and agricultural activities.
In general, secondary drinking water standards are not exceeded in
waters from the Tertiary aquifer system or Quaternary aquifers.
Existing data indicate sulfate and chloride standards are exceeded
locally in deeper aquifers.
8. Water use within the basin is estimated to be about 411,000
acre-feet/year. Water for irrigation and other agricultural needs
constitute about 85 percent of this total, with public and domestic
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water supplies and industrial water needs comprising roughly equal parts
of the remainder. Ground-water sources, mainly the Tertiary aquifer
system and Quaternary aquifers, supply about 192,000 acre-feet of water
per year, 47 percent of the basin's total water demand.
9. Agricultural ground-water use for irrigation is estimated at
164,500 acre-feet/year. Major sources of irrigation ground water are
the Tertiary aquifer system and Quaternary aquifers. Stock water use is
about 3,760 acre-feet/year. Virtually all water-bearing units within
the basin provide stock water.
10. Ground-water withdrawals for public and domestic drinking
water supplies total about 18,000 acre-feet/year. The Tertiary aquifer
system and Quaternary aquifers supply most of this water. The Lance/Fox
Hills aquifer, the Precambrian aquifer, and to a lesser extent Mesozoic
sandstone aquifers supply water to domestic wells locally.
11. Industrial water use within the basin is roughly 5,000
acre-feet/year. Major industrial uses of ground water are for power
generation, chemical processing, and oil production and refining. The
Tertiary aquifer system supplies virtually all industrial ground water
used within the basin.
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II. GEOGRAPHIC AND GEOLOGIC
SETTING
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II. GEOGRAPHIC AND GEOLOGIC
SETTING
PHYSIOGRAPHY
The Wyoming part of the Denver-Julesburg basin covers an area of
about 8,000 square miles in the southeast corner of the state (Figure
II-l). The basin is bounded on the west by the Laramie Mountains, on
the north and northwest by the Hartville Hills and associated uplifts,
and on the south and east by the Wyoming-Colorado and Wyoming-Nebraska
state lines, respectively. As defined, the basin includes all of
Laramie and Goshen, the majority of Platte, and parts of Niobrara and
Albany counties.
Topography
Much of the Denver-Julesburg basin is occupied by the High Plains
surface (Figure II-l), a gently rolling tableland sloping eastward at 20
to 100 feet per mile. Elevation of the surface varies from over 7,000
feet in the west to about 5,000 feet at the Wyoming-Nebraska state line.
In the east-central part of the basin this surface has been breached by
the North Platte River and its tributaries, forming the Goshen Hole
Lowland, a gently rolling plain (Figure II-l). The lowland is comprised
of two subareas, Goshen Hole proper to the south, and the North Platte
River Valley to the north. The area is surrounded by discontinuous
escarpments rising several hundred feet that mark the edge of the High
Plains surface. Elevations within the lowland vary between 4,000 and
5,000 feet.
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Figure II-l. Location map of the Denver-Julesburg basin.
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Two terraced, alluviated lowland areas, Wheatland Flats and the
Pine Bluffs Lowland, identify depressions in the High Plains surface in
central Platte and southeast Laramie counties, respectively (Figure
II-l).
The Laramie Mountains, a high eastward-sloping plateau broken
locally by steep-sided valleys and rugged peaks, form the west border of
the basin (Figure II-l). The mountains rise moderately above the High
Plains surface along most of the western basin, reaching elevations of
8,000 to 8,500 feet.
Near the north-central basin boundary the High Plains surface is
disrupted by the Hartville Hills (Figure II-l), a broad uplifted area
which rises to elevations over 6,000 feet. The North Platte River
dissects the southern end of the hills, resulting in rugged topography
and relief in excess of 1,500 feet locally.
The highest elevation in the basin, about 8,500 feet, is along the
west basin boundary in the Laramie Mountains. The lowest elevation,
about 4,000 feet, occurs where the North Platte River crosses the
Wyoming-Nebraska state line. Total basin relief, therefore, is about
4,500 feet.
Surface Drainage
The Denver-Julesburg basin lies within the Missouri River drainage
(Table II-l). Most of the basin is drained by the North Platte River and
its tributaries (Figure II-l). The majority of these tributaries head in
the Laramie Mountains west of the basin, with the exceptions of Rawhide
Creek, which originates within the basin, and the Laramie River, which
heads in Colorado and crosses the Laramie Mountains. Several streams
originating along the southern end of the Laramie Mountains (FigureII-l)
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Table II-l. Surface drainage systems in the Denver-Julesburg basin,
Wyoming.
a
Missouri River
Platte River3
North Platte River
Laramie River
North Fork Laramie River
Chugwater Creek
Sybille Creek
Horse Creek
Bear Creek
South Platte Rivera
Lodgepole Creek
Crow Creek
Lone Tree Creek
Niobrara River
Cheyenne River3
£
Lance Creek
Old Woman Creek
Spring Creek
£
Stream lies outside of Denver-Julesburg hasin.
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flow into the South Platte River, with the divide between the North
Platte and South Platte drainages in northern Laramie County. The far
northeastern part of the basin is drained by the Niobrara River, a
tributary of the Missouri River, or by Spring Creek, part of the
Cheyenne River system.
Climate
The climate of the Denver-Julesburg basin is typified by low
precipitation, a high rate of evaporation, and widely variable
temperatures. Precipitation over most of the basin varies between 12
and 16 inches per year, with the higher elevations in the Laramie
Mountains receiving over 20 inches annually. About half of the annual
precipitation falls during April, May, and June, mainly through sporadic
and unevenly distributed thunderstorms. Average maximum and minimum
temperatures in the warmest month of the year, July, are about 88°F and
55°F, respectively, for most of the area. Average maximum and minimum
temperatures for January, the coldest month, are about 40°F and 10°F,
respectively. The growing season averages 140 to 150 days for most
parts of the basin.
HUMAN GEOGRAPHY
Population Distribution
Preliminary 1980 Census figures (Table II-2) indicate that about
95,000 persons reside in the Denver-Julesburg basin. Almost one-half of
the total basin population lives in the City of Cheyenne (Figure II-l)
and more than two-thirds reside in Laramie County, mainly in the
Cheyenne vicinity. No municipality in the basin, with the exception of
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Table II-2. Population figures for counties and incorporated areas,
Denver-Julesburg basin, Wyoming.
County/Incorporated Place
1980a
1970b
Laramie
68,022
56,360
PlatteC
12,022
5,989
Goshen
11,199
10,885
Niobrara0
1,995
2,154
Total
94,979
75,229
Albin
128
118
Burns
267
185
Cheyenne
47,207
41,254
Chugwater
285
187
Ft. Laramie
356
197
Guernsey
1,503
793
Hartville
148
246
LaGrange
232
189
Lingle
474
446
Lusk
1,654
1,495
Pine Bluffs
1,082
937
Torrington
5,431
4,237
Van Tassel
10
21
Wheatland
5,655
2,498
Yoder
110
101
Total
64,542
52,904
1980 Census of Population and Housing Preliminary Report, U.S.
Department of Commerce, Bureau of the Census, 1980.
^U.S. Department of the Interior, 1974.
c
Estimated population of county area within the basin.
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Cheyenne, has a population in excess of 10,000; only six incorporated
towns have more than 1,000 residents (Table II-2).
A comparison of 1970 and preliminary 1980 Census figures (Table
II-2) indicates a 26 percent population increase over the past decade.
This increase is lower than the 41 percent increase for all of Wyoming
for the same period. The Denver-Julesburg basin does not contain the
wealth of mineral resources found in many parts of the state, and
therefore has not experienced the population growth associated with
resource development. The areas within the basin which had the greatest
population increases over the last decade are within or adjacent to
Cheyenne and Wheatland (Figure II-l). Population increases in the
Wheatland area are due mainly to construction of a large power
generating plant. Growth around Cheyenne, the state capital, is a
reflection of rapid population growth in the state as a whole.
Land Use and Ownership
Approximately 95 percent of the land within the basin is utilized
for agricultural purposes, mainly for stock grazing with lesser acreages
used to raise crops. The small amount of non-agricultural land in the
basin is used for human habitation and recreation. About 88 percent of
the basin lands are privately owned, with most of the remainder owned by
the state.
GEOLOGY
Stratigraphy
The Denver-Julesburg basin is underlain by up to 12,000 feet of
sedimentary rocks which range in age from Cambrian to Recent and include
both marine and non-marine deposits. The sedimentary deposits
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unconformably overlie Precambrian basement rocks which are exposed in
the Laramie Mountains and Richeau dome on the west side of the basin,
and in the Hartville Hills (Figure II-3).
A generalized stratigraphic column for the Denver-Julesburg basin
indicating lithologies and stratigraphic sequence is given in
Figure II-2. Detailed descriptions of individual geologic units may be
found in Darton and others (1910), Denson and Botinelly (1949), Condra
and Reed (1950), McGrew (1953), Rapp and others (1953, 1957), Morris and
Babcock (1960), Denson and Bergendahl (1961), and Maughan (1963, 1964).
Summary descriptions of the units are included in Table IV-1.
Rocks of Paleozoic age generally consist of sandstones, shales, and
carbonates and are over 1,000 feet thick in the eastern part of the
basin. Outcrops of Paleozoic rocks are limited to the east edge of the
Laramie Mountains, Richeau dome, and the Hartville uplift.
Mesozoic rocks are divisible into three general lithologic
assemblages. The lowest unit consists of shales, siltstones, and
sandstones which range in age from Triassic to Lower Cretaceous and may
exceed 3,000 feet thick near the Denver-Julesburg basin trough. The
middle assemblage is a sequence of marine shales of Lower to Upper
Cretaceous age. This unit is up to 7,000 feet thick in some areas of
the basin. The two lower units of the Mesozoic rocks crop out over
small areas immediately east of the Laramie Mountains and along the
crest of Old Woman anticline (Figure II-3). The upper assemblage is
composed of up to 2,000 feet of sandstones and shales and crops out in
southern Goshen County.
Tertiary age sediments consist of fine- to coarse-grained
sandstones, siltstones, and claystones with a maximum thickness of more
15
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Figure II-2. General geologic column, Denver-Julesburg basin,
Wyoming.
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EXPLANATION
Precombrian rock
Anticline, with direction
of plunge
Syncline, with direction
of plunge
A A Thrust fault, sawteeth on side
of overriding block
D
Normal fault, showing relative
movement, dashed where
inferred
A Location of structure section
Figure II-3. Major structural features of the Denver-Julesburg
basin, Wyoming.
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than 2,000 feet. Tertiary rocks are at the surface or covered by
Quaternary deposits throughout over 90 percent of the Denver-Julesburg
basin.
Quaternary age alluvial, terrace, flood plain, and dune deposits
range from 0 to 200 feet thick. Alluvial deposits occur in all of the
major stream valleys of the basin and cover large lowland areas in
western Platte County and southeastern Laramie County.
Structural Geology
The general structural setting of the Denver-Julesburg basin is
depicted in Figures II-3 and II-4 and Plate 1.
The Denver-Julesburg basin is a broad synclinal trough located
immediately east of the Laramie Mountains, a northern extension of the
Rocky Mountain Front Range. The axis of the syncline trends north to
south in the southern part of the basin and northeast to southwest in
the northern part (Figure II-3 and Figure II-4). Pre-Tertiary rocks
adjacent to the Laramie Mountains are steeply dipping (Dockery, 1939).
East of the synclinal axis, sediments are nearly horizontal.
The basin is bounded on the west by the Laramie Mountains, and on
the north by the Hartville uplift and Old Woman anticline. The
structural basin extends eastward to the Chadron-Cambridge arch, 70 to
180 miles east of the Wyoming-Nebraska boundary, and southward to the
Las Animas arch, more than 160 miles south of the Wyoming-Colorado
boundary. For a descriptive summary of the structural features in the
Denver-Julesburg basin outside of Wyoming, refer to Anderman and Ackman
(1963).
The east flank of the Laramie Mountains is bounded by a series of
high angle thrust faults and tightly flexed folds from the
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A'
Wholen Fort Loromie
Foult Anticline
Denver-Jule&burg Basin
Trough
Seo Level —
12 5 Kilometer t
5 0 5 [0 15 20 M.les
5 0 5 10 15 20 25 Kilometers
Note Lines doihed where contact is inferred
Figure II-4.
Structural cross-sections, Denver-Julesburg basin, Wyoming. Lines of sections are
shown on Figure II-3. (A-A' after Droullard, 1963; B-B' based on data from
Petroleum Information files of the Wyoming Geological Survey.)
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Wyoming-Colorado state line north to the Hartville uplift (Figure II-3).
Maximum structural relief is approximately 17,000 feet between the
exposed Precambrian rocks of the Laramie Mountains and the
Denver-Julesburg basin trough near Cheyenne (Anderman and Ackman, 1963).
Separating the Denver-Julesburg basin from the Powder River basin
to the north is the Hartville uplift (Figure II-3 and Figure II-4,
cross-section A-A'). The uplift includes a broad southwest plunging
syncline (Broom Creek syncline), with the asymmetric Cassa anticline and
Hartville fault forming the western and eastern boundaries of the
topographically elevated Hartville Hills, respectively. Up to 12,000
feet of structural relief occurs between the Hartville uplift and the
trough of the Denver-Julesburg basin (Droullard, 1963). The southeast
flank of the uplift has a complex series of normal faults with
associated overturned beds. These include the Wheatland, Whalen, and
Hartville faults (Figure II-3).
To the west of the Cassa anticline the Hartville uplift is deformed
by the Elkhorn anticline and several small attendant faults. This
uplift extends west to the Laramie Mountains.
The Wheatland-Whalen fault system (Figure II-3 and Figure II-4,
cross-section A-A') produces major stratigraphic discontinuities between
the Hartville Uplift and the Denver-Julesburg basin proper. Along the
Whalen fault, evidence exists for two separate episodes of
movement—northwestward thrusting during the Laramide Orogeny and normal
faulting, with downdropping of the southeast block, during post-Miocene
time (Denson and Botinelly, 1949; Anderman and Ackman, 1963). Vertical
displacement in Paleozoic strata is 4,800 feet along the Whalen fault,
20
-------
whereas displacement in Tertiary beds is only 300 to 700 feet
(Droullard, 1963).
Hydrostratigraphy
All stratigraphic units within the Denver-Julesburg basin can
locally produce adequate amounts of water for stock or domestic use.
However, few of these units can regionally produce sufficient quantities
to be characterized as dependable water-bearing units. The
hydrostratigraphy for the Denver-Julesburg basin has been identified
through analysis of water yield reports in Wyoming State Engineer permit
records, oil and gas well test results, and previously published
ground-water studies.
Aquifers are defined herein as parts or all of geologic formations
that regionally produce adequate amounts of water for exploitation.
Aquifer stratigraphic boundaries are not necessarily limited by
formational boundaries; they are, however, limited by the relative
permeabilities of the rock units. Aquifers are classified as minor or
major, with minor aquifers characteristically producing sufficient water
only for stock or domestic purposes. Low permeability zones, composed
of siltstone, claystone, and shale, will generally yield little water to
wells, act to restrict ground-water flow between aquifers, and are
termed confining beds, or aquitards.
Where aquifers are not separated regionally by an aquitard, and have
similar recharge/discharge mechanisms and therefore similar ground-water
flow paths, they are considered to be in hydraulic connection and are
grouped as an integrated aquifer system. Individual member aquifers
within an aquifer system may be hydraulically isolated to varying
degrees locally by intervening low permeability horizons.
21
-------
Figure II-5 delineates the hydrostratigraphy of the
Denver-Julesburg basin. Several distinct water-bearing horizons are
identified. Where exposed, surficial weathered zones of Precambrian
granites and metasediments constitute a minor aquifer. The oldest
sedimentary rocks found within the basin—the Cambrian Flathead
Sandstone, limestones of the Mississippian-Devonian Guernsey Formation,
and sandstones and carbonates of the Pennsylvanian-Permian Casper and
equivalent Hartville formations—comprise the Paleozoic aquifer system.
The Hartville (Casper) aquifer has the greatest water producing
capability. This system is isolated from younger aquifers by shales of
the overlying Permian-Triassic Goose Egg Formation (Figure II-5).
The sequence of rocks from the Triassic Chugwater Formation through
the Upper Cretaceous Pierre Shale consists primarily of low permeability
shales and siltstones, but contains several dispersed permeable
sandstone horizons which are minor aquifers (Figure II-5). These
sandstones, with the exception of the lower Cretaceous Cloverly
Formation, are generally lenticular, discontinuous units which grade
laterally and vertically into relatively impermeable shales and
siltstones.
The Upper Cretaceous Fox Hills Sandstone and Lance Formation
(Figure II-5) consist of permeable sandstone beds and thin shale layers.
Collectively, the permeable sandstones constitute a minor aquifer. The
Lance/Fox Hills aquifer overlies the Pierre Shale, a thick (+5,000 feet)
regional aquitard, and is isolated from younger aquifers by the
relatively impermeable claystones and siltstones of the Oligocene White
River Group.
