Timber Creek, near Mc Gill, Nevada.
WATER RESOURCES-RECONNAISSANCE SERIES
REPORT 42
WATER-RESOURCES APPRAISAL OF STEPTOE VALLEY,
WHITE PINE AND ELKO COUNTIES, NEVADA
By
Thomas E. Eakin, Jerry L Hughes
and
Donald Q_ Moore
Prepared cooperatively by the
Geological Survey, U.S. Department of the Interior
JUNE 1967
•
View northeast of McGill Worm Sprin g, near McGill, Nevada; discharge about 10 cubic feet per second; telflperoture 78° F.
FRONT COVER PHOTOGRAPH
Timber Creek, a tributary of Duck Creek, drains a part of the west flank of the
Schell Creek Range, northeast of Mc.Gill Nevada. View is downstream, a hort
distance above the pipeline intake.
,.
WATER RESOURCES - RECONNAISSANCE SERIES
REPORT 42
i>.
WATER-RESOURCES APPRAIS.'\L OF STEPTOE VALLEY,
-WHITE PINE AND ELKO COUNTIES, NEVADA
.,.
'
___
By
'
Thomas E. Eakin,
Jerry L. Hughes,
and
Donaid o. Moore
J:'repared coopera.tively by the
Geological survey,
u. s.
Department of the Interior
June 1967
•
CONTENTS
Page·
summary .
• •
•
1
•
Introduction.
Purpose and scope of the report.
Previous reports
Acknowledgments.
Physical setting.
Climate~
a
~
.
•
•
u
¥
3
4
•
•
5
5
•
~
•
Landforms and drainage
Mountains . • .
Alluvial apron. •
Valley lowland. •
Drainage~
3
3
•
~
Q
•
•
..
•
•
•
~
~
•
D
•
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Geology and water-bearing character of the rocks •
•
Hydrology . • . • .
• •
•
Precipitation.
Surface water.
1-\vailable records
•
•
Estimated runoff from the mountains
Ground water • • • • • . •
Estimated average annual recharge •
Estimated average annual discharge.
Storage • • . . •
•
Perennial yield •
" "
.
Effects of pumping in the valley-fill reservoir
Provisional budget for the valley-fill hydrologic
system
•
.
...
.
..
.
..
~-
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9
9
9
10
10
11
13
13
15
16
17
21
22
24
24
24
26
34
Chemical quality • •
•
•
•
Water quality and its re.lation to the ground-water
system
• • .
•
•
•
36
Use of water • • • •
Present use. •
Potential use.
38
38
39
~
.. ... .. .
•
•
Designation of wells and springs.
•
References cited.
•
• .
• • • •
• •
•
• •
40
•
List of previously published reports in this series
36
46
•
48
•
ILLUSTRATIONS
Pago
Plate l .
Generalized hydrogeologic map • .
In pockGt
0
Figure lo Map of east-central Nevada showing principal
roads, communities, weather stations, and
snow courses in Steptoe Valley . • • . o••
2. Map showing areas in Nevada described in
previous reports of the Water Resources Reconnaissance Series and the area described in this report • • • • . o o . .
Precedes
48
3, Graph showing cumulative departure from
average annual precipitation at McGill
(1913-63), Ely (1888-1912), and Kimberly
·Follows
(1929-57)o.
•
•
Follows
4
0
0
• • • •
0
13
• •
40
Hydrograph of Murry Springs at Ely.
..
Follows
5.
Graph showing monthly discharge in percent
of mean annual discharge of Cleve creek • •
Follows
16
21
TABLES
Page
Table 1.
2.
••
Average monthly and annual precipitation, in
inches, at five stations. • • • • .
.
.
water content, in inches, as of April l, at six
snow courses. . • • .
6
.7
..
14
3.
Quartile distribution of precipitation
4,
Miscellaneous measurements of selected springs
and streams, October 1965 • •
5.
Estimated average annual runoff.
6.
Summary of streamflow of Cleve Creek near Ely._
7,
Estimated average annual precipitation and groundwater recharge . • . . • • . . • • • • • • •
23
B.