22
-------
Geologic Age
Lit hology
Geologic Unit
Hydrologic Role
Hydrologic Unit
Quaternary
Ailuvlol,flood ploin ond
terrace deposit*
Major Aquifer
Quaternary Aquifers
Tertiary
•'.v.o .•
Ogallala Formation
Major Aquifer
Tertiary
Aquifer
System
a-'iY.v
Arikaree Formation
White
River
Group
Brule Fm.
Aquitard w/Discontmuous
Ma|or Aquifers
— —
Chodron Fm.
Aquitord v/Oiscontinuout
Minor Aquifers
Lance Formation
Minor Aquifer
Lance-Fox Hills
Aquifer
¦V. v:v:.
Fox Hills Sandstone
Upper
Cretaceous
Pierre Shale
Major Aquitard
with Discontinuous
Minor Aquifers
1—1 1 L_1
Niobrara Formation
Frontier Formation
Lower
Cretaceous
Mowry Shale
Newcastle Sandstone
Minor Aquifer
Newcastle Aquifer
I.I.I
Skull Creek Shale
Aquitard
Cloverly Formation
Minor Aquifer
Cloverly Aquifer
Jurassic
Morrison Formation
Aquitard v/Oisconhnuous
Miner Aauifers
Sundance Formation
?
?
Triassic
Permian
Chugwater Formation
Aquitard w/Discontinuoui
Miner Aquifers
Chugwater Aquifer
Goose Egg Formation
Aquitard
\"\ i' fY | 'i r ri-t*?
Hartville
Formation
Casper
Formation
Major Aquifer
Paleozoic
Aquifer
System
Pennsylvanian
MississiDDian
Oevonlon
Cambrian
1 ^ - 1 1 1 l( 1
.'P.v..' ¦'v.vix:7vV: .0-:
Guernsey Formation
Flathead Formation
Minor Aquifer
Precambrian
w \ / \
/ * N-" \ "/ * /
Precambrian Rocks
Minor Aquifer
Precambrian
Aquifer
Figure II-5. Hydrostratigraphy of Che Denver-Julesburg basin, Wyoming.
23
-------
The youngest water-bearing bedrock unit within the basin is the
Tertiary aquifer system. This system is comprised of sandstones and
conglomeratic lenses and channel deposits of the Miocene Arikaree and
the Miocene-Pliocene Ogallala formations (Figure 11-5). Locally, where
the underlying White River Group contains coarse-grained channel
deposits or zones of secondary permeability, it is considered part of
the system. Elsewhere, the siltstones and claystones of the White River
Group hydraulically isolate the Tertiary aquifer system from underlying
water-bearing zones.
Where present, Quaternary age flood plain and terrace deposits of
sand and gravel represent a major aquifer.
Available data on the hydrologic properties of and circulation of
ground water within the above aquifers is presented in Chapter IV.
Ground-water quality is discussed in Chapter V.
24
-------
III. WATER USE
-------
III. WATER USE
Water use within the Denver-Julesberg basin is estimated at
approximately 410,000 acre-feet/year; of this total about 53 percent
(218,000 acre-feet/year) is surface water and 47 percent (192,000
acre-feet/year) is ground water.
Agricultural water use accounts for about 87 percent (355,260
acre-feet/year) of the total basin water use, almost solely for
irrigation. Slightly more than half of the irrigation water is supplied
by the North Platte River; the Tertiary aquifer system and Quaternary
aquifers supply most of the ground water.
Public and domestic water use is estimated at 7 percent (29,000
acre-feet) of the basin's annual water demand. About two-thirds of the
public and domestic water demand is met by ground water, derived mainly
from the Tertiary aquifer system. Interbasin transfer of surface water
supplies the remaining public water needs.
Industrial use is about 6 percent (26,000 acre-feet/year) of the
basin's total water needs, with surface water supplying about 80 percent
of these demands. Ground water for industrial use is supplied by the
Tertiary aquifer system.
Water use by economic sector is discussed below, and summarized in
Table III-l and Figure III-l. Additional data on water use are
contained in Appendix A.
26
-------
Table I1I-1. Water use in the Denver-Julesburg basin, Wyoming.
Economic Sector
Estimated
Total Water Use
(ac-ft/yr)
Estimated Ground-Water
Use (ac-ft/yr)
Percent of Total
Ground-Water Use
Estimated Surface Water
Use (ac-ft/yr)
Percent of Total-
Surface Water Use
Percent of Total
Water Use
N3
-J
Agricu1ture
lrrigat ion
Industrial Water Supply
Domestic Water Supply
Public Water Supply
Munic ipa1
Non-Municipal
Non-Commun ity
331,500
26,000
5,505
22,050
180
233
165,200
3,760b
5,000
5,505
12,050
180
233
19
100
52
100
100
Tertiary
aquifer
system,
Quaternary
aquifers
Tertiary
aquifer
system
Table A-l
Tertiary
aquifer
system,
Quaternary
aquifers
Table A-2
Table A-3
Table A-4
86
6
<0.01
<0.01
186,300
11,000
0
0
53
48
North Platte
system
85
3 21 ,000 81 Table A-l
3 -
10
Douglas Creek
5
<1
<1
410,228
191,928
47
218,300
53
aPercent of total use for the economic sector.
^For calculations assuming all stock use is supplied by ground water.
-------
. IRRIGATION
•351,500 A-F/Y
STOCK (1%) 3760 A-F/Y
DOMESTIC (1%)
5505 A-F/Y
PUBLIC SUPPLY (6%)
23,460 A-F/Y
INDUSTRIAL 16%) 26,000 A-F/Y
Figure III-l. Estimated water use in the Denver-Julesburg basin, Wyoming.
Shaded area represents surface-water use; unshaded area
represents ground-water use.
28
-------
AGRICULTURAL WATER USE
Irrigation
An estimated 296,000 acres of land are permitted for irrigation
within the basin. About 138,000 acres are irrigated with ground water
(Wyoming State Engineer, 1981). The Wyoming Water Planning Program
(1971) indicates that as of 1969, roughly 158,000 acres were permitted
for surface water irrigation within the basin boundaries. More recent
figures on lands irrigated with surface water are not available.
However, the 1969 estimate is considered accurate, as dependable surface
water supplies within the basin were largely appropriated by 1930
(Wyoming Water Planning Program, 1973).
During 1978, about 212,500 acres of irrigated land were cultivated
within the basin (Wyoming Crop and Livestock Reporting Service, 1979),
72 percent of the total permitted acreage. Acreages of the various
crops harvested and the average annual consumptive water requirements
for the respective crop types were used to estimate a basinwide
irrigation water use of about 351,500 acre-feet/year (Table III-2).
Assuming a constant irrigated acreage, and similar crop type
distribution on lands irrigated by surface water and by ground water,
roughly 186,500 acre-feet/year of surface water and about 164,500
acre-feet/year of ground water are used for irrigation.
Use of ground water for irrigation is largely limited to specific
areas within the basin. Aquifers developed for irrigation within these
areas include: (1) the Arikaree aquifer (Tertiary aquifer system) in
parts of northern Goshen and southern Niobrara counties; (2) the
Arikaree aquifer and Quaternary aquifers in Wheatland Flats and adjacent
areas; (3) Quaternary terrace aquifers and the White River aquifer
29
-------
Table III-2. Irrigation water use, Denver-Julesburg basin, Wyoming.
Annual Consumptive
Annual
Irrigation Requirement
Water Use
County
Crop
Acreage
(inches)
(acre-feet)
Goshen
wheat-barley-oats
5,900
23.06
11,338
beans
11,800
11.65
11,455
beets
14,200
16.66
19,714
corn
33,300
17.82
49,450
hay
40,600
21.12
71,456
county total
105,800
-
163,413
Laramie
wheat-barley-oats
9,300
21.86
16,941
beans
700
10.98
7,686
beets
300
15.39
1,026
corn
2,600
16.45
3,564
hay
25,000
19.94
41,542
county total
37 ,900
-
70,759
Niobrara
wheat-barley-oats
5,200C
20.13
8,723
corn
1,700C
16.13
2,285
hay
10,500°
18.46
16,152
county total
17 ,400C
-
27,160
Platte
wheat-barley-oats
4,700
24.14
9,474
beans
2,100
12.97
2,270
beets
2,600
17.66
3,826
corn
13,000
19.23
20,833
-------
Table III-2. (continued)
County
Crop
Acreage3
Annual Consumptive
Irrigation Requirement
(inches)
Annual
Water Use
(acre-feet)
Platte (contd.)
hay
29,000
22.23
53,722
county total
51,400
-
90,126
Basin Total
212,500
-
351,458
Wyoming Crop and Livestock Report, 1979.
^From Trelease and others, 1972. Stations used to calculate county irrigation requirements are
Torrington (Goshen Co.), Pine Bluffs (Laramie Co.), Lusk (Niobrara Co.), and Wheatland (Platte Co.).
c
Includes all of Niobrara County.
-------
(Tertiary aquifer system) in the area around Pine Bluffs and the
southeast part of Goshen Hole; and (4) the Ogallala aquifer (Tertiary
aquifer system) in northeast Laramie County.
The North Platte River system supplies virtually all surface water
used for irrigation.
Livestock
Livestock water use within the basin is estimated at 3,760 acre-
feet/year, based on cattle and sheep populations of about 239,000 and
52,000, respectively (Wyoming Crop and Livestock Reporting Service,
1979), and daily water consumption of about 15 and 3 gallons per day
(gpd), respectively. Ground water is assumed to supply all stock-water
use. The Tertiary aquifer system and Quaternary aquifers are the major
sources of stock water, although older aquifers are used where they are
not deeply buried along the basin periphery.
PUBLIC AND DOMESTIC WATER USE
Public and domestic drinking water use is estimated at 29,000
acre-feet/year (U.S. Environmental Protection Agency, 1978, and
preliminary 1980 Census figures). About 18,000 acre-feet/year is
derived from ground-water sources, with the remainder being surface
water transferred into the basin. Public and domestic water uses are
discussed separately below.
Public Water Use
Public water systems are subdivided into municipal, non-municipal
community, and non-community supplies. Municipal systems are publicly
owned and operated, and within the basin serve incorporated places or
water-user districts. Non-municipal community systems are privately
32
-------
owned, and serve a permanent population of 25 or more. These systems
are associated with trailer courts and one company town in the basin.
Non-community systems are privately owned, serve a transient population
of over 25, and are mainly restaurants, inns, schools, and recreation
areas.
Municipal Water Use
Municipal water use is about 23,050 acre-feet/year. Slightly over
one-half (12,050 acre-feet/year) is derived from ground-water sources,
mainly the Tertiary aquifer system with lesser amounts withdrawn from
the Quaternary and Lance aquifers (Appendix A, Table A-l). The
remainder of municipal water demands, 11,000 acre-feet/year, is supplied
by water transferred from the Little Snake River system of south-central
Wyoming for the City of Cheyenne. This surface water transfer is about
75 percent of the city's water supply.
Non-Municipal Community and Non-Community Water Use
Non-municipal community and non-community water systems use about
180 and 233 acre-feet/year, respectively. The Tertiary aquifer system
supplies most of this water. Tables A-2 and A-3 (Appendix A) summarize
water use for these systems.
Domestic Water Use
No records of domestic water use exist for the basin. According to
1980 preliminary census figures and data from the U.S. Environmental
Protection Agency (1978), roughly 28,600 persons are not served by a
community water system. Based on an average use of 180 gallons/
capita/day (Wyoming Water Planning Program, 1973), domestic use is
estimated at 5,175 acre-feet/year. Ground water from several aquifers
33
-------
is used for domestic supplies (Plate 2), although the vast majority of
permitted domestic wells are completed in the Tertiary aquifer system or
Quaternary aquifers. Within Goshen Hole (Figure II-l) where the Lance
aquifer crops out, this unit is developed for domestic needs. Older
units, especially weathered surficial zones of the Precambrian, are used
where they crop out along basin margin uplifts.
INDUSTRIAL WATER USE
Industrial water use within the basin is estimated at 26,000
acre-feet/year, and is supplied by about 21,000 acre-feet/year of
surface water and 5,000 acre-feet/year of ground water. This estimate
includes a 23,250 acre-feet/year projected water use for the Missouri
Basin Power Project, currently under construction near Wheatland (Figure
II-l) and scheduled for completion in the early 1980s. Ground-water
withdrawals of 2,750 acre-feet/year from the White River aquifer
(Tertiary aquifer system) are permitted for the project (Wyoming State
Engineer, 1981), with surface water from the Greyrocks Reservoir
(Laramie River) (Figure II-l) furnishing the remainder of the project's
needs.
Petroleum industry water use is about 1,900 acre-feet/year. The
majority of this water, about 1,680 acre-feet/year, is used by the Husky
Oil Company Refinery near Cheyenne, and is purchased from the City of
Cheyenne. Additional petroleum industry water use includes about 145
acre-feet/year withdrawn as a by-product of petroleum production, mainly
from the Newcastle aquifer at Horse Creek oil field (T. 16-17 N., R. 68
W.); about 88 acre-feet/year is withdrawn from the White River aquifer
(Tertiary aquifer system) at Horse Creek, and is used for secondary oil
recovery.
34
-------
Other industrial water users in the basin are Wycon Chemical
Company, which withdraws about 870 acre-feet/year from the Ogallala
aquifer (Tertiary aquifer system) in T. 13 N., R. 67-68 W. , and Holly
Sugar Company, which uses about AO acre-feet/year, mainly from the North
Platte River. Industrial water use is summarized in Table A-4
(Appendix A).
35
-------
IV. AQUIFER PROPERTIES AND
GROUND - WATER CIRCULATION
-------
IV. AQUIFER PROPERTIES AND
GROUND-WATER CIRCULATION
Existing data from water wells and oil well tests indicate that
virtually all strata within the Denver-Julesburg basin yield water to
wells. Even thick shale sequences, generally considered aquitards, will
yield water from fractured zones and sandy intervals. However, only a
few units are considered aquifers on a regional basis. The following
sections discuss the hydrologic properties of and ground-water
circulation within the important aquifers and aquifer systems identified
in the basin. Hydrologic and lithologic characteristics for all
stratigraphic units within the basin are summarized in Table IV-1. The
well numbering system used in this report is explained in Appendix B.
PALEOZOIC AQUIFER SYSTEM
The Paleozoic aquifer system consists of up to 1,300 feet of
Cambrian through Permian age sandstones and carbonates. Formational
members of this system include the Cambrian Flathead Sandstone, the
Mississippian-Devonian Guernsey Formation, and the Pennsylvanian-Permian
Casper and equivalent Hartville formations.
The Flathead Sandstone, present in parts of the northern basin,
consists of up to 60 feet of quartzitic sandstone and conglomerate
(Morris and Babcock, 1960). The Guernsey Formation contains mainly
limestones and dolomites with minor interbedded shales and siltstones.
Maximum thickness is about two hundred feet. In the far northern part
of the basin the equivalent Madison Limestone is present and varies from
100 to 300 feet in thickness (Eisen and others, 1980).
38
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Table IV-1. Lithologic and hydrologic characteristics of rock units in the Denver-Julesburg basin, Wyoming.
ERA
System
Series
Geologic
Unit
Thickness
(ft)
Lithologic Characteristics
Hydrologic Characteristics
CENOZOIC
Quaternary Recent
and
Alluvial
flood plain
and terrace
deposits
Pleistocene
0-200
Fine sands, silts, and clays, to
poorly sorted coarse sands and
gravels, cobbles and boulders
locally.
Sand, gravel, cobbles, and
boulders, contain some lenses
of clay, silt, and fine sands.
Major aquifer. Main deposits located
along N. Platte River, Wheatland FlaL^
Pine Bluffs Lowland. Developed
heavily for irrigation in these areas.
Yields are generally 500-1,000 gpm but
exceed 3,000 gpm locally.
Permeability: 700-9,600 gpd/ft
Transmissivity: 6,500-1,650,000 gpd/ft:
Specific Capacity: 2.5-250 gpm/ft
Tertiary Pliocene Ogallala
Formation
0-330 Heterogeneous deposits of gravel,
sand, and silt containing some
cobbles and boulders. May be
either unconsolidated or well
cemented. Increases in thickness
in southern portion of study area.
Present mainly as channel
deposits in Platte and Goshen
counties.
Major aquifer. Member of Tertiary
aquifer system. Present mainly in
Laramie County and is utilized for
irrigation, municipal and industrial
supplies. Yields of several hundred
gpm common, and coarse channel
deposits yielding over 1,000 gRm.
Permeability: 160-4,000 gpd/ft (?)
Transmissivity: 1,610-700,000 gpd/ft
Specific Capacity: 0.26-229 gpm/ft
Miocene Arikaree 0-1200
Formation
Loose to moderately cemented
very fine to fine grained
sand and silt. The basal unit
consists of coarse channel
conglomerate.
Major aquifer. Member of Tertiary
aquifer system. Present over much of
the basin. Developed for irrigation,
municipal, and industrial supplies.
Yields are commonly several hundred
gpm to over 1,000 gpm locally.