Estimated average annual ground-water discharge
by evapotranspiration in the valley lowland
25
Effects of pumping from an unbounded aquifer .
27
9.
'*'
..
Follows
16
"'
•
18
20
-'
10.
Provisional budget for the valley-fill hydrologic
system • • • • • . • . • • . • . • . • • . .
35
11.
Field chemical analyses of water from selected
wells, springs, and streams.
12.
Records of selected wells • .
13.
Drillers' logs of selected w_ells.
•
FOllows
• 36
J"ollows
• • 36
•
41
•
WATER-RESOURCES
APP~~ISAL
OF STEPTOE VALLEY,
WHITE PINE AND ELKO COUNTIES, NEVADA
By
T. E. Eakin, J. L. Hughes, and D. 0. Moore
SUMMARY
Steptoe Valley in .eastern Nevada has a drainage area of
1, 975 square miles.
It extends northward fro1n the sc>uthern end of
\"1hite Pine County for about 110 miles into the southern part of
Elko County.
From Currie the valley axis rises southward from an
altitude of 5,800 feet to about 7,000 feet at the southern end.
Schell Creek Range bounds the east side of the valley and the Egan
and Cherry Creek Ranges form the western boundary. Commonly the
crests of these ranges are 3,000 to 4,000 feet above the valley
axis. East of McGill, the crest of the Schell Creek Range is about
11,000 feet for several miles.
··
•
Precipitation ranges from as little as 6 inches in the valley
lowland to more than 20 inches in the higher parts of the mountains.
Most of the runoff from t.he mountains above 7, 000 feet is derived
from snowmelt in the spring months.
Nearly half of the 78,000
acre-feet of runoff is generated in the drainage areas of Duck and
Steptoe Creeks in the Schell Creek Range and about one-fifth is
generated in the drainage areas of Goshute and McDermitt Creeks in
the Cherry creek Range.
Additional runoff generated below 7,000 feet in the alluvial
apron and valley lm<land occasionally may reach high rates for short
periods but this runoff generally is erratic . and commonly is not
susceptible to management for use.
A large quantity of ground water is stored in the valley-fill
reservoir, as is suggested by the 2.1 million acre-feet estimated
to be stored in the upper 100 feet of saturated deposits beneath
the principal area of ground-water evapotranspiration. Additional
ground water also is stored and transmitted in the consolidated
rocks.
Natural discharge from lowland springs is on the order of
22,000 acre-feet.
In turn, this is removed from the lowland by
evapotranspiration and is included in the 70,000 acre-feet of
annual evapotranspiration from the valley lowland.
.;,;.
•
The che.:nical quality of ground water generally is goOd in
Steptoe Valley, but locally, it may not be suitable for a·ll uses .
Copper production at McGill requires about 20 cfs, about
14,500 acre-feet a year, for plant operat:j;on.
The principal communities, Ely, East Ely, McGill, and Ruth, obtain their public
supplies mostly from springs, but a minor part cL>mes from wells .
Th<o ~~mh.i.ned requirements for public supply may be on the order of
1,200 acre-r~at a year.
1.
••
To date, most of the water used for agriculture in the valley
i.s derived from streams and springs. Much Of the water is us<~d on
natural pasture or meadow land.
However, the acreage of cultivated
crops and improved meadow is increasing., Pumping ground water for
irrigation has been practiced to a limited degree for many years,
commonly to supplement other supplies but partly as the principal
supply. In the last few years pumping ground water for irrigation
has been 2, 000 to 3, 000 acre-feet a year. ~'urther developtuent of
wells is in process following the release of Federal land under
provisions of the Desert Land Act.
The general effect of pumping on the ground-water system is
shown by hypothetical examples in which four pumping centers distributed along the valley lowland might withdraw water under either
continuous or cyclic pumping patterns. Part of the water would be
supplied by salvage of natural discharge, but a significant part
would be derived from ground-water storage and some from water
recycled within the well fields. vhth appropriate spacing of wells
and of pumping centers drawdowns may remain moderate for several
tens of years, with annual withdrawals of about 70,000 acre-feet .