Permeability: 1.3-375 gpd/ft
Transmissivity: 110-77,000 gpd/ft
Specific Capacity: 0.2-230 gpm/ft
Oligocene White River 0-1120
Group
Brule Formation 0-420
Argillaceous siltstone with
channel deposits of sand and
sandstone, localized beds of
limestone, moderately thick beds
of clay and a few beds of volcanic
ash.
Aquitard with discontinuous major
aquifers. Member of Tertiary aquifer
system where coarse channel deposits
or zones of secondary permeability are
present. Yields over 1,000 gpm pos-
sible often in these areas. Elsewhere
yields are low, although adequate for
stock or domestic use. High yields
available in southeast and east-
central basin.
Permeability: <0.02-36 gpd/ft
Transmissivity: 480-780,000 gpd/ft
Specific Capacity: 0.4-257 gpm/ft
-------
Table IV-1. (continued)
ERA
System
Series
Geologic
Unit
Thickness
(ft)
Lithologic Characteristics
Hydrologic Characteristics
CENOZOIC Tertiary Oligocene Chadron 0-700 Consists mainly of bentonitic,
(cont.) (cont.) Formation loosely to modererately cemented
clay and silt. Contains channel
deposits of sandstone and
conglomerate. Lower unit con-
sists of variegated fluviatile
deposits.
Aquitard with discontinuous minor
aquifers. Developed for stock and
domestic use in Goshen Hole area.
Dispersed, coarse-grained channel
deposits are major water-bearing
zones. Yields are commonly less than
15 gpm.
MESOZOIC Cretaceous
Upper Lance 0-1500 Sandstone with beds of soft
Cretaceous Formation shale and coal. Absent in
northern portion of study area.
Minor aquifer. Developed mainly where
exposed in Goshen Hole for stock or
domestic supplies; also supplies town
of Yoder. Yields generally <25 gpm
to 100 gpm locally. ^
Permeability: 7.5-125 gpd/ft
Transmissivity: 450-5,000 gpd/ft
Specific Capacity: 0.4-257 gpm/ft
O
Fox Hills
Sandstone
0-550
Medium-grained silty sandstone
interbedded with shale.
Minor aquifer (?). Not developed as r.
water source within basin; hydrologic
properties unknown.
Pierre 0-5700 Predominantly shale containing Major aquitard with discontinuous
Shale thin to moderately thick beds minor aquifers. Dispersed sandstone
of sandstone. beds yield 10-25 gpm to stock/domestic
wells in outcrop areas.
Niobrara 0-500 Calcareous shale with a 20-foot
Formation bed of nearly pure chalk near
the middle. Contains thin
bentonite beds in some areas.
Base is a 25-foot bed of dense
sandstone.
Aquitard with discontinuous minor
aquifers. Not developed as a water
source within basin. Basal sandstone
will likely yield water to wells.
Frontier 0-1400+ Mainly shales with beds of
Formation limestone and sandstone. Includes
formations from top of Lower
Cretaceous to base of Niobrara
Formation.
Aquitard with discontinuous minor
aquifers. Not developed as a water
source within basin. Dispersed sand-
stones might yield water.
Porosity: 4-17% „
Permeability: <0.05 gpd/ft
-------
Table IV-1. (continued)
ERA
System
Series
Geologic
Unit
Thickness
(ft)
Lithologlc Characteristics
Hydrologic Characteristics
MESOZOIC Cretaceous Lower Mowry
(cont.) (cont.) Cretaceous Shale
80-220+ Siliceous shale containing
numerous beds of bentonite.
Formation thins out to the
southeast.
Aquitard. Not developed as a water
source within basin; hydrologic
properties unknown.
Newcastle 0-1100+ Coarse-grained massive sand-
Sandstone stone interbedded with silt-
stone and claystone. Equivalent
to the Muddy Sandstone.
Minor aquifer. Yields of 10-20 gpn
likely, sufficient for stock or
domestic use.
Porosity: 2-25%
Permeability: 0-4.7 gpd/ft
Transmissivity: 0-41 gpd/ft
Skull Creek
Shale
70-200+
Fissile shale interbedded
with limestone.
Aquitard. Not developed as a water
source within basin. Hydrologic
properties unknown.
Cloverly 0-300 Sandstone, conglomerate, quart-
Formation zite, siltstone and shale. In
outcrop upper and lower sandstone
units are separated by shale.
Equivalent to Inyan Kara Group to
the north of study area.
Jurassic
Morrison
Formation
0-250
Variegated shale, thin sand-
stone, and limestone beds.
Minor aquifer. Yields 10-20 gpm in
far northeast part of basin, 33 gpm to
spring in north-central basin.
Porosity: 7.3-12.2%
Permeability: 0-0.3 gpd/ft
Aquitard with discontinuous minor
aquifers. Yields 5 gpm to one well
along western basin flank. Sandstone
units are local aquifers.
Sundance 0-550 Predominantly sandstone and sandy Minor aquifer (?). Not developed as a
Formation shale. water source within basin. Sandstones
would likely yield adequate stock and
domestic water supplies.
Triassic Chugwater 0-675 Siltstone and very fine-grained Aquitard with discontinuous minor
Formation sandstone. aquifers. Yields 5-15 gpm to stock/
domestic wells along west bdsin
margin.
-------
Table IV-1. (continued)
Geologic Thickness
ERA System Series Unit (ft) LitholoRic Characteristics Hydrologic Characteristics
MESOZOIC Triassic
(cont.) (cont.)
Goose Egg 0-450 Siltstone and sandstone Aquitard. Not developed as a water
Formation interstratified with limestone, source within basin. Sandstones may
PALEOZOIC dolomite, and gypsum. produce small yields.
Permian
Pennsylvanian
ho
Hartville 0-1225 Primarily carbonate sequence with
Formation interbedded silts and shales and
(Casper Fra. distinct upper and lower sand-
equivalent) stone members ("Converse sands"
and Fairbank Member, respectively).
To the southwest, near the Laramie
Mountains, sandstone percentage
increases and shale and limestone
percentages decrease (Casper
Formation). Sandstones are
arkosic, quartzitic and cross-
bedded .
Major aquifer. Member of Paleozoic
aquifer system. Sandstones and frac-
tured carbonates represent major
water-bearing zones. Yields generally
less than 100 gptn, but locally up to
800 gpm. Where fractured, high yields
are likely.
Permeability: 0.7-86 gpd/ft
Transmissivity: 340-10,300 gpd/ft
Specific Capacity: 0.06-4.8, possibly
400(?) gpm/ft
Mississippian
Devonian
Guernsey 0-200 Cherty, massive to thin-bedded
Formation carbonates with minor dolomitic
shale and siltsonte.
Minor aquifer. Member of Paleozoic
aquifer system. Not generally devel-
oped as a water source within basin.
One well in north-central basin
reportedly yields 750 gpm.
Cambrian Flathead
Sandstone
0-60+ Coarse-grained conglomeratic
quartzitic sandstone.
Minor aquifer (?). Member of Paleo-
zoic aquifer system. Not developed
as a water source within basin. Will
likely yield small quantities of
water.
Precambrian Igneous and ? Complex sequence of gneiss, Minor aquifer. Weathered surficial
Metamorphic schist, granite, phyllite, zones will yield adequate water for
Rocks quartzite, and limestone; stock and domestic use.
intruded by ultrabasic rocks
and permatite dikes.
aData sources: Darton and others (1910), Maughan (1963), Maughan (1964), Denson and Botinelly (1949), Denson and Bergendahl (1961),
Rapp and others (1953), Rapp and others (1957), Condra and Reed (1950), Morris and Babcock (1960), and McGrew (1953).
-------
The Pennsylvanian-Permian Casper Formation, present along the
southern part of the Laramie Mountains, consists of 1,100 to 1,200 feet
of interbedded limestones and sandstones. Limestone units reach
thicknesses of over 150 feet, with the sandstone interbeds rarely
exceeding 80 feet in thickness. Total sandstone content of the Casper
is 30 to 40 percent in this area (Eisen and others, 1980). The
Hartville Formation is present in the Hartville Hills area, and consists
primarily of carbonates and fine-grained clastic rocks, with lesser
amounts of sandstone. Three sandstone horizons, commonly termed the
"Converse" and "Leo" sands and the Fairbank Member, exist within the
upper, middle, and lower parts of the Hartville, respectively. The
"Converse" sands and Fairbank Member reach 100 feet in thickness
locally, while the "Leo" sands are considerably thinner and locally
absent. Where the Hartville Formation crops out in the Hartville Hills,
the "Converse" sands have been largely eroded away. Total sandstone
percentage of the Hartville Formation is generally less than 20 percent
and decreases to the east (Eisen and others, 1980).
The Paleozoic aquifer system crops out along the southern part of
the Laramie Mountains, in the Richeau dome, and in the Hartville Hills
(Figure II-3 and Plate 3). Between the Richeau dome and Hartville
Hills, and westward to the Laramie Mountains, the system is absent
(Figure IV-1). Throughout much of the basin, the system lies at great
depths, exceeding 10,000 feet along the basin axis.
The low permeability shales of the overlying Permian-Triassic Goose
Egg Formation isolate the Paleozoic aquifer system from younger
aquifers. Precambrian granites and metasediments underlie the system.
43
-------
EXPLANATION
*¦•5000— Potennometric Contour in feet above
mean sea level (dashed where
inferred, contour interval 250 feet)
Data range over 30 yeors
Data Sites
x Spring 9 Soring in Precambrian rocks
o Water Well (solid symbol mdicotes
well flows ot surfoce)
A Oil Well Drill Stem Test
Figure IV-1. Potentiometric map of the Paleozoic aquifer system,
Denver-Julesburg basin, Wyoming (modified from Eisen
and others, 1980).
44
-------
Identified as major water-producing zones within the Paleozoic
aquifer system are the permeable sandstones of the Casper and Hartville
formations, and, where structural deformation has produced significant
fracturing, carbonate rocks of the Casper, Hartville, and Guernsey
formations. Eisen and others (1980) identify areas along the Laramie
Mountains and within the Richeau dome and Hartville Hills areas where
significant fracturing of the Paleozoic strata has occurred.
Unfractured carbonate rocks within the system have generally low perme-
abilities and are considered minor aquifers. Water production potential
of the Flathead Sandstone is largely unknown.
Hydrologic Properties
Available data on the hydrologic properties of the Paleozoic
aquifer system within the Denver-Julesburg basin are sparse. No
reported permeability or transmissivity values exist. Data from pump
tests of three wells located one to three miles north of the basin
boundary (T. 29 N., R. 68-69 W.) indicate that, where undeformed, the
"Converse" sands have permeabilities between 22 and 86 gallons per day
2
per square foot (gpd/ft ) and transmissivities between 2,000 and 10,300
gallons per day per foot (gpd/ft). One test in unfractured Hartville
carbonates in the same area indicates permeability and transmissivity of
2
0.7 gpd/ft and 340 gpd/ft, respectively (Welder and Weeks, 1965).
Data from the Laramie basin indicate that, --.'here fractured, perme-
2
abilities of the Casper aquifer are 125 to 300 gpd/ft and locally
2
10,000 gpd/ft . Associated transmissivities vary from 8,000 to 195,000
gpd/ft, and may exceed 1,000,000 gpd/ft (Lundy, 1978; Richter, 1980).
Fractured Paleozoic zones within the Denver-Julesburg basin may have
45
-------
permeabilities and transmissivities of similar magnitude to those of the
Casper aquifer in the Laramie basin (Eisen and others, 1980).
Available specific capacity data for the Paleozoic aquifer system
within the basin are for Hartville carbonates in the Hartville Hills
area (Table IV-2), and vary from less than 0.1 to 5.0 gallons per minute
per foot of drawdown (gpm/ft). Well yields are generally 10 gpm or less
from Hartville carbonates, and up to 80 gpm from the "Converse" sands.
Two anomolously high yields, 750 and 800 gpm, are reported for the
Guernsey and Hartville carbonates, respectively. These high yields
suggest the presence of secondary permeability.
Ground-Water Circulation
A potentiometric map for the Paleozoic system is shown in Figure
IV-1. Outcrop areas in the Laramie Mountains, Richeau dome, and
Hartville Hills act as recharge zones. Flow from the Laramie Mountains/
Richeau dome outcrops is to the east and northeast, into the basin.
Available data indicate flow from the Hartville Hills outcrops is to the
southwest, converging along the Broom Creek syncline. Additional flow is
to the northeast, roughly paralleling basin-bounding structures. Flow
to the southeast is disrupted by the Whalen fault. The nature of this
disruption is not currently known.
Recharge to the system is through direct outcrop infiltration of
precipitation and leakage from streams and reservoirs. Estimates by
Eisen and others (1980) indicate outcrop areas on the east flank of the
Laramie Mountains and within the Hartville Hills receive 5,200 and 8,400
acre-feet/year of recharge, respectively, from precipitation. An
unknown quantity is discharged by springs, and therefore limits
intrabasin recharge. Additionally, about 6,600 acre-feet/year enters
46
-------
Table IV-2. Hydrologic properties of the Paleozoic aquifer system, Denver-Julesburg basin, Wyoming.
Test
Specific
Well
Duration
Drawdown
Discharge
Capacity
Transmissivity
Storage
Permeability
(Rpd/fO
Locat ion
(hours)
(ft)
(upm)
(Rpm/ft)
(gpd/ft)
Coefficient
Remarks3
Source
27/65-7 ac
750
Well completed in
10
Guernsey(?) aquifer
27/66-15
aaa
15(?)
Well completed in Hartville
and Guernsey aquifers
9
'27/66-22
cb
4
14
32
2.3
9
27/66-27
cb
4
7
9
27/70-24
ad
4
2( ?)
800
400(?)
9
28/65-14
dba
50
3
0.06
9
28/65-20
ccc
3
9
28/65-30
ddd
1
70
3
0.04
9
26/66-1 1
bed
2
5
20
4.0
9
26/66-2 bac
2
0
20
9
26/66-13
edd
1
0
10
9
26/66-24
cad
1
1
5
50
9
26/66-28
abc
5
9
29/64-19
bad
1
0
10
9
29/64-30
deb
3
9
29/65-21
cdb
1
30
10
0.33
9
29/66-14
ca
20
9
29/66-15
bb
2
9
29/66-20
cab
5
9
29/66-26
bd
3
9
29/66-35
dac
2
40
9
29/66-35
dad
2
0
40
9
29/68-20
abb
0.5
126
33
0.3
-A
3
29/68-20
abd
24
30
78
2.6
10,300
2x10
86
Well in "Converse Sand" of
Hartville aquifer; well
completed several miles
north of basin boundary.
4
29/69-24
dbc
12
67
38
0.6
340
0.7
Well in "Converse Sand" of
Hartville aquifer; well
completed several miles
north of basin boundary.
4
29/69-24
dbc
24
27
60
2.2
2,100
25
Well in "Converse Sand" of
Hartville aquifer; well
completed several miles
north of basin boundary.
4
29/69-33
bac
12
5.8
14.6
2.5
2,000
22
Well in "Converse Sand" of
Hartville aquifer; well
completed several miles
north of basin boundary.
4
aData are for the Hartville aquifer unless otherwise noted.
^Data sources for hydrologic properties are listed in Table IV-10, unless given.
-------
the system as leakage from the Guernsey Reservoir-North Platte River
system (Eisen and others, 1980), just north of the basin boundary.
Total recharge to the system, therefore, is about 20,000 acre-feet/year,
less spring discharge.
MESOZOIC AQUIFERS
The sequence of rocks from the Triassic Chugwater Formation through
the Upper Cretaceous Pierre Shale is composed of primarily low
permeability shales and siltstones. Several permeable sandstone
horizons within this sequence are identified as minor aquifers. These
include: (1) discontinuous sandstones within the Triassic Chugwater and
Jurassic Morrison formations; (2) two sandstone units within the Lower
Cretaceous Cloverly Formation; (3) the Lower Cretaceous Newcastle
Sandstone; (4) discontinuous sandstones within the Upper Cretaceous
Frontier Formation; and (5) discontinuous sandstones within the Upper
Cretaceous Pierre Shale (Table IV-1). Development of these aquifers,
for stock and domestic purposes, is limited to outcrop and near-outcrop
areas adjacent to the Laramie Mountains and along the flanks of Old
Woman anticline in the far northeast part of the basin.
Hydrologic Properties
Hydrologic properties of Mesozoic aquifers are poorly known, and
limited to data from the petroleum industry (Table IV-3). The majority
of the data are for the Newcastle aquifer, historically a major zone for
oil exploration in the area. Newcastle porosities are generally about
15 percent, and locally exceed 20 percent. Reported permeabilities vary
2
from essentially 0 to about 5.0 gpd/ft , and tested interval transmis-
sivities range up to about 40 gpd/ft. Sparse data from other Mesozoic
48
-------
Table IV-3.
Hydrologic properties
of Mesozoic aquifers, Denver-Julesburg basin,
Wyoming.3
Tested Interval
Tested Interval
Depth 1
Porosity
P ermeability
Thickness
Transmissi vity
Tested Inl
Location
Aquifer
(%)
(millidarcies)
(spd/£t )
(ft)
(epd/£t)
(ft)
13/61-8 db
Newcastle
8-19
<1-1
<0.02
7,820
13/63-4 aa
Newcastle
7-12
-
-
8,350
14/60-5 be
Newcas tie
17.7-20
130-249
2.4-4.5
7,362
14/60-22 ac
Newcastle
13. 7
13-55
0.2-1
7,549
14/60-27 cb
Newcastle
23.3
43-63
0.8-1.1
7,346
14/60-27 dc
Newcastle
22
64
1.1
7
8
7,484
14/60-27 cc
Newcastle
18.6
24
0.4
7,365
14/60-29 be
Newcastle
6.2-17.5
<3
<0.05
7,406
14/60-30 da
Newcastle
9-17
<14
<0.25
7,419
14/60-33 ca
Newcas tie
18
5
0.09
5
<1
7,521
15/60-15 db
Newcastle
8.6-13
2-121
0.04-2.2
7,513
15/61-28 bd
Newcastle
17.2
71
1.3
14
18
7,653
15/61-29 da
Newcastle
13.8
39
0.8
6
5
7,700
15/67-19 bb
Newcastle
2.9-12
<1
<0.02
10,442
16/61-19 db
Newcastle
17. 3
99
1.8
23
41
7,673
16/62-19 db
Newcastle
17. 7
76
1.4
10
14
8,036
16/62-19 bd
Newcastle
11.9
21
0.4
9
4
8,082
16/62-20 bd
Newcastle
15.7
51
0.9
14
12.6
7,969
16/64-5 da
Newcastle
12.6
3
0.05
11
<1
8,729
16/64-23 bb
Newcastle
13.7
<3.2
<0.06
8,591
17/62-14 bb
Newcastle
14.7-19
2-256
0.04-4.7
7,889
17/62-19 da
Newcastle
10.9-22.2
2-138
0.04-2.5
8,107
17/63-13 bb
Newcastle
6.8-23.7
1-45
<0.02-0.8
7,990
17/64-5 dd
Newcastle
4.5-23.3
0-61
0-1.1
8,723
18/64-35 cc
Newcastle
3.4-13.4
<1
<0.02
8,400
19/60-15 aa
Newcas tie
21
160
2.9
2
6
6,670
19/60-15 da
Newcastle
25
172
3.1
6,762
20/67-26 cc
Newcastle
3.7-11.8
<0.6
<0.05
9,204
21/63-10 aa
Newcastle
4.6-7.3
<0.1
<0.02
8,004
21/64-15
Newcastle
12.7
0.2
<0.02
8,812
22/62-7
Frontier
4.4-16
0-1.3
<0.02
24
<1
6,953
22/62-7
Newcastle
7.8-16.1
0.1-1.4
<0.02
7,724
22/63-27
Cloverly
7.3-12.2
0.1-18
0-0.3
8,131
23/61-4
Newcastle
13-20
0-63
0-1.1
6,984
23/62-27
Frontier
7.4-17.8
<3
<0.05
6 ,49i
23/66-5
Frontier
4.4-15.9
0.2-1.4
<0.02
3,538
23/67-1
Newcastl e
1.2-15.6
0-2.4
<0.04
3,003
24/61-20
Newcastle
5.2-19.5
0-128
0-2.3
6,578
25/60-31
Mowry
2.4-8.4
0-0.1
<0.02
6,265
25/62-25
Newcastle
2-18
0-137
0-2.5
6,265
26/60-31
Newcastle
19.2-22.1
1.2-2.2
<0.04
6,646
28/60-22
Newcastle
4.1-21.5
0-69
0-1.2
5,341
28/60-35
Newcastle
16-25.8
1.1-18
0.02-0.3
5,575
30/62-1
Newcastle
13.8-23.4
6.7-168
0.12-3.1
2,566
aData source: 11 (see Table 1V-10).
-------
aquifers indicate generally lower porosities and permeabilities,
relative to the Newcastle aquifer (Table IV-3).
Well and spring yields from Mesozoic aquifers are given in Table
IV-4. Yields are generally about 10 gpm. The highest reported yield is
33 gpm from a group of Cloverly aquifer springs (29/68-35 cb). In areas
immediately north of the Denver-Julesburg basin, the Cloverly is an
important aquifer capable of yields up to 250 gpm (Crist and Lowry,
1972) and may represent an important, though currently undeveloped,
water source in parts of the basin.
Ground-Water Circulation
Ground-water movement within Mesozoic aquifers is generally
unknown. The dispersed, discontinuous nature of sandstone aquifers
within all units except the Cloverly make interpretation of
potentiometric data difficult.
Stock (1981) has developed potentiometric data for the Cloverly
aquifer in the far northern end of the basin. In this area, the
Cloverly crops out along the east flank of the Old Woman anticline
(Figure II-3). Outcrop recharge waters move downdip, to the east, into
South Dakota. Artesian conditions exist east of outcrop, with several
flowing wells reported.
LANCE/FOX HILLS AQUIFER
The Lance/Fox Hills aquifer consists of the Upper Cretaceous Lance
Formation and Fox Hills Sandstone, and is comprised of about 1,500 feet
of fine-grained sandstones with occasional interbedded shales and thin
coal layers (Table IV-1). The main exposure of this aquifer is within
the Goshen Hole area, with small outcrop areas present locally along the
50
-------
Table IV-4. Yields of Mesozoic aquifers, Denver-Julesburg basin,
Wyoming.
Yield3
Location Aquifer (gpm)
14/69-5 aa
Pierre
10
14/69-5 da
Pierre
6
14/69-5 bb
Pierre
12
14/69-5 cb
Pierre
8
14/69-31 ab
Pierre
10
16/70-4 dd
Pierre
25
17/69-29 cb
Pierre
4
17/70-24 dd
Pierre
25
17/70-35 dbl
Pierre
10
17/70-35 db2
Pierre
17.5
17/70-35 db3
Pierre
17.5
19/70-3 db
Pierre
5
19/70-31 ca
Chugwater
10
19/70-31 dbl
Chugwater
10
19/70-31 db2
Chugwater
7.5
19/70-31 db3
Chugwater
10
19/70-32 ca
Chugwater
7.5
20/69-23 ad
Chugwater
15
20/69-23 cd
Chugwater
15
20/69-25 be
Chugwater
3
20/69-25 dd
Chugwater
5
20/69-26 cd
Morrison
5
29/68-35 cb
Cloverly
33
35/60-27 ab
Pierre
10
36/61-5 bb
Newcastle
15
36/61-24 be
Cloverly
10
36/62-3 bd
Cloverly
0.2
37/62-1 ab
Cloverly
7
38/61-15 ca
Cloverly
18
aData source: 9 (see Table IV-10).
51
-------
east flank of the Laramie Mountains. Throughout most of the basin the
aquifer lies at depths of 1,000 feet or more. The Lance/Fox Hills
aquifer is isolated from older water-bearing zones by the underlying
Pierre Shale, a thick (+5,000 feet) regional aquitard. Low permeability
claystones and siltstones of the Oligocene White River Group act as the
overlying confining unit (Table IV-1).
The fine-grained sandstones comprising most of the Lance/Fox Hills
are the major water-producing zones within this aquifer. Locally,
interbedded low-permeability shales cause hydrologic isolation of
discrete sandstone beds, forming subaquifers. However, these shales are
generally discontinuous, and the Lance/Fox Hills is regionally
considered as one aquifer.
Hydrologic Properties
Hydrologic data for the Lance/Fox Hills aquifer are available from
wells completed in the Lance Formation in the Goshen Hole Lowland
(Figure II-l) where the formation crops out. No data are available for
the Fox Hills Sandstone within the basin.
No reported permeability or transmissivity data exist for the
Lance/Fox Hills aquifer within the basin. Order of magnitude estimates
of these parameters using specific capacities (Theis and others, 1963)
and thickness of producing zones are given in Table IV-5. Perme-
2
abilities vary from 7.5 to 125 gpd/ft , with transmissivities of 400 to
5,000 gpd/ft. These data are derived from fairly shallow (<300 feet)
stock and domestic wells. Wells penetrating a complete section of the
aquifer would likely have higher transmissivities.
Reported specific capacities for the Lance aquifer vary from less
than 0.1 to 3.0 gpm/ft drawdown. Well yields are generally 25 gpm or
52
-------
Table IV-5.
Hydrologic
properti es
of the Lance
aqui fer,
Denver-Julesburg
basin, Wyoming.
Test
Specific
Well
Duration
Drawdown
Discharge
Capacity
Transmissivity
Storage Permeability3
Coefficient (gpd/ft )
Location
(hours)
(ft)
(gpm)
(Rpm/ft)
(spd/ft)
Remarks
Source
21/62-13 ccl
4
20
3.5
0.17
10
21/62-13 cc2
24
57
15
0.20
450
7.5
Transmissivity
estimated
125
from specific
capacity.
10
22/60-6 ba
48
6
16.7
2.80
5,000
Transmissivity
from specific
estimated
capacity.
22/62-11 da
2
100
7
0.07
19
10
22/62-15 ba
8
218
10
0.05
775
Transmissivity
from specific
estimated
capacity.
10
22/62-17 aa
0.5
2
4
2.0
10
22/64-34 ca
4
29
12
0.41
11. A
10
23/60-20 cd
24
35
10
0.29
400
Transmissivity
estimated
10
16
from specific
capacity.
23/60-21 da
24
15
18
1.20
3,500
Transmissivity
estimated
10
30
from specific
capacity.
23/60-31 bb
18
35
25
0.70
1,300
Transmissivity
from specific
estimated
capac ity.
10
23/60-32 ab
1
15
15
1.0
25
10
23/61-2 ab
48
10
16
1.6
3,200
Transmissivity
from specific
estimated
capacity.
10
23/61-14 cb
8
12
9
0.75
1,500
Transmissivity
from specific
est imated
capacity.
10
23/62-34 cd
T
67
100
1.5
Discharge estimated.
10
25/63-25 bd
7
6.6
31
4.7
10
Permeability from transmissivity estimate + reported thickness of producing; zone(s).
bData sources for hydrologic properties are listed in Table IV-10.
-------
less, but reach 100 gpm locally (Table IV-5). Larger yields are
possible from wells penetrating a greater thickness of the aquifer,
although Rapp and others (1957) state it is doubtful that supplies
adequate for irrigation or large industrial applications could be
obtained from this aquifer.
Ground-Water Circulation
Regional ground-water movement within the Lance/Fox Hills aquifer
is unknown. Downdip flow to the east from near-vertical outcrops along
the Laramie Mountains is likely. Rapp and others (1957) compiled water
data for wells completed in the unconfined Lance sands within a portion
of Goshen Hole. These data indicate ground-water flow toward the North
Platte River. Deeper Lance wells within Goshen Hole produce water under
artesian pressure, indicating that interbedded shales act as confining
zones.
TERTIARY AQUIFER SYSTEM
The Tertiary aquifer system consists primarily of up to 1,500 feet
of permeable sandstones, conglomeratic lenses, and channel deposits.
Included within the system are the Miocene Arikaree and Miocene-Pliocene
Ogallala formations.
The Arikaree Formation consists of up to 1,200 feet of very fine to
fine-grained sandstones with scattered coarse-grained channel deposits,
beds of siltstone, volcanic ash, and, commonly a basal conglomerate
(Morris and Babcock, 1960; Lowry and Crist, 1967). The Arikaree is
present over most of the basin, except uplifted areas along the west and
north margins and within the Goshen Hole Lowland (Figure II-l and
Plate 7).
54
-------
The Ogallala Formation is highly heterogeneous and consists of
lenticular beds and channel fills of semiconsolidated to unconsolidated
sand and gravel with occasional beds of siltstone, clay, and limestone.
The Ogallala Formation is present in Laramie County, with equivalent
rocks found in parts of Platte County. The maximum thickness of the
formation is 330 feet (Lowry and Crist, 1967).
Regionally, the Tertiary aquifer system is isolated from deeper
aquifers by the underlying White River Group, which consists of an upper
and lower member, the Brule and Chadron formations, respectively. The
Brule Formation consists primarily of massive siltstone, and reaches
thicknesses of over 400 feet (Morris and Babcock, 1960). The Chadron
Formation consists of up to 700 feet of claystone, siltstone, and
dispersed sandstone. Low permeability within this sequence is indicated
2
by: (1) Brule Formation primary permeability less than 0.2 gpd/ft
(Rapp and others, 1957), and (2) spring discharge at the contact between
the Brule and Arikaree formations (Rapp and others, 1953; 1957).
Locally, permeable zones exist within the White River Group due to
the presence of coarse-grained channel deposits or, within the Brule
Formation, through secondary permeability development. The origin of
secondary permeability within the Brule Formation has been ascribed to
fractures and fissures, which are prominent features of many Brule
outcrops and penetrate the unit to unknown depths (Rapp and others,
1957; Morris and Babcock, 1960). Lowry (1966) reported that pipes,
tubular openings in semiconsolidated rock, contribute to Brule perme-
ability locally. Crist and Borchert (1972) indicate that where the
Brule is a calcareous siltstone, solution of soluble minerals also
enhances Brule permeability. Where coarse-grained deposits or zones of
55
-------
secondary permeability exist within the White River Group, the unit is
not an effective barrier to ground-water flow, and is considered part of
the Tertiary aquifer system.
Identified as major water-producing zones within this system are
lenses, beds, and channel deposits of coarse-grained sandstones and
conglomerates found within all formational members of the system, and
zones of secondary permeability found primarily in the Brule Formation.
Yields from these zones are adequate for irrigation, municipal, and
industrial water supplies. The massive, fine-grained sandstones of the
Arikaree Formation have generally lower permeabilities but are
sufficiently thick (300-1,000 feet) to yield more than adequate supplies
for stock and domestic use, and locally for municipal and irrigation
demands (Morris and Babcock, 1960; Whitcomb, 1965).
Hydrologic Properties
Hydrologic properties of the Tertiary aquifer system are highly
variable, due to differing lithologies and thicknesses of water
producing zones. Numerous data are available due to the widespread
development of the system as a water source.
Permeability
Permeability data are available for all formational members of the
Tertiary aquifer system. The highest permeability estimates (5,000 to
2
6,000 gpd/ft ) are from zones of secondary permeability within the White
River aquifer (Brule Formation) (Table IV-6) in southwestern Goshen
County (Figure II-l). Crist and Borchert (1972) and Borchert (1976)
investigated Brule secondary permeability in Goshen County and in
southeast Laramie County with a down-hole camera. They described many
56
-------
Table LV-o. Hydrologic properties of the White River aquifer. Tertiary aquifer system, Denver-Julesburg basin, Wyoming.
Test Specific
Well Duration Drawdown Discharge Capacity Transmissivity
Location (hours) (ft) (gpnQ (gpm/f t) (gpd/ft)
Storage
Coefficient
Permeability
(ftpd/ft )
Remarks
Source
12/60-5 baa
7
26.8
685
25.6
12/60-6 ccd
54.3
780
14.4
13/60-5 acb
4.3
1,105
257
13/60-8 bbb
15.1
600
39. 7
13/60-L8 dda
20
750
37.5
13/60-31 aba
31.8
476
15.0
13/62-26 caa
11
400
36.6
13/69-16 ebb
39
130
3.3
14/60-6 dbb
36
732
20.3
14/60-15 dbb
6
500
83.3
14/60-16 dec
14.8
1,400
94.7
14/60-17 deb
42.2
422
10
14/60-28 bbb
11.8
1,465
124.2
14/60-29 bbc
9.8
1,355
138.3
14/60-29 cbd
13
1,200
92.3
14/60-30 beb
8.9
507
57
14/60-32 aba
6
1,000
166.7
14/60-32 dbb
7.5
1,105
147.3
14/61-21 bbb
12
490
40.8
14/61-21 caa
35
600
17.1
14/61-35 abc
15
360
24.0
14/62-11 dbb
20
1,600
80.0
14/62-24 bbb
11.9
805
67.6
15/60-34 bbb
13
585
45.0
15/69-27 ccd
123
450
3.7
19/60-8 abb3
31. 2
375
12
19/60-20 dca
117
1,050
9
19/61-9 cad
11
220
20
19/61-9 dbbl
24
8.5
580
68
19/61-
20/60-
20/61-
20/61-
20/61-
20/61-
20/61-
20/61-
20/61-
11 abc
30 dbb
25 acb
26 aaa
30 dbal
30 dba2
30 dbdl
30 dbd2
36 adb
23. 5
7
15.3
22
21
19. 5
23
18. 7
12
800
920
980
980
250
175
275
225
940
34
131
64
45
12
9
12
12
78
577,000
504,000
627,000
780,000
1 x 10
1 x 10
-4
Discharge estimated.
Pumped well.
5,240 Observation well 50 ft
northwest of pumped well.
6,000 Observation well BOO feet
west of pumped well.
-------
Table IV-6. (continued)
Test Specific
Well Duration Drawdown Discharge Capacity Transmissivity Storage Permeability
Location (hours) (ft) (gpm) (gpm/ft) (gpd/ft) Coefficient (gpd/ft ) Remarks Source3
20/65-8 abb
3
3.6
2.5
0.7
480
16
3
22/67-21 aaa
3
5
3.9
0.8
900
36
3
29/68-9 bed
?