•
•
2.
•
INTRODUCTION
Steptoe Valley lies almost entirely within Fhite Pine county
(fig, 1). U.S" Highways 6, 50, and 93 provide'ready access to
other parts of Nevada and beyond. Secondary paved,or graveled
roads provide access to all sections of the valley under most
weather conditions. The Nevada Northern Railroad linl<s the ElyMcGill area with the Vlestern pacific Railroad at Shafter and the
Southern Pacific company Railroad at Cobre.
Ely, East Ely, McGill, and Ruth are the principal communities
in the valley. Their economy is closely tied to the mining and
ranching activities in the county.
Mining activity began with the discovery of gold in 1863 in
Egan Canyon. Of the eight n1ining districts subsequently established within the drainage area of Steptoe valley, the Ely
(Robinson) district has had the most sustained and largest production. Minerals produced in the Ely district for the period
1908-60 h<lve a reported value of $814 million (Bauer, Cooper, and
Breitrich, 1960, fig. 1), Copper production has supplied more
than 90 percent of the dollar value and gold and silver production
the rest. Processing of the copper ore at McGill makes that in·,
dustry the largest single user of water in the valley.
•
Ranching and farming began in the early days of mining to
supply local needs in the valley. Livestock production gradually
increased to supply more distant markets,
In recent years farming
too has been expanding through withdrawals of Desert Land for
agriculture. Increased activity in recreation and tourism in
recent years has added income to the area, Three oil tests drilled
in the valley in 1965 attest to continued interest in the potential
development of oil in eastern Nevada.
Purpose and Scope of the Report
Brief investigations are being made by the u. S, Geological
Survey, in cooperation with the Department of conservation and
Natural Resources, to provide reconn<lissance information on water
resources for essentially the entire State. Previous reports of
the Reconnaissance series are listed at the end of this report.
Areas discussed in the previous reports are shown in figure 2,
which precedes the list of reports.
This report on Steptoe valley
is the 42d of the reconnaissance series.
It is based on a few
weeks field investigation, mostly during 1965, The report provides preliminary evaluations o£ the ground-,water system, including
estimates of average natural recharge and di'scharge, 'surface-water
runoff from the mountains, and chemical quality of the water"
Previous Reports
•
The principal previous report on the water resources of
Steptoe Valley is that of Clark and Riddell (1920) . They described general ground-water conditions and the location of thenexisting wells, and measured the discharge of many streams and
3.
•
spr 1n<JS in .t.ho;'. V'-1}).-:.y •... Their. ?rincipal eff?rt, how>ver, W<'lS test
drillin<:r i).~J:c'it'c"'~J'<•\1\''\. •i;f ~;:!Gill ·to exJ;l:ore ~he );:q,o<sib:clity of developing 'of.1"0Uh:::_ wit:.e;r for irr igatiD!l i,n · gav.9ral;lle eesert vallGy's.
Acknowledgments
Many people in Steptoe Valley kindly supplied informat~on
pertinent to this inv,~stigation, for •..which the authors are· most
appreciat::.ve. Hr. Dnane E. Everett and Mr. Otis Purkiss of the
Geologic.>l survey also .assisted the authors, 'bot)'! ih "j:i.!'fld and
office operations, in this study,
"
4.
.
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EXPLANATION
E
L
K
0
'I
Basin boundMy
I
0
Town
"
Weatt)cr stations
---------1
I
Snow course
20
10
0
I
30
o==l
b:=.
Scale In Miles
}
Area ot report
• Kalam•IZoo Creek
•
w
T
H
N
•
y
E
E
p
N
E
'r---_ _,__ ------i
LINCOLN
Figure 1 .-Map of east-central Ne-vada showing principal roads, cor'!lnlunities,
weather stations, and snow coul'ses ir' Steptoe Valley
I
-·
PHYSICAL SETTING
Climate
Annual precipitation at the Ely Airport on the lowlands
generally is less than 9 inches. Annual precipitation may average
as little as 6 inches in the other lowland areas toward the north
end of the valley. Precipitation at the higher altitudes in both
the Egan and Schell Creek Ranges averages more than 20 inches, and
locally may exceed 30 inches. Table 1 gives monthly and annual
precipitation at five stations in Steptoe valley. The winter accumulation of snow in the mountains is an important indication of
runoff conditions in the spring. Table 2 gives the April 1 water
content for the period of record at six snow courses in or adjacent to the drainage area of Steptoe Valley.