55
10.0
0.2
3
29/69-33 bac
12
7.7
78
10.1
4
34/61-6 ab
?
70
4
0.06
7
34/62-1 ad
?
9.9
4
0.4
7
34/64-9 ac
?
4
6
1.5
7
aData sources for hydrologic properties are listed in Table IV-10.
Ln
CO
-------
tubular or cavernous openings with few fractures. Intergranular
permeabilities from this area are several orders of magnitude lower
(Rapp and others, 1957).
Permeabilities of coarse sand and gravel deposits within the
2
Ogallala aquifer vary from 165 to 4,000 gpd/ft , with the higher values
from very coarse-grained channel fill in northeast Laramie County (Table
IV-7).
2
Arikaree aquifer permeabilities vary from 1 to 375 gpd/ft (Table
IV-8) with higher values from coarse-grained deposits or fractured
2
zones. Whitcomb (1965) considers 65 gpd/ft , obtained from a well
(32/62-17 cb) completed in unfractured, fine-grained Arikaree sandstone,
as a characteristic permeability for the formation. Lines (1976) used
2
permeability estimates of 5 to 50 gpd/ft in construction of a digital
model of the Arikaree in central Platte County.
Transmissivity
Transmissivities from zones of secondary permeability within the
White River aquifer (Brule Formation) in southeast Goshen County vary
from 500,000 to over 780,000 gpd/ft'(Table IV-6). Two other available
Brule transmissivities are less than 1,000 gpd/ft. These values,
although several orders of magnitude lower than transmissivities
reported from Goshen County, are enhanced by fractures within the Brule
(Morris and Babcock, 1960).
The highest reported Ogallala transmissivity (700,000 gpd/ft) is
from a very thick coarse-grained channel deposit in northeast Laramie
County (Table IV-7). Borchert (1976) considers this value anomolously
high, but reports that transmissivities of over 100,000 gpd/ft are
likely in most channel fills thicker than 100 feet. Ogallala
59
-------
Table IV-7. Hydrologic properties of the Ogallala aquifer, Tertiary aquifer system, Denver-Julesburg basin, Wyoming.
Test
Specific
Well
Durat ion
Drawdown
Discharge
Capacity
Transmissivity
Storage
Permeability
Loca tion
(hours)
(ft)
(spin)
(spm/ft)
(gpd/ft)
Coefficient
(fipd/ft )
Remarks
Sour
13/64-23
aaa
7
7
350
50
Discharge reported.
2
13/64-23
daa
7
220
31
Discharge reported.
2
13/66-18
aca
308
80
0.26
2
13/67-15
cdd
140
42
0.3
Discharge reported.
2
13/67-16
bca
32
110
3.4
2
13/67-16
bcc
50
130
2.6
2
13/67-16
ebb
50
74
1.5
2
13/67-17
add
49
108
2.2
2
13/67-17
uaa
28
84
3
2
13/67-17
dab
20
52
2.6
2
13/67-17
dba
45
128
2.8
2
13/68-14
bbb
31,700
2
13/68-14
cba
23,392
2
14/67-7 ccb
7
5,580
2
14/67-18
cbd
46
46
6
4.7
6,900
13,600
5.6 x 10"4
575
Observation well 1,700
west of pumped weLl.
ft
2
2
14/67-18
ddc
12
12
1.5
4,300
16,400
1.8 x 10~A
Observation well 1,320
west of pumped well.
ft
2
2
14/67-19
bbd
27
1.5
3,000
2
14/67-24
acb
7
1,670
2
14/68-13
acb
73
15.3
23,000
2
14/68-13
ccd
25
13.5
27,000
358
2
14/68-13
dad
45
2.9
10,800
2
14/68-14
ded
24
24
19,200
31,000
5.9 x 10~5
581
Observation well 2,140
north of pumped well.
ft
2
2
14/68-23
ddc
?
4,750
2
14/68-24
bdd
46
5.5
'6,200
2
14/68-25
bed
7
16,750
476
2
14/68-26
bdd
7
1,065
2
14/68-26
cbc
168
168
5.2
26,400
28,200
3.11 x lO-4
Observation well 1,320
west of pumped well.
ft
2
2
14/68-27
dec
7
17,000
762
2
14/68-33
bcc
?
34,300
390
2
14/68-34
aab
7
16,400
2
14/68-35
cac
7
12,300
_A
164
2
14/68-36
aac
4
15,000
1.4 x 10
Observation well 2,000
west of pumped well.
ft
2
15/67-2 dba
232
39,200
_
2
15/67-16
bca
56
0.3
1,835
6.7 x 10
Observation well 835 ft
west of pumped well.
2
-------
Table JV-7. (continued)
Well
Location
Test
Duration
(hours)
Drawdown
(ft)
Discharge
(Rpm)
Speci f ic
Capacity
(gpm/ft)
Transmissivity
(gpd/ft)
Storage Permeability
Coefficient (gpd/ft )
Remarks
Source
15/67-16 bca
56
1,730
4.9 x 10~5
Observation well 1,981 ft
2
_ s
southeast of pumped well.
56
1,870
3.2 x 10
Observation well 1,200 ft
2
southwest of pumped well.
15/67-34 ccc
?
15
15
1.0
Discharge reported.
2
16/60-3 bad
34
1,835
54
5
16/60-9 abd
7
675
96
5
16/60-10 bcc
11.8
600
51
Discharge estimated.
5
16/60-10 dda
11.8
900
76
5
16/60-27 abc
77.8
700
9
5
16/61-2 dec
7.2
730
101
5
16/61-3 bdd
7
1,100
157
5
16/61-7 edd
56
1,180
21
5
16/61-9 abd
27.9
920
33
5
16/61-10 dbd
118.9
830
7
5
16/61-17 cba
11
1,600
145
5
17/60-28 ccc
9.4
1,150
122
5
17/60-29 cbd
14
700
50
Discharge estimated.
5
17/60-29 dca
11.5
750
65
Discharge estimated.
5
17/60-33 bcc
4.8
1,100
229
Discharge estimated
5
17/60-33 dbb
24
6
850
142
708,000
4,000
5
17/60-34 cac
8
1,100
138
5
3Data sources for hydrologic properties are listed in Table IV-10.
-------
transmissivities within the Cheyenne municipal well field vary from
1,650 to 39,200 gpd/ft. The heterogeneous nature of the Ogallala
results in the wide range of reported values, with higher trans-
missivities related to wells penetrating thick lenses of gravel and
coarse sand. Lowry and Crist (1967) calculated an average transmis-
sivity of 3,800 gpd/ft for the Ogallala in the Cheyenne vicinity, and
considered this value representative for the aquifer.
Arikaree aquifer transmissivities vary from 61 to 77,000 gpd/ft
(Table IV-8). Wells penetrating fractured zones, coarse sandstone beds,
or large aquifer thicknesses yield the highest transmissivities.
Results of regional transmissivity analyses (Weeks, 1964), calibrated
estimates used in digital models (Lines, 1976), and data from wells
completed outside of coarse deposits or fracture zones (Weeks, 1964;
Whitcomb, 1965) indicate characteristics Arikaree transmissivities of
10,000 to 30,000 gpd/ft.
Specific Capacity and Well Yields
Specific capacities show a wide range of values, from 0.06 to 275
gpm/ft (Tables IV-6, 7, and 8). Most available specific capacity data
have no test duration reported, making comparison of individual values
difficult.
Specific capacities from wells completed in the White River aquifer
range from 0.06 to 257 gpm/ft and are generally greater than 20 gpm/ft
(Table IV-6). Most reported values are from high yield (>300 gpm) Brule
aquifer wells located in eastern Laramie and southeastern Goshen
counties. Many of the wells withdrawing water from the Brule in this
area, particularly in the Pine Bluffs Lowland (Figure II-l) , may
actually be completed in alluvium derived from the Brule (Lowry and
62
-------
Table IV-8. Hydrologic properties of the Arikaree aquifer, Tertiary aquifer system, Denver-Julesburg basin, Wyoming.
Test
Specific
Well
Duration
Drawdown
Di scharge
Capacity
Transraissi"ity
Storage
Permeability
Location
(hours)
(ft)
(gpm)
(gpm/ft)
(gpd/ft)
Coefficient
(RPd/ft )
Remarks
Source3
15/61-4 deb
27
900
33.3
2
15/61-9 bbb
50
200
4.0
2
16/61-4 cca
114
800
7
5
16/61-15 dda
28.9
1,100
38
Discharge estimated.
5
16/63-26 ddd
35
840
24
Discharge estimated.
5
17/60-19 caa
171
685
4
5
17/62-25 cbd
208
830
4
5
17/62-31 acc
48
88
530
6
9,300
Pumped well.
5
48
NR
"
"
9,225
Observation well 41 ft
south of pumped well.
5
48
NR
— —
21,725
Observation well 156 ft
east of pumped well.
5
17/63-26 dba
43.5
1,000
23
5
18/60-34 dbd
96.7
580
6
5
22/66-12 ddd
5
4.6
1.4
0.3
3
23/68-4 abc
1,000
1,000
178
480
2.7
9,800
3 x 10"3
-L
Pumped well.
Observation well 100 ft
east of pumped well.
3
6
1,000
—
—
—
6,200
6x10
Observation well 200 ft
6
5 x 10"5
_ R
east of pumped well.
1,000
—
4,000
Observation well 300 ft
east of pumped well.
b
1,000
—
9,800
5 x 10
Observation well 1,600 ft
east of pumped well.
6
23/68-4 acc
130
128
575
4.5
6
23/68-10 ede
1
56
250
4.5
b
23/68-27 baa
0.5
35
60
1.7
b
24/66-20 cbc
1
0.33
2.0
6
15,000
375
3
24/66-22 ddd
5
4.6
1.4
0.3
110
1.3
3
24/67-4 acc
NR
21.7
90
4.1
3
24/67-5 acc
140
130
475
3.6
3,200
-A
Puraped well.
h
140
NR
—
—
3,200
5 x 10
-L
Observation well 400 ft
east of pumped well.
6
140
NR
—
—
2,600
5 x 10
Observation well 800 ft
east of pumped well.
6
24/67-6 bed
120
120
98
350
3.6
4,000
3,700
-A
3 x 10
Pumped well.
Observation well 597 ft
east of pumped well .
6
6
24/67-7 add
1
650
10,000
1.6 x 10
Observation wc1J 660 ft
west of pumped well .
6
24/68-12 dbbl
100
220
2.2
6
24/68-12 dbb2
100
560
5.6
A
6
24/68-12 dbc
46
81.7
600
7.3
9,400
7.5 x 10
19
6
24/68-12 deb
180
1,030
5.7
6
24/68-17 abc
700
120
460
3.8
6
24/68-22 acc
30
80
550
6.9
6
24/08-27 acc
73
44
900
20.5
6
-------
Table IV-8.
(continued)
Test
Specific
Well
Duration
Drawdown
Discharge
Capacity
Transmissi"ity
Storage
Permeability
(gpd/ft )
Location
(hours)
(ft)
(Rpm)
(gpm/ft)
(gpd/ft)
Coefficient
Remarks
c. a
Source
24/68-34 bcc
43,000
2.5 x 103
Observation well
north of pumped
800 ft
well.
6
25/67-31 dec
210
98
415
4.2
6
25/68-31 edd
144
105
505
4.8
8,000
6
25/68-35 dbc
5
101
600
5.9
6
25/68-36 beb
8
106
670
6.3
6
25/68-36 ccc
5
124
550
4.4
6
26/65-17 bdd
15
38
6.2
0.2
140
3.1
3
30/66-24 baa
5
10.8
2.2
0.2
61
_ O
1.6
3
32/62-17 cd
96
47.4
730
15
32,000
1.5 x 10 ,
64
7
32/63-2 cc
115
10.4
370
36
77,000
2 x 10 J
310
7
32/63-33 bb
16
20.2
160
8
8,000
30
7
32/64-24 da
72
2.8
650
230
7
34/62-29 cd
17
30
195
6
10,000
100
7
aData source for hydrologlc properties are listed in Table IV-10.
-------
Crist, 1967). Well yields of several hundred to over 1,000 gpm are
common for the Brule where secondary permeability is developed.
Reported specific capacities of less than 2.0 gpm/ft and yields of under
25 gpm are characteristic of the unit where secondary permeability is
poorly developed.
Specific capacities for wells completed in the Ogallala aquifer
vary from less than 1 to 229 gpm/ft (Table IV-7). Very high specific
capacities are limited to wells completed in coarse, relatively thick
channel deposits (Borchert, 1976). Away from these channel fills,
specific capacities range from less than 1 to 50 gpm/ft. The large
range in Ogallala specific capacities reflects the extreme heterogeneity
of the aquifer.
Specific capacities for wells completed in the Arikaree aquifer are
generally less than 40 gpm/ft (Table IV-8). One anomalously high value,
230 gpm/ft, is reported for a well (32/64-24 da) completed in a fracture
zone. Weeks (1964) and Whitcomb (1965) suggest values of at least 5
gpm/ft are typical for the Arikaree, with wells penetrating a large
thickness of the aquifer likely to yield values up to 30 gpm/ft.
Ground-Water Circulation
A water table map within the Tertiary aquifer system is given in
Figure IV-2. Regionally, ground-water movement is away from uplifts
along the west and north edges of the basin. In the northern two-
thirds of the area, a significant component of flow is directed toward
Goshen Hole and the North Platte River Valley. Locally, smaller
drainages have similar effects and flow is from topographic highs toward
gaining reaches of streams (Welder and Weeks, 1965). Depth to water
65
-------
EXPLANATION
¦5000 Water table contour; contour
interval 200 feet
Limit of Tertiary outcrop
Water table map of the Tertiary aquifer system, Denver-
Julesburg basin, Wyoming (from Gutentag and Weeks, 1980)
66
-------
varies from several hundred feet along major interstream divides to near
zero along major stream valleys.
Through much of the basin the water table slopes at 40 feet/mile to
140 feet/mile (Lowry and Crist, 1967; Rapp and others, 1957). Where the
water table is within low-permeability zones of the White River Group,
gradients may reach 400 feet/mile. The Tertiary aquifer system is
generally unconfined throughout most of the basin, but confined or
semiconfined conditions exist locally in all member aquifers (Weeks,
1964; Lowry and Crist, 1967; Lines, 1976).
Recharge
No regional estimate of recharge to the Tertiary aquifer system has
been published for the entire basin. Within the basin, this system is
exposed over 8,190 square miles (Gutentag and Weeks, 1980). Assuming an
average precipitation of 15 inches/year with 5 percent of the
precipitation available as recharge (Rapp and others, 1953; Morris and
Babcock, 1960), direct infiltration of precipitation supplies roughly
325,000 acre-feet/year to the Tertiary aquifer system. Recharge from
applied irrigation water and seepage from irrigation canals is very
important locally, but has not been quantified (Rapp and others, 1957).
Leakage from streams, especially near the Laramie Mountains, also
recharges the system (Lowry and Crist, 1967). Bjorklund (1959) suggests
local upwelling from pre-Tertiary strata occurs where the White River
Group has well-developed secondary permeability.
Discharge
Discharge from the Tertiary aquifer system occurs by several
processes, including well pumpage, leakage to gaining streams and
67
-------
Quaternary aquifers, underflow into adjacent states, and through
numerous springs and seeps. The regional magnitude of differing
discharge mechanisms is unknown, though local estimates have been made.
Morris and Babcock (1960) estimated Tertiary discharge of roughly
28,000 acre-feet/year to the 40-mile reach of the North Platte River in
the northwest part of the basin. Tertiary discharge into Quaternary
aquifers is unknown. Underflow to adjacent states likely accounts for
large discharges of Arikaree waters. Underflow across the Niobrara
County-Nebraska boundary was estimated at 5,600 to 8,960 acre-feet/year
by Babcock and Keech (1957). Discharge by contact springs occurs along
the escarpments bounding the Goshen Hole and Pine Bluffs lowlands, where
the White River is overlain by the generally more permeable Ogallala
and/or Arikaree aquifers (Rapp and others, 1953, 1957). A line of
springs discharging from the Ogallala lies in western Laramie County,
and was considered by Morgan (1946) to mark the eastern edge of a thick,
highly permeable zone. This spring line has migrated east over the past
several decades, in apparent response to pumping at the Cheyenne
municipal well field (Lowry and Crist, 1967).
QUATERNARY AQUIFERS
Quaternary age flood plain and terrace deposits are found in
numerous parts of the basin. Thick, extensive deposits are generally
limited to several distinct areas: (1) adjacent to the North Platte
River and its major tributaries, (2) the Wheatland Flats, and (3) the
Pine Bluffs Lowland and adjacent areas (Figure II-l). Quaternary
deposits consist of lenticular beds of fine to very coarse sand, gravel,
silts, and clay with occasional cobbles and boulders (Lowry and Crist,
1967). Thickness of Quaternary deposits is variable, reaching maxima of
68
-------
200 feet in the North Platte River Valley (Rapp and others, 1957), 85
feet in Wheatland Flats (Morris and Babcock, 1960), and 120 feet in the
Pine Bluffs area (Rapp and others, 1953). Alluvium underlying the
valleys of smaller drainages, except along their extreme lower reaches,
is generally less than 50 feet thick.