Steptoe Valley is characterized by a wide range in daily and
seasonal temperatures. At McGill, the average annual temperature
is 47.4°F. January and July have the lowest and highest avera~e
monthly temperatures. The average January temperature is 16.5 F,
and the average July temperature is 7l.2°F. McGill has recorded a
maximum temperature of 100°F on several dates; the lowest recorded
temperature was -25°F on January 20, 1937. At Ely Airport the
average annual, January, and July temperatures are 44,l°F, 23.2°F,
and 67.l°F, respectively. Daily ranges in temperature commonly
are 30 degrees or more.
Houston (1950, p. 16) indicated the growing season for this
area to be about 119 days. However, the average growing season
may vary significantly, depending upon the relative topographic
location in the valley. The growing season also varies substantially from year to year at a given location •
•
5.
·.~'
'
....
•
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.
••
.
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'
.,
,,
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''·''
Table 1.
Average monthly and annual precipitation, in .inches,
at five stations
ffirom published records of the U. S. \·'!ea ther BureauJ
Jan.
Feb.
Mar.
;~pr.
Nay
June
July
:1ug.
sept.
Oct.
Nov.
Dec.
.
t1/
Ely Al.rpor
0.68
0.62
0.97
l.CS
0.93
0.83
0.57
0 .. 48
0.64
0. 71
o·.6l
0~
Kirnberlyll
1.50
1.45
1. 57
1.28
1.07
.67
.• 86
.90
.6S
.82.
~lcGilll./
. 71
.68
.77
l.OC
1.05
.78
.67
.83
.57
RuthY
.. $4
1 .. 48
1.02
1.30
.7C,-
1. 27
.33
.67
Sche11bourne Pass2f
.S4
l.W
1.30
1.3S
1.5S
.72
.52
.S3
Station
il.nnua1
'
58
8.65
.82
1.41
12.77
.75
.55
.62
8.91
.66
.4·8
.84
.5S
10.27
.78
.56
.73
.6S
11.02
0\
•
Altitude
Location
Period of record
1.
6,257 feet
17/63.-35d
25 years, 1S·39-6co
2.
7,232 feet
16/62-Bc
30 years, 1S28-58
3.
6,3<10 feet
18/64-28c
52 years, 1913-6<>
4.
6,832
f~et
16/62 -'c·d
7 years, 1958-64
5.
8,150 feet
22/65-Sa
11 years, lS 54.-64
Remarks
Gage moved to Ruth, 1958
.)•"-
Table 2.--hlater content, in inches, as of April:!, at six snow
courses
LFrorn published records of the Soil Conservation'Service_7
~-
Berry CreekY
water
Date
content
Bird CreeJ{1/
Kalamazoo creeklz
Water
Hater
Year
Date
content
Date
content
-------------~~i~n~c~h~e~s~)__________~(~i~n~c~l•~e~s~)__________~linch~e~s~)~---
-~~--:-:;-,...,-.,.--.-------::-:--..,-------~~----~--
19'-18
1949
1550
1951
3-29
3-30
4-03
4-02
14,2
18.9
16.7
12.2
3-29
3-29
4-03
4-02
6.8
7.3
.0
1952
1953
1954
1955
1956
4-01
3-31
4-01
3-29
3-27
30.7
12.7
17.6
15.8
17.9
3-31
3-31
4-01
3-29
3-27
11.3
1957
1958
lSSS
1960
1961
3-25
3-24
3-26
3-28
3-28
12.4
16.4
9.9
10.9
14.9
3-29
3-24
3-26
3-28
3-28
1962
1963
196<!1965
3-29
3-29
4-01
4-01
24-.0
8.3
11.3
16.6
3-29
3-28
4-01
4-01
.o
.o
4.6
4.2
.0
.o
6.0
.o
1.0
3.7
5.3
1.4
2;·7
2.5
3-27
3-30
3""":'29
3-30
4-02
3-27
3-29
10.4
1.6
7.3
6. ~.