Hydrologic Properties
Extensive data are available on the hydrologic properties of
Quaternary aquifers, due to the generally excellent water-producing
capabilities of terrace and flood plain aquifers.
Permeability
Reported permeabilities for Quaternary aquifers vary from 700 to
2
9,600 gpd/ft (Table IV-9). This range in permeability is due to
differing grain sizes and degrees of sorting in Quaternary deposits.
Quaternary aquifers adjacent to the North Platte River have the highest
2
permeabilities, generally exceeding 4,000 gpd/ft . Within Wheatland
2
Flats, permeabilities vary from 500 to 5,600 gpd/ft , usually exceeding
2
2,500 gpd/ft . Two reported permeabilities from the Pine Bluffs Lowland
2
(Figure II-l) indicate a range of about 700 to 3,000 gpd/ft .
Transmissivity
Reported Quaternary aquifer transmissivities range from 6,500 to
1,650,000 gpd/ft (Table IV-9). Transmissivities greater than 150,000
gpd/ft are limited to areas adjacent to the North Platte River and its
major tributaries, particularly the reaches of these drainages that lie
within the Goshen Hole Lowland. Extensive areas within the Lowland are
underlain by greater than 100 feet of coarse-grained, saturated
Quaternary gravels (Crist, 1975). Reported transmissivities are
69
-------
Table IV-9. Hydrologic properties of Quaternary aquifers, Denver-Julesburg basin, Wyoming.
Well
Location
Test
Duration
(hours)
Drawdown
(ft)
Discharge
(RPm)
Specific
Capacity
(gpm/ft)
Transmissivity
(gpd/f t)
Storage Fermeabi
Coefficient (ppd/ft
lity
>
Remarks
Sour
12/62-2 bcb
97.25
58.0
105,000
, 3,180
Pumped well.
2
97.25
146,000
5.43 x 10
Observation well 745
ft
2
west of pumped well.
12/62-3 bcc
7.5
37.4
53,300
2
12/62- 22 abb
84.25
13.9
59,000
694
Pumped well.
2
84.25
44,800
4.65'x 10
Observation well 305
ft
2
east of pumping well
13/61-11 aca
?
21
700
33.3
Discharge reported.
2
14/69-3 ebb
5
40
8
Discharge reported.
2
19/61-4 bca
15
120
8
5
19/61-4 cbal
25
430
17
5
19/61-4 cddl
16.7
600
36
5
19/61-4 cdd3
15
380
25
5
19/61-4 cdd4
30
231,000
Pumped well.
5
30
258,000
4.7 x 10 J
Observation well 158
ft
5
_2
west of pumped well.
30
376,000
1.9 x 10
Observation well 288
ft
5
west of pumped well.
20/61-32 cac
?
11
650
59
5
20/61-32 cadi
10
460
46
5
20/61-32 cad3
14.6
410
28
5
20/61-32 cad4
10
250
25
5
20/61-33 cba
22
840
38
5
20/61-33 cbd
19.5
800
41
5
20/61-33 cddl
27
780
29
5
20/61-33 cdd2
1.5
129,000
5
20/61-33 dec
24
28
0.9
5
20/67-3 ebb
17
100
5.9
Discharge reported.
3
20/67-9 cc
7.5
90
12
Discharge reported.
3
20/67-19 bbb
15
50
3.3
Discharge reported.
3
20/68-25 bbb
16
40
2.5
Discharge reported.
3
20/68-34 baa
10
50
5
Discharge reported.
3
22/64-21 aa
29
275
9.5
1
23/60-10 aa
24
370
15.4
1
23/60-10 bb
10
180
18
1
23/60-15 ba
11.8
910
79.7
1
23/68-1 ccd
3
44
80,000
4,000
6
24/61-2 cb
12
9.1
1
,040
114
335,000
5,900
1
24/61-5 cbl
25
6.1
1
,060
174
614,000
0.235 3,800
1
24/61-10 bd
7
11
1
,000
91
1
24/61-10 cdl
9
7.6
900
119
250,000
1,500
1
24/61-10 cbl
?
9
650
?2
1
24/61-15 eel
37
18.3
3
,400
186
1,650,000
0.235 8,700
1
24/61-23 ac
7
7.2
580
80.1
1
24/61-23 ad
?
8.2
740
90
1
24/63-3 bcb
?
18.1
130
7.2
1
-------
Table IV-9. (continued)
Test
Specific
Well
Duration
Drawdown
Discharge
Capacity
Transmissivity
Storage
Permeability
(Rpd/ft )
Source'1
Location
(hours)
(ft)
(SPin)
(Rpm/ft)
(spd/ft)
Coefficient
Remarks
24/63-3 bcc
?
10.7
200
19
1
24/63-4 cbc
18
230
13
1
24/63-5 acb
11.3
320
28
1
24/63-16 ccd
14.5
460
32
1
24/63-18 acc
9.1
270
30
1
24/63-18 acd
2.5
380
150
1
24/67-6 bcdl
170
17
22,000
1,000
6
24/68-2 dec
354
34
45,000
2,400
6
24/68-3 beb
10
7
9,000
500
6
24/68-4 cbc
50
13
20,000
1,400
6
24/68-7 dec
5
8
13,000
1,200
6
24/68-9 ccc2
24
15
22,000
2,500
6
24/68-llcbc
8
10
17,000
700
6
24/68-11 ccc
7
39
70,000
2,600
6
24/68-15 acb
?
28
45,000
4,000
6
24/68-16 edd
24
14.5
460
32
67,000
2,700
3
24/68-18 acc
6
9.1
270
30
8,700
2,600
3
24/68-20 ccdl
40
40
72,000
5,600
24/68-33 cdd2
22
22
36,000
3,600
25/61-12 bd
3
9.8
1,590
162
2 7,000
4,200
I
25/61-27 cb
?
28
800
29
1
25/61-28 be
5.2
560
96
1
25/61-28 cc
8
920
115
1
25/61-28 db
15
290
19
1
25/61-29 da
6.1
860
111.5
1
25/61-31 db
?
8.8
40
4.6
1
25/61-33 ab
24
9.3
1,210
130
310,000
0.216
2,300
1
25/61-33 bb
?
8
1,000
125
1
25/61-33 db
47
1,000
21.2
1
25/61-34 bb
14
1,160
83
1
25/61-35 bb
11
1,200
109
1
25/62-18 ca
7
1,040
149
1
25/63-12 bd
3
9.8
1,590
160
270,000
1
25/67-31 ccc2
3
5.2
250
48
120,000
25/67-18 db2
4
1,000
250
1
25/67-18 db3
4
1,000
250
J
25/68-36 ccc
1
14.7
160
11
26/65-9 cc
0.6
6.3
1,050
170
27/66-35 dba
6
330
55
3
28/68-27 abc
1
5.3
66
12
6,500
1,000
3
29/68-21 bcc
3
5.3
770
145
240,000
9,600
3
30/68-17 ebb
0.5
12.2
940
77
3
30/68-18 aac
240
17.5
430
25
90,000
3,000
3
aData sources for hydrologic properties are listed in Table IV-10.
-------
Table IV-10.
Data sources for hydrologic properties.
1
Rapp and others, 1957
2
Crist and Lowry, 1967
3
Morris and Babcock, 1960
4
Welder and Weeks, 1965
5
Borchert, 1976
6
Weeks, 1964
7
Whitcomb, 1965
8
Rapp and others, 1953
9
Wyoming State Engineer's Office, Information Files,
1981
10
Dana, 1962
11
Wyoming Geological Survey, Information Files, 1981
72
-------
generally 10,000 to 70,000 gpd/ft in Wheatland Flats and 50,000 to
150,000 gpd/ft in the Pine Bluffs area.
Specific Capacities and Well Yields
Specific capacities of wells completed in Quaternary aquifers vary
from 3.3 to 250 gpm/ft (Table IV-9), and commonly exceed 50 gpm/ft.
Wells developed in Quaternary aquifers commonly yield 500 gpm,
often to large diameter (>10-inch) irrigation wells. Locally, yields of
over 3,000 gpm are reported.
Ground-Water Circulation
Ground-water movement within Quaternary aquifers generally follows
the downstream flow of adjacent drainages in flood plain aquifers, and
is toward drainages in terrace aquifers (Crist, 1975). Recharge to the
Quaternary aquifers takes place through direct infiltration of
precipitation and excess irrigation water, and from influent stream and
canal seepage. Locally, water from the underlying bedrock units
recharges Quaternary deposits (Welder and Weeks, 1965), though Crist
(1975) considers this mechanism insignificant in the thick deposits
adjacent to the North Platte River. Ground water discharges from
Quaternary deposits into streams at low flow, and to contact springs
where terrace deposits overlie less permeable bedrock. Underflow across
the Wyoming-Nebraska state line also is significant, especially adjacent
to the North Platte Valley. Crist (1975) estimates underflow at about
17,000 acre-feet/year in this area.
Water table conditions exist throughout the Quaternary aquifers.
Depth to water varies from a few feet to generally less than 50 feet in
flood plain deposits. The water table is usually deeper in terrace
73
-------
deposits, but is rarely over 100 feet below the surface (Rapp and
others, 1953, 1957). Near streams, where the water table lies close to
the surface, evapotranspiration is a significant discharge mechanism
(Morris and Babcock, 1960).
74
-------
V. WATER QUALITY
-------
V. WATER QUALITY
Approximately 800 water quality analyses were reviewed for this
report. Data sources include: the Wyoming Water Resources Research
Institute (WRRI) data system (WRDS), the U.S. Geological Survey WATSTORE
data system, a compilation of water quality analyses by the U.S.
Geological Survey (1971), analyses by Stock (1981) , and a compilation of
oil field water analyses by Crawford and Davis (1962). All analyses
used are published or available elsewhere and therefore are not
tabulated in this report.
In general, data availablility and spatial distribution for deeper
aquifers (below the Pierre Shale) are poor. While numerous analyses are
reported for aquifers above the Pierre Shale, most are for relatively
shallow wells.
The first part of this chapter discusses the general water quality
(dissolved solids content and major ion composition) of principal
aquifers within the basin. Total dissolved solids concentrations for
these aquifers are shown on Plates 3 through 8. The second part of the
chapter addresses water quality related to U.S. Environmental Protection
Agency drinking water standards.
GENERAL WATER QUALITY
Paleozoic Aquifer System
Most water quality data for the Paleozoic aquifer system are
analyses of water from shallow wells completed in the Hartville aquifer.
Few wells have been drilled into other aquifers of the system, or into
76
-------
the Hartville in the central basin. Therefore, basinwide trends of
water quality cannot be identified.
Wells in and near outcrops of the Hartville aquifer produce water
with less than 500 mg/1 total dissolved solids (Plate 3). These waters
predominantly contain dissolved calcium-magnesium-bicarbonate (Figure
V-l). A sample of Hartville water away from outcrop, taken from a depth
of about 2,300 feet in central Goshen County (28/63-32), contained
sodium sulfate rich water, with 2,897 mg/1 TDS.
Samples from the Madison Limestone (Guernsey Limestone equivalent)
at Old Woman anticline (36/62-28) are mixed-anion waters with TDS con-
centrations between 500 and 600 mg/1.
Precambrian rocks underlying the aquifer system yield water with
less than 500 mg/1 TDS to shallow wells in outcrop areas near the
western basin boundary (Plate 3). Chemical constituents cannot be
characterized because only partial analyses are available.
Mesozoic Aquifers
In the Glendo area, a Goose Egg Formation test well (29/69-24;
Welder and Weeks, 1965) produced calcium or sodium sulfate rich waters
with 615 to 2,550 mg/1 TDS. TDS and calcium concentrations decreased as
tested well depth increased, reflecting dilution of calcium-sulfate rich
water produced in the shallow-most, gypsiferous strata.
Water from the Cloverly aquifer generally contains under 3,000 mg/1
TDS based on available analyses (Plate A). However, data from the
central basin are not available. Wells near outcrops tend to have less
than 1,000 mg/1 TDS, while wells away from outcrop recharge areas
produce more saline water. Dilute (<500 mg/1 TDS) waters from the
aquifer typically are sodium bicarbonate rich, whereas more saline
77
-------
Aquifer
Total Dissolved Solids
(mg/1)
Figure V-l. Major ion compositions of representative waters of the Paleozoic
aquifer system, Denver-Julesburg basin, Wyoming.
78
-------
waters are sodium sulfate enriched (Figure V-2). The dominance of
sodium is due to cation exchange reactions. Northeast of the Old Woman
anticline and immediately outside the basin boundary, sodium bicarbonate
waters with over 1,000 mg/1 TDS are typical, with the dominance of
bicarbonate caused by reduction of sulfate (Stock, 1981).
Total dissolved solids concentrations of Newcastle aquifer waters
range from 860 to 22,918 mg/1, but geographic distribution of reported
analyses is poor (Plate 4). Two wells near Newcastle outcrops on the
Old Woman anticline have water with 890 and 2,900 mg/1 TDS. The
remainder of the analyses are from the vicinity of the Borie and Horse
Creek oil fields (Plate 1) and range from 15,113 to 22,918 mg/1 in TDS.
Shallow, relatively dilute (<3,000 mg/1 TDS) waters have mixed ion
composition, whereas sodium chloride is dominant in water from deeper
oil field wells.
Poor water quality within the Newcastle and Cloverly aquifers is
caused by leakage from surrounding confining beds and dissolution of
soluble salts from the aquifer matrix. Sandstone units within the
Newcastle and upper Cloverly are lenticular and often contain siltstone
or shale, restricting ground-water circulation and producing high TDS
water. Oil field waters are examples for this restricted circulation.
Lance/Fox Hills Aquifer
There are few recorded analyses of Lance/Fox Hills aquifer water,
and most are for Lance waters from outcrop areas in Goshen Hole.
Reported total dissolved solids concentrations range from 231 to
4,076 mg/1 (Plate 5). TDS concentrations less than 500 mg/1 are present
in Laramie County, while within Goshen Hole the outcrop area west of
79
-------
Total Dissolved Solids
Aquifer (mg/1)
Figure V-2. Major ion composition of representative waters from Mesozoic
aquifers, Denver-Julesburg basin, Wyoming.
80
-------
Hawk Springs (T. 21 N., R. 62 W.) produces water with over 1,000 mg/1
TDS. Elsewhere TDS values are between 500 and 1,000 mg/1.
Dilute (<500 mg/1 TDS) Lance aquifer waters are calcium bicarbonate
to sodium bicarbonate in composition, whereas more concentrated waters
typically are enriched in sodium bicarbonate (Figure V-3). Rapp and
others (1957) attribute the dominance of sodium to natural softening by
ion exchange with clays within the Lance aquifer. They also indicate
that sulfate reduction accounts for the dominance of bicarbonate over
sulfate.
Increases in TDS and ion composition changes from calcium to sodium
dominated water from the southern part of the basin to Goshen Hole
indicate ground-water discharge west of Hawk Springs. The lack of
potentiometric data for the Lance/Fox Hills prevents verification of
this geochemically based conclusion.
Tertiary Aquifer System
The Tertiary aquifer system generally produces good quality calcium
bicarbonate rich water with less than 500 mg/1 total dissolved solids.
Poorer water quality (500-1,000 mg/1 TDS) with increased sodium content
is primarily limited to the White River aquifer in the Goshen Hole area,
which is a regional discharge zone for the Tertiary aquifer system (see
Figure IV-2).
White River aquifer water quality is discussed separately from
other member aquifers of the Tertiary aquifer system because
intra-aquifer chemical differences are present. There are no apparent
differences in quality of water derived from the Arikaree and Ogallala
aquifers of the Tertiary aquifer system; consequently they are grouped
for this discussion.
81
-------
F indicates water from Fox Hills
Sandstone
Total Dissolved Solids
(mg/1)
0-500
500-1,000
>1,000
points
Figure V-3. Major ion composition of representative waters from the Lance/
Fox Hills aquifer, Denver-Julesburg basin, Wyoming.
82
-------
to a greater degree than the fine-grained sandstones comprising the bulk
of these aquifers. Therefore, the channel deposits are likely sources
of lower TDS ground water.
There is no apparent regional trend in Arikaree and Ogallala water
composition. The absence of an identifiable downgradient trend in water
composition is atypical for Wyoming Tertiary aquifers. The relatively
higher precipitation rate (recharge) for this basin and more permeable
Tertiary sandstones producing more rapid circulation of ground water,
result in better water quality relative to other parts of the state.
Quaternary Aquifers
Waters from Quaternary terrace and alluvial aquifers range from 228
to 1,410 mg/1 TDS (Plate 8), and most values exceeding 500 mg/1 are from
central Platte and Goshen counties. In Laramie County and southern
Goshen County most waters are calcium-bicarbonate in composition,
whereas in the higher TDS waters from Platte and Goshen counties, sodium
and sulfate are also significant constituents (Figure V-6).
In Laramie County and southern Goshen County, Quaternary aquifer
water composition is similar to that of water in underlying Tertiary
aquifers (compare Plates 6, 7, and 8 and Figures V-4, V-5, and V-6).
This is due to either good communication between these aquifers or
lithologic similarity of Quaternary and Tertiary deposits. In central
Platte and Goshen counties there is little similarity between Quaternary
and Tertiary aquifer system waters. In central Platte County, water
movement is downward from Quaternary aquifers to the Arikaree (Weeks,
1965), whereas in Goshen County, discharge from bedrock aquifers to the
alluvial aquifer is considered insignificant compared to other recharge
mechanisms (Crist, 1975).
83
-------
Total Dissolved Solids
(mg/1)
0-500
500-1,000
>1,000
Figure V-4. Major ion composition of representative waters of the White River
aquifer, Tertiary aquifer system, Denver-Julesburg basin,
Wyoming.
84
-------
Aquifer
O OgalLala
Arikaree
Total Dissolved Solids
(mg/1)
0-500
A >500
Figure V-5. Major ion composition of representative waters of the Arikaree
and Ogallala aquifers, Tertiary aquifer system, Denver-Julesburg
basin, Wyoming.
85
-------
OA
Aquifer
Alluvial
Total Dissolved Solids
(mg/1)
O® 0-500
500-1,000
>1,000
Figure V-6. Major ion composition of representative waters of the Quaternary
aquifers, Denver-Julesburg basin, Wyoming. Dashed field repre-
sents typical composition of aquifer water in Laramie County.
86
-------
White River Aquifer
White River aquifer TDS concentrations range from 168 to 1,410 mg/1
within the Denver-Julesburg basin (Plate 6). Most reported values
greater than 500 mg/1 occur in waters from the Chadron Formation in the
Goshen Hole Lowland. This area is a regional discharge point for
Tertiary ground-water circulation (Figure IV-2).
Waters from the White River aquifer range from calcium to sodium
bicarbonate in composition (Figure V-4). Waters with more than 500 mg/1
TDS tend to be sodium enriched.
White River water from Laramie County is compositionally similar to
other Tertiary aquifers (see below), whereas waters from Goshen County
range from typical Tertiary aquifer composition to typical Lance/Fox
Hills composition (compare Figures V-3, V-4, and V-5). This water
quality variation is a result of downgradient changes in White River
water or interaquifer mixing of waters in the Goshen Hole discharge
zone.
Arikaree and Ogallala Aquifers
The Arikaree and Ogallala aquifers in the Denver-Julesburg basin
generally contain water with less than 500 mg/1 TDS (Plate 7). Calcium
bicarbonate is the dominant ion composition (Figure V-5).
Total dissolved solids vary on a local basis. In the Cheyenne
vicinity, TDS concentrations range from 150 to 2,012 mg/1, with no clear
relationship to either well depth or location. Local differences in TDS
may be related to the variable lithologies present in these aquifers.
Where present, coarse-grained channel deposits allow for rapid
transmission of ground water and are likely leached of soluble minerals
87
-------
In Platte and Goshen counties , there is significant recharge to
Quaternary aquifers from streams and irrigation canals (Rapp and others,
1957; Morris and Babcock, 1960; Crist, 1975). Increased sodium and
sulfate concentrations in these areas reflect the composition of surface
water in the North Platte and Laramie rivers.
Lowry and Crist (1967) report TDS changes with time in Quaternary
aquifer water from one well near Pine Bluffs (14/60-11 bcc). TDS
concentration increased from 302 mg/1 in 1947 to 486 mg/1 in 1964. They
consider this increase to be due to irrigation. Few wells have multiple
analyses reported; therefore this trend of increasing TDS cannot be
confirmed.
DRINKING WATER STANDARDS
Primary Standards
Within the Denver-Julesburg basin relatively large amounts of
analytical data are available for fluoride and nitrate concentrations in
ground water. Few data are available for the remaining eight inorganic
species for which primary drinking water standards have been
established, and there are no reported exceedences of the standards for
these species.
Fluoride
Fluoride concentrations exceed 2.0 mg/1 in water samples from
several wells completed in the Lance/Fox Hills aquifer in Goshen County,
and in water from two wells (36/62—28) completed in the Madison
Limestone (Guernsey Limestone equivalent) of the Paleozoic aquifer
system. The distribution of reported fluoride concentrations exceeding
2.0 mg/1 is shown in Figure V-7. There are no reported analyses with
88
-------
0 622.
9 7r7 V48.
75. @S3-4
079.
2.4,2.2®
051.
B24
¦2". 5^2.8"
O?o.
66.A^^i-(14)A49-150-
48.Z&80.
£61.
68. £
EXPLANATION
Flouride
gj Lance/Fox Hills aquifer
X Paleozoic aquifer system
(Madison Limestone)
Nitrate
O Quaternary aquifers
A Arikoree S Ogallala aquifers ) Tertiary
V White River aquifer ) ^qu'fer
v M ' System
Q Precambrian rocks
£\4I number indicates concentration in mg/l
Figure V-7. Locations of high fluoride and nitrate levels in ground
water, Denver-Julesburg basin, Wyoming.
89
-------
fluoride levels in excess of 2.0 mg/1 for water from the Tertiary
aquifer system or Quaternary aquifers.
Nitrate
The distribution of reported nitrate concentrations in excess of
the primary drinking water standard (45 mg/1 as N0^~) is shown in
Figure V-7.
About half the reported exceedences of the nitrate standard are
from wells less than 200 feet deep in areas north of Cheyenne. In these
areas substandard lot size, substandard well-septic tank spacing, and
livestock populations all contribute nitrates to the shallowest part of
the Tertiary aquifer system (Don Peck, Cheyenne/Laramie City/County
Division of Environmental Health, personal communication, September,
1981). Use of these wells for drinking water supply is being phased
out, as the areas are being annexed to Cheyenne, with city water supply
provided.
The nitrate standard is also exceeded in water from some wells in
the Tertiary aquifer system and Quaternary aquifers in other parts of
the basin (see Figure V-7). Most of these reported high nitrate levels
occur in areas of extensive farming and irrigation. In Laramie County,
Lowry and Crist (1967) attributed generally higher than expected nitrate
concentrations (^10 mg/1) to chemical and organic fertilizer derived
nitrate.
Secondary Standards
The secondary drinking water standards for which water analyses are
available in the Denver-Julesburg basin include sulfate, chloride, iron,
and total dissolved solids. Total dissolved solids concentration ranges
90
-------
are displayed spatially on Plates 3 to 8. Table V-l summarizes sulfate,
chloride, and iron concentration ranges by county. Waters from most
aquifers generally do not exceed the secondary drinking water standards
for these constituents. However, central basin composition of ground
waters from pre-Pierre Shale aquifers is poorly known.
Sulfate concentrations consistently exceed the recommended maximum
(250 mg/1) in Cloverly aquifer waters from Niobrara County, and some
Newcastle aquifer waters in Laramie County. Waters from shallow
aquifers in Platte and Goshen counties occasionally exceed the standard.
Chloride concentrations consistently exceed the recommended maximum
(250 mg/1) in waters from the Newcastle aquifer in Niobrara and Laramie
counties.
High iron concentrations occur sporadically in waters from most
aquifers.
Radionuclear Species
Limited data are available on concentrations for radionuclear
species in the Denver-Julesburg basin (Table V-2). Several
determinations of dissolved uranium and radium-226, a decay product of
uranium-238, have been made. Three determinations of gross alpha
radiation are available. Primary drinking water standards have been
established for radium-226 (5 pCi/1) and gross alpha radiation (15
pCi/1).
Analysis for radium-226 and gross alpha may contain an error limit
that generally indicates the 95 percent confidence interval of the
analysis. Variance in measured concentrations is usually due to either
(1) instrument insensitivity at low concentrations or (2) particle
absorption in samples containing high dissolved solids. Where the
91
-------
Table V-l. Range of reported concentrations (mg/1) of chloride, sulfate, and iron, by aquifer and
county, Denver-Julesburg basin, Wyoming.
Aquifer
County
Chloride
Sulfate
Iron
Paleozoic Aquifer System:
Madison (Guernsey)
Hartville (Casper)
Mesozoic Aquifers:
Cloverly
Newcastle
Lance/Fox Hills
Tertiary Aquifer System:
White River
Arikaree
Ogallala
Niobrara
Laramie
Niobrara
Platte
Laramie
Niobrara
Platte
Laramie
Niobrara
Goshen
Laramie
Goshen
Laramie
Niobrara
Platte
Goshen
Laramie
Niobrara
Platte
Laramie
(2)
(1)
(3)
(15)
(1)
(7)
(1)
(9)
(6)
(29)
(78)
(5)
(9)
(11)
(16)
(8)
(10)
(48)
110-130
3
0.7-29
1.7-9
108
5.9-320
3.6
(10) 2360-13600
(2) 9.5-10
7.5-113
5.2-31
2.7-268
2.0-31
12-70
3.5-52
2-22
2.0-16
2.8-40
4-25
1.0-62
(2)
(1)
(3)
(15)
(1)
(7)
(1)
(8)
(2)
(9)
(6)
(29)
(81)
(5)
(9)
(11)
(17)
(8)
(10)
110-120
7
7-146
1.6-118
62
29-1400
4.0
0-8823
300-1600
0.9-405
28-54
13-486
3.8-74
25-150
16-305
0.0-73
6.0-97
4.8-30
6-172
(1) 0.04
(3) 0.12-1.6
(14) 0.00-0.04
(1) 0.04
(8) 0.02-0.97
(4) 0.01-0.11
(28)
(44)
(3)
(8)
(12)
(9)
(8)
(9)
0.00-1.1
0.00-1.1
0.01-3.3
0.00-0.26
0.01-0.26
0.00-0.14
0.00-0.29
0.01-0.27
(48) 0.3-87
(32) 0.00-5.8
-------
Table V-l. (continued)
Aquifer
County
Chloride
Sulfate
Iron
Quaternary Aquifers:
Terrace deposits
Alluvial deposits
Goshen
(7)
1.7-14
(9)
80-200
(11)
0.
,01-0.
.11
Laramie
(10)
4.0-19
(10)
8.6-42
(4)
0.
.00-0.
,02
Platte
(11)
12-21
(11)
155-340
(11)
0.
.01-0.
,15
Goshen
(47)
1.7-29
(54)
29-430
(58)
0.
.01-5.
, 3
Laramie
(20)
5-27
(20)
16-162
(6)
0.
,00-0.
,19
Niobrara
(6)
4.0-15
(6)
6.6-6600
(1)
0.
.05
Platte
(14)
3.0-27
(14)
2.4-634
(14)
0.
,02-2.
8
dumber of analyses represented by range.
-------
Table V-2. Reported analytical data for radiometric species in
ground water, Denver-Julesburg basin, Wyoming.
Gross Radium Uranium
Alpha 226 (as U)
Location Aquifer (pCi/1) (pCi/1) (yg/1) Source
21/61-15 cdd
Lance
-
0.01
15
a
21/61-32 adc
Lance
-
0.20
140
a
22/62-5 cdc
Lance
-
0.28
270
a
22/62-10 bbc
White
River
-
0.10
97
a
23/61-16 bbb
White
River
-
0.24
120
a
23/62-26 ddd
White
River
-
0.14
160
a
23/63-6 ddd
White
River
-
0.15
38
a
24/62-26 dad
White
River
-
0.10
200
a
Town of Fort
Laramie
Quaternary
9.8+2.8
0.2+0.4
-
b
Town of
Guernsey
Quaternary
2.2+1.5
-
b
Town of
Hartville
Quaternary
& Arkiaree
7.0+2.5
0.0+0.5
b
Sources: a - U.S. Geological Survey Water-Data Report //WY-78-1.
b - U.S. Environmental Protection Agency, information
files, Denver, Colorado
94
-------
confidence interval is large relative to the given absolute value,
interpretation of results is difficult.
Gross alpha data are from tested community supplies deriving their
water principally from Quaternary aquifers. All three determinations of
gross alpha are below the primary drinking water standard.
Radium-226 determinations exist for Platte Valley Quaternary
aquifers and the White River and Lance/Fox Hills aquifers in Goshen
Hole. Reported values are all less than 0.28 pCi/1, well below the
primary drinking water standard.
Eight dissolved uranium determinations, made in 1978 by the U.S.
Geological Survey, for water from the Lance/Fox Hills and White River
aquifers in Goshen Hole range from 15 to 270 pg/1 dissolved uranium.
These uranium levels are higher than the typical range for natural water
(0.1 to 10 yg/1; Hem, 1970), and radium values from the same samples are
well below typical concentrations (<1 pCi/1; Hem, 1970). The source of
high uranium levels in these waters is unknown. Equivalent strata
contain economic uranium deposits elsewhere in the state, although no
commercial uranium deposits are known in Goshen Hole.
95
-------
VI. REFERENCES
-------
VI. REFERENCES
Anderman, George G., and Edward J. Ackman, 1963. Structure of the
Denver-Julesburg basin and surrounding areas, in Katich, P. J.,
and D. W. Bolyard, eds., pp. 170-175.
Babcock, H. M., and C. F. Keech, 1957. Estimate of underflow in the
Niobrara River basin across the Wyoming-Nebraska state line: U.S.
Geological Survey Open-File Report, 14 p.
Bjorklund, L. J., 1959. Geology and ground water resources of the upper
Lodgepole Creek drainage basin, Wyoming: U.S. Geological Survey
Water-Supply Paper 1483, 40 p.
Borchert, W. B., 1976. Geohydrology of the Albin and La Grange areas,
southeastern Wyoming: U.S. Geological Survey, Water Resources
Investigations 760-118, Open-File Report, 72 p.
Condra, G. E., and E. C. Reed, 1950. Correlation of the formations of
the Hartville uplift, Black Hills, and western Nebraska [Revised]:
Nebraska Geological Survey Bull. 13-A, 52 p.
Crawford, J. C., and C. E. Davis, 1962. Some Cretaceous waters of
Wyoming. In Guidebook, Wyo. Geol. Assoc. 17th Annual Field Conf.,
p. 257-267.
Crist, M. A., 1975. Hydrologic analysis of the Valley-Fill aquifer,
North Platte River Valley, Goshen County, Wyoming: U.S. Geol.
Survey Water-Resources Investigations 3-75, 60 p.
, and W. B. Borchert, 1972. The ground-water system in
southeastern Laramie County, Wyoming: U.S. Geological Survey Open-
File Report, 49 p.
, and M. E. Lowry, 1972. Ground water resources of Natrona
County, Wyoming: U.S. Geological Survey Water-Supply Paper 1897,
92 p.
Dana, G. F., 1962. Ground-water reconnaissance study of the State of
Wyoming, Part I: Wyoming Natural Resource Board, 195 p.
Darton, N. H., Eliot Blackwelder, and C. E. Siebenthal, 1910. Descrip-
tion of the Laramie and Sherman quadrangles [Wyoming]: U.S.
Geological Survey Geol. Atlas Folio 173, 13 p.
Denson, N. M., and T. Botinelly, 1949. Geology of the Hartville uplift,
eastern Wyoming: U.S. Geological Survey Preliminary Oil and Gas
Inv. Prelim. Map 102.
98
-------
Denson, N. M., and M. H. Bergendahl, 1961. Middle and upper Tertiary
rocks of southeastern Wyoming and adjoining areas, in Short
papers in the geologic and hydrologic sciences: U.S. Geological
Survey Prof. Paper 424-C, p. C168-C172.
Dockery, W. Lyle, 1939. Underground water resources of Horse Creek and
Bear Creek valleys, southeastern Wyoming: Masters thesis,
University of Wyoming, Laramie, Wyoming, 53 p.
Droullard, E. K., 1963. Tectonics of the southeast flank of the Hart-
ville uplift, Wyoming, in Katich, P. J., and D. W. Bolyard, eds.,
pp. 176-178.
Eisen, C. E., K. R. Feathers, and G. Kerr, 1980. Report on the
preliminary findings of the Madison baseline study: Wyoming Water
Resources Research Institute, 72 p.
Gutentag, E. D., and J. B. Weeks, 1980. Water table in the High
Plains aquifer in 1978 in parts of Colorado, Kansas, Nebraska,
New Mexico, Oklahoma, South Dakota, Texas, and Wyoming: U.S.
Geological Survey Open-File Report 80-50.
Hem, J. D., 1970. Study and interpretation of the chemical character-
istics of natural water: U.S. Geological Survey Water-Supply
Paper 1473, 363 p.
Katich, P. J., and D. W. Bolyard, eds., 1963. Geology of the northern
Denver basin and adjacent uplifts: Rocky Mtn. Assoc. of Geologists
14th Field Conf. Guidebook, 295 p.
Lines, G. C., 1976. Digital model to predict effects of pumping from
the Arikaree aquifer in the Dwyer area, southeastern Wyoming: U.S.
Geological Survey Water Resource Investigations Open-File Report
8-76, 24 p.
Lowry, M. E., 1966. The White River Formation as an aquifer in south-
eastern Wyoming and adjacent parts of Nebraska and ColoradoIn
Geological Survey Research, 1966: U.S. Geological Survey Profes-
sional Paper 550-D, p. 217D-222D.