--------------------------····--·--·----·--
••
1.
Berry Creek, altitude 9,100 feet, sec. 26, T. 17 N., R. 65 E,
2,
Bird creek, altitude 7,500 feet, sec. 34, T. 19 N,, R. 65 E.
3.
Kalamazoo creek, altitude 7,400 feet, sec. 34, T, 20 N.,
R. 65 E,
7.
Table 2;--Continued
.
. 4/
'Murray Summit-"'
5/
Robinson Summit-
VJater
.Year. Date
'
.
••
•
content
(inches)
Date
1937
1938
1939
1940
1941
4-01
4-01
5.1
2 .. 3
4-01
4-01
.4
4.8
1942
1943
1944
1945
1946
4-02
4-01
4-01
4-04
4-02
2.8
1947
1948
1949
1950
1951
4-02
3-29
3-31
4-03
4-02
1952
1953
1954
1955
1956
3-30
4-01
3-31
3-28
3-29
12.7
.0
4.5
4.2
.0
3-30
4-01
3-31
1957
1958
1959
1960
1961
3-29
3-25
3-25
3-29
3-27
.0
2.7
3-29
3-25
3-25
3-29
3-31
1962
1963
1964
1965
3-28
3-26
4-02
4-02
4~4
Water
c:ontent
(inches)
.
6/
Ward Mountal-n #2- · '
Date
Water
content
(inc:hes)
3-28
3-25
3-25
3-29
3-27
8.5
14.0
8.4
8.7
7,6
3-28
3-26
4-02
4-02
21.9
3.9
8.2
12.2
.o
5.6
4.8
3.0
.o
"L2
5.8
.0
.0
•0
.o
2.0
.0
3.3
T
.o
.o
4-01
4-02 .
14.0
.o
.o
.o
.o
2.9
3-28"
3-29
1.0
.0
.0
1.8
3-30
3-26
4-03
3-29
1.8
.o
2.8
T
4,
Murray Summit, altitude 7,250 feet, sec. 25, T. 16 N., R. 62 E.
5,
Robinson Summit, altitude 7,600 feet, sec:. 34, T. u3 N·.,
R. 61 E.
6.
Ward Mountain ii'2, altitude 8,900 feet, sec:. 25, · R. 15 N"''
R. 62 E •
8.
.. '·
•
.r '· -'
Landforms and Drainage
Steptoe Valley, '"'" used in this report, essentially is the
same as used by Clark and Riddell (1920) in their study, However,
in the present study the northern boundary was shifted northward
to cross the axial drainage through the gap about_ 5 miles north of
currie. The drainage area added to that used by Clark and RiddE,ll
includes McDermitt and Cottonwood creeks, 'rw~.:,l Springs about 7
miles northwest of currie, and the spring areas on ·the alluvial
apron and lowlands south and west o.f Currie. The Steptoe Valley
drainage area as-thus defined provides a more complete hydrologic
entity.
lt is noted however that many maps show Steptoe Valley
as extending northward to perhaps the vicinity of Shafter.
such
eJctension tends to weaken the value of using the name of Steptoe
Valley as a topographic and hydrologic unit.
Steptoe Valley, as restricted (pl. 1), extends from its
southern boundary northward 110 miles to the bedJ::·ock narrows 5
miles north· of Currie. Between drainage divides, the valley is
about 30 miles wide near McGill, but commonly its width is less
than 20 miles. The total drainage area of the valley is 1,975
square miles.
The lowest point j_s somewhat less than 5, 800 feet above sea
level near Currie. North Schell peak, altitude 11,890 feet, east
of McGill is the highest point.
steptoe Valley may be divided· into three general physiographic units--the mountains, alluvial apron, and the valley lowland.
Mountains
The crest of the Schell Creek Range,. east of McGill, exceeds
an altitude of 11,000 feet for a distance of more than 10 miles.
Elsewhere the higher peaks of the Schell creek and Egan H~anges
and Cherry Creek Mountains commonly exceed 10,000 feet.
These
mountains are 3,000 to 5,000 feet higher than the adjacent valley
flooro
'I'he flanks of the mountains generally are deeply incised.
The gradients of the canyons draining the mountains usually exceed
500 feet per mile and locally exceed 1,000 feet a mile.
The steep slopes aid the production of runoff.
However, some
upland areas have much flatter slopes, a condition which tends to
reduce runoff.
The most extensive area of low-gradient upland is
in theCurJ::ie and Boone Spring Hills and Antelope Range. Other
areas are in the south end of the valley and northwest of Ely.
Alluvial Apron ·
•
The alluvial apron occupies an area of intermediate slope
between the mounta·ins <~nd the valley lowland. surface gradients
commonly are 200 to 300 feet per mile but are as much as 500 feet
per mile adjacent to the mountains.
9.
•
.
Some parts of the alluvial apron are veneered by unconsoli~
dated deposits overlying an eroded surface. of consolida~ed or
par~ly consolidated rock.
These surfaces·, called pedimen~s, occur
opposite mountain segments with poorly developed canyons and be~
·tween some of the principal canyons. There are large alluvial
fans at the mouths of some of the principal canyons. 'l'he alluvi~
al fan formed by deposits from the Duck Creek drainage area is of
remarkable size. The fan extends westward 7 miles from the apex
at Gallagher Gap.
It displaces the axis of valley drainage west~
ward several miles.
It is estimated that the maximum thickness
o£ the alluvial deposits forming the fan may exceed 300 feet near
the apex. For the most part, however, the thickness of unconsolidated alluvium underlying the surface of much of the alluvial
apron probably is 200 feet or less.
Valley Lowland
The valley lowland has a general northward gradient of a
little more than 9 feet per mile.
The gradient, however" is not
uniform.
It is about 15 feet per mile for several miles'south of
Comins Lake.. Between comins Lake and Ely it increases to about
18 feet per mile. The gradient further increases to about 30
feet per mile between Ely Airport and west of McGill. Northward
from the latitude of McGill the gradient decreases.
Between Warm
Springs station and Schellbourne the gradient is about 5 feet per
mile.
Between Cherry Creek highway and Currie:': the gradient averages about 3 feet per mile although in the Goshute Lake segment
the gradient probably is less than one foot per mile.
The lowland ranges in width from about one-quarter roile in
the r"'stricted flood-plain. segments south of Ely to more than 7
miles in the Goshute Lake area in the north.
·..,. ...
""
Most of the valley lowland is a flood plain incised in the
lower parts of the alluvial apron by streamflow through the valley in late Pleistocene time, The bluffs, bounding the flood
plain, are most prominent and the flood plain is narrowest south
of Ely and in ·the narrow part of the valley in the vicinity of
Warm Springs Station. Tributary stream channels are graded to
the valley lowland.
Drainage
•
Duck and St0ptoe Creeks which drain the-higher parts of the
Schell Creek Range, arE> the principal streams in the valley. Several smaller creeks, . such as Wilson and Big. Indian Creeks, drain
the Schell Creek Range north of Duck creek. Murry and Gleason
Creeks drain the Egan Range in the vicinity of Ely; Goshute and
McDerroitt Creeks drain parts of the Cherry Creek Mountains in the
northern part of the .valley. Flow in most· strean1s ·reaches the
valley-lowland only during periods of high runoff froro snOWinelt or
high~intensity precipitation,
However, Steptoe Creek is peren~
nial to the floor of the valley. water froro Duck creek is routed
10.
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. t'
by.pipeline through the smelter at McGill, but then is discharged
·in the valley lowl~nd. A through-flowing stream draineq steptoe
valley through the.gap north of currie during parts of Pleistocene
time. Now, flow occurs from Steptoe creek through the valley and
beyond Currie only when runoff is large,
During early March 1966, lowland