, and M. A. Crist, 1967. Geology and ground-water resources
of Laramie County, Wyoming: U.S. Geological Survey Water-Supply
Paper 1834, 71 p.
Lundy, D. A., 1978. Hydrology and geochemistry of the Casper aquifer
in the vicinity of Laramie, Albany County, Wyoming: Wyoming Water
Resources Research Institute, Misc. Pub. No. 75, 76 p.
Maughan, E. K., 1963. Mississippian rocks in the Laramie Range,
Wyoming, and adjacent areas, jui Short papers in geology and
hydrology: U.S. Geological Survey Prof. Paper 475-C, p. C23-C27.
99
-------
, 1964. The Goose Egg Formation in the Laramie Range and adjacent
parts of southeastern Wyoming, in Geological Survey Research, 1964:
U.S. Geological Survey Prof. Paper 501-B, p. B53-B60.
McGrew, L. W., 1953. The geology of the Grayrocks area, Platte and
Goshen counties, Wyoming: Masters thesis, University of Wyoming,
Laramie, Wyoming.
Morgan, A. M., 1946. Progress report on the geology and ground-water
resources of the Cheyenne area, Wyoming: U.S. Geological Survey
Open-File Report, 55 p.
Morris, D. A., and H. M. Babcock, 1960. Geology and water resources
of Platte County, Wyoming: U.S. Geological Survey Water-Supply
Paper 1490, 195 p.
Rapp, J. R., D. A. Warner, and A. M. Morgan, 1953. Geology and ground-
water resources of the Egbert-Pine Bluffs-Carpenter area, Laramie
County, Wyoming: U.S. Geological Survey Water-Supply Paper 1140,
67 p.
, F. N. Visher, and R. T. Littleton, 1957. Geology and ground-
water resources of Goshen County, Wyoming: U.S. Geological Survey
Water-Supply Paper 1377, 145 p.
Richter, H. R., Jr., 1980. Occurrence and characteristics of ground
water in the Laramie, Shirley, and Hanna basins, Wyoming: Wyoming
Water Resources Research Institute, report for U.S. Environmental
Protection Agency, v. II1-A, 117 p.
Stock, M. D., 1981. Geohydrology of the shallow aquifers in the
vicinity of Old Woman anticline, Niobrara County, Wyoming: Masters
thesis, Department of Ceology, University of Wyoming, Laramie,
in preparation.
Theis, C. V., R. H. Brown, and R. R. Meyer, 1963. Estimating the trans-
missivity of aquifers from wells, Iii Methods of determining
permeability, transmissivity, and drawdown: U.S. Geological Survey
Water-Supply Paper 1536-1, p. 331-341.
U.S. Environmental Protection Agency, 1978. Public water supply
inventory, U.S. EPA Region 8, Water Supply Division, Denver,
Colorado.
U.S. Geological Survey, 1971. Chemical quality of water in southeastern
Wyoming: U.S. Geological Survey Basic Data Report, 13 p.
Weeks, E. P., 1964. Hydrologic conditions in the Wheatland Flats area,
Platte County, Wyoming: U.S. Geological Survey Water-Supply
Paper 1783, 80 p.
100
-------
Welder, G. E., and E. P. Weeks, 1965. Hydrologic conditions near
Glendo, Platte County, Wyoming: U.S. Geological Survey Water-
Supply Paper 1791, 82 p.
Whitcomb, H. A., 1965. Ground-water resources and geology of Niobrara
County, Wyoming: U.S. Geological Survey Water-Supply Paper 1788,
101 p.
Wyoming Agricultural Statistics, 1979. Wyoming crop and livestock
reporting service, 106 p.
Wyoming Geological Survey, 1981. Petroleum information files.
Wyoming State Engineer, 1981. Information files.
Wyoming Water Planning Program, 1971. Water and related land resources
of the Platte River basin, Wyoming: Wyoming State Engineer's
Office, 200 p.
, 1973. The Wyoming framework water plan: Wyoming State
Engineer's Office, 243 p.
101
-------
APPENDIX A
GROUND-WATER USE
NONMUNICIPAL
INDUSTRY IN THE
BASIN,
BY MUNICIPAL AND
SYSTEMS AND BY
DENVER-JULESBURG
WYOMING
-------
Table A-l. Water use by municipalities in the Denver-Julesburg basin, Wyoming.
Location
Number of
Operating
Wells
Primary Source Secondary Source
Source
Source
Average Production
Source
Source
Average
Population gal/cap/da
Served Production
Supplementary
In formation
>
Goshen
Fort Laramie
T24N, R64W,
Sec.
23
2
ground
Quaternary
-
24 7,500
277 .4
300
825
Lingle
T25N, R62W,
Sec.
18
3
ground
Quaternary
White R.
-
130,000
145.7
460
282
South Torrington
Water District
33,000
37.0
600
52
Purchases water
from Torrington.
Torrington
T27N, R61W,
9,10,15
Sec.
3,
12
ground
Quaternary
White R.
-
4,300,000
4,820.2
4,000
1,075
Voder
T23N,R62W,
Sec.
34
2
ground
Lance
-
11,250
12.6
102
110
Laramie
Albin
T17N.R60W,
Sec.
29
3
ground
Arikaree
-
61,200
68.6
125
489
Burns
T14N, R62W,
Sec.
7
4
ground
Arikaree
-
60,000
67.3
300
200
Cheyenne
T13-15N, R68-69W
47
surface
Douglas ground
Creek
Ogallala
White R.
13,000,000
14,572.8
50,000
260
12 of the 47 wells
are for emergency
and standby use.
Orchard Valley
T13N, R66W,
Sec.
18
2
ground
Ogallala
-
40,000
£-
CD
400
100
Pine Bluffs
T14N, R60W,
Sec.
14,15
6
ground
Quaternary
White R.
-
425,000
476.4
1,000
425
South Cheyenne
Water District
411,000
460
6,000
69
Purchases water
from Cheyenne; total
is included in
Cheyenne figures.
Niobrara
Lusk
T32N, R63W,
Sec.
7,8
7
ground
Arikaree
-
163,000
182.7
1,600
102
Platte
Chugvater
T21N, R66W,
Sec.
30
3
ground
White R.
-
14,000
15.7
200
70
Glendo
T29N, R68W,
Sec.
19
?
ground
White R.
-
20,000
22.4
450
44
Guernsey
T27N, R66W,
Sec.
35
1
ground
Quaternary
-
220,000
246.6
1,115
197
Hartville
T27N, R66W,
Sec.
12,13
3
ground
Quaternary
Arikaree
-
40,000
.£>
¦O
00
246
163
Wheatland
T24N, R68W,
Sec.
12-14
12
ground
Arikaree
-
1,750,000
1 ,961.7
4,600
380
Average gallons/capita/day production =
(average production gallons/day)
(population served)
Figures include some industrial use.
SOURCES: U.S. Environmental Protection Agency,
Files.
Region 8, Water Supply Division, 1979, Public Water System Inventory; Wyoming State Engineer Permit
-------
Table A-2. Non-municipal community public drinking water supplies in the Denver-Julesburg basin (supplied by ground water).
County
Location
EPA PWS Average Production Population
ID Number Aquifer gallons/day AF/y Served
Service
Facility Name
Goshen
>
I
ro
T24N, R61W, Sec. 5 DD
T13N, R66W, Sec. 4 CD
T14N, R66W, Sec. 22
T14N, R67W, Sec. 36 DC
T14N, R66W, Sec. 15 CA
T14N, R66W, Sec. 15 AD
T14N, R66W, Sec. 26 AD
T16N, R65U, Sec. 17 BB
T14N, R66W, Sec. 22 AA
T13N, R66W, Sec. 5 DB
Platte T27N, R65W, Sec. 7 AC
5600171
5600170
5600268
5600266
5600057
5600264
5600272
5600263
5600085
5600267
5600051
5600282
5600021
5600260
5600265
5600261
5600262
5600024
Quaternary
Ogallala
Ogallala
Ogallala
Ogallala
Ogallala/
White River
Ogallala
Arikaree
Ogallala
Ogallala
Precarabrian
2,500
1,550
8,750
4,250
13,350
4,200
2,600
7,875
3,225
8,700
3,500
5,300
1,600
3,750
5,250
9,000
5,625
70,000a
2.8
1.7
9.8
4.8
15.0
4.7
2.9
8.8
3.6
9.7
3.9
5.9
1.8
4.2
5.9
10.1
6.3
78.5
50 Mobile Homes Potlach Trailer Court
31 Mobile Homes Westwood Mobile Home Court
175 Mobile Homes A & A Mobile Home Park
85 Mobile Homes Avalon Trailer Park
267 Mobile Homes Cimmaron Village
84 Mobile Homes Circle ER
52 Mobile Homes Continental
105 MobiJe Homes Hideaway Mobile Home Park
43 Mobile Homes Hilltop
174 Mobile Homes Hyland Mobile Home Park
90 Mobile Homes Miller Lower Mobile Home Park
108 Mobile Homes Mountain View Mobile Home Park
32 Mobile Homes Pines Mobile Home Park
51 Mobile Homes Prairie Haven Mobile Ranch
70 Mobile Homes Shannon Heights
120 Mobile Homes Town and Country MobiJe Park
75 Mobile Homes Trails End Mobile Home Park
230 Company Town CF&I Steel Corporation
Industrial and non-municipal community use.
Sources: U.S. Environmental Protection Agency, Region 8, Water Supply Division, 1979, Public Water System Inventory, Wyoming State Engineer Permit Files
-------
Table A-3. Non-community public drinking water supplies in the Denver-Julesburg basin (supplied by ground water).
County
Location
EPA PWS Average Production
ID Number Aquifer gallons/day AF/y
Population
Served
Facility Name
Albany
Goshen
T19N, R61W, Sec. 2
T19N, R61W, Sec. 2 CD
T29N, R63W
T19N, R61W
T19N, R61W, Sec. 8
T21N, R62W, Sec. ?
T21N, R62W, Sec. >
Laramie
T25N, R62W, Sec. 20 AD
T13N, R67W, Sec. 14 AA
T13N, R69W, Sec. 13 AA
T14N, R63W, Sec. 6 BC
5600415
5600491
5600412
5600237
5600411
5600676
5600420
5600734
5600696
5600711
5600416
5600489
5600414
5600413
5600409
5600410
5600170
5600418
5600427
5600428
5600298
5600593
5600494
White River
Quaternary
Arikaree
Quaternary
White River
Lance
Lance
White River
Quaternary
White River
Ogallala
White River
Ogallala
2,500
350
4,000
7,000
950
250
7,000
250
500
1,000
1,000
3,000
350
400
3,250
1,400
300
2,500
1,000
3,750
25,000
2.000
1,500
2.8
.39
4.5
7.8
1.1
.30
7.8
.30
.60
1.1
1.1
3.3
.39
.45
3.6
1.6
.33
2.8
1.1
4.2
28
2.2
1.8
500
60
100
220
30
25
175
25
50
100
25
160
50
40
130
35
150
500
200
375
800
200
75
Buford Store and Tavern
Asmeria Oil Inc.
Bear Mountain Station
Frontier School of the Bible
Huntly School
Jay Em Campground
La Grange Bar
La Grange School
Little Maverick Cafe
Little Moon Supper Club
Longbranch
Maverick Motel
Scotts Cafe
Stateline Oasis
Valli Hi Supper Club
Veteren School
Western Motel
Wheelers
Wyoming State Highway Department - Rest Stop 22
All the Kings Men
Antelope Cafe and Station
Arts Truck Terminal
Bar 13
Carpenter Elementary School
-------
Table A-3. (continued)
County
Location
EPA PWS
ID Number
Aquifer
Laramie
(cont.) TUN, R70W, Sec. 22 BB
T14N, R69W, Sec. 23 CA
>
4>
T14N, R63W, Sec. 6
T13N, R67W, Sec. 2 BA
T14N, R66W, Sec. 27 DA
T13N, R69W, Sec. 18 BB
T14N, R66W, Sec. 36 DA
T13N, R66W, Sec. 11 DD
Niobrara T32N, R64W, Sec. 13 BD
Platte
T32N, R64W, Sec. 13 AC
T26N, R68W, Sec. 12
T27N, R66W, Sec. 17 CD
5600648
5600426
560082
5600561
5600481
5600485
5600425
5600293
5600740
5600621
5600424
5600292
5600608
5600622
5600609
5600700
5600735
5600731
5600646
5600580
5600551
5600509
560039
5600693
Precambrian
White River
Ogallala
Ogallala
Ogallala
White River
Ogallala
Ogallala
Quaternary/
White River
Arikaree
Arikaree
Arikaree
Hartville
Average Production Population
gallons/day AF/y Served
750 .84 25
2,000 2.2 200
1,375 1.5 55
12,000 13.4 1,200
2,000 2.2 80
42,000 47.1 3,000
700 .78 70
12,096 13.6 346
1,500 1.8 100
250 .30 25
480 .54 48
750 .84 1,000
1,000 1.1 100
750 .84 150
400 .45 40
4,000 4.5 400
300 .33 30
750 .84 25
2,000 2.2 400
5,250 5.9 150
300 .33 30
2,250 2.5 45
13,500 15.1 300
50 .06 50
Facility Name
Curt Gowdy State Park
Fern and Rays Drive-ln
Gilchrist School
Hillsdale Bingo
Hillsdale School
Holdings Little America
Husky Terminal
KOA Campground
Little Bear Inn
Maxwells Trading Post
Morrison-Knudsen Co.
Rock Crest Water Co.
Stateline Cafe
Wyoming Information Center
Wyoming Potatoes Inc.
Wyoming Truck Plaza
Lusk Drive-ln Theater
Lusk Municipal Golf Course
Wyoming Highway Department Rest Aren 26
Diamond Guest Ranch
El Rancho
Frontier Recreations Inc.
Glendo Marina
Guernsey State Park - Sandy Beach 1
-------
Table A-3. (continued)
County
Location
EPA PWS
ID Number
Aquifer
Average Production
gallons/day AF/y
Platte
(cont.) T27N, R66W, Sec. 18 DD
T27N, R66W, Sec. 21 CB
T27N, R66W, Sec. 9 AB
T27N, R66W, Sec. 27 BA
T24N, R68W, Sec. 1 CD
T26W, R68W, Sec. 21 BB
5600694
5600692
5600691
5600569
5600568
5600644
Arikaree
Hartville
Hartville
Hartville
Arikaree
Arikaree
25
4,000
50
2,000
1,200
500
2,500
.03.
4.5
.06
2.2
] .3
.6
2.8
T28N, R68W, Sec. 17 CC
T22N, R65W, Sec. 6 AA
5600645
5600643
5600642
5600586
Arikaree
Arikaree
Arikaree
Arikaree
2,000
2,500
2,500
500
2.2
2.8
2.8
.6
Population
Served
Facility Name
25 Guernsey State Park - Sandy Beach 2
200 Guernsey State Park - Dump Station
50 Guernsey State Park - Long Canyon
200 Guernsey State Park - Headquarters
120 Rompoon Saloon and Steak House
50 Shamrock Station
500 Wyoming Highway Department - Dwyer Junction
Rest Area
400 Wyoming Highway Department - Rest Area 19
500 Wyoming Highway Department - Rest Area 20
500 Wyoming Highway Department - Rest Area 21
100 7 Flags Drive-in
-------
Table A-4. Industrial water use, Denver-Julesburg basin, Wyoming.
County
Facility/Industry
Primary
Source Type
Source
Source
Secondary
Source Type
Source
Source
Number
of Wells
Average Product ion
(ac-ft/yr)
Goshen
Holly Sugar Co.
surface
North Platte
ground
Quaternary
11
40
Lance
Petroleum Industry3
ground
White River
-
-
6
0.5
Laramie
Petroleum Industry
ground
White River
-
-
51
233
Husky Oil Co. Refinery
purchased
from Cheyenne
-
-
1,680
Wycon Chemical Co.
ground
Ogallala
-
-
19
869
Niobrara
Petroleum Industry
-
-
3
<0.1
Platte
Missouri Basin
surface
Grayrocks
ground
Arikaree
h
23,250b
Power Project
Reservoir
S> aPetroleum water use data from Wyoming Oil and Gas Conservation Commission, 1979. All other data from the respective industry.
On U
Roughly 20,500 acre-feet/year surface water, 2,750 acre-feet/year ground water.
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A P P E N
LOCATION AN
SYS
D I X B
D NUMBERING
T E M
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Location-Numbering System
The location sites of the wells are designated by a numbering
system based on the federal system of land subdivision.
The first number denotes the township, the second number denotes
the range, and the third number denotes the section. One or more
letters follow the section number and denote the location within
the section. The section is divided into four quarters (160 acres)
and lettered a, b, c, and d in a counterclockwise direction, beginning
in the northeast quarter. Similarly, each quarter may be further
divided into quarters (40 acres) and again into 10-acre tracts and
lettered as before. The first letter following the section number
denotes the quarter section; the second letter, if shown, denotes
the quarter-quarter section; and the third letter denotes the quarter-
quarter-quarter section, or 10-acre tract (Figure B-l).
R.66WR.63WR 64WR63WR 62W
Figure B-l. Well identification system based on township-range
subdivisions.
B-l
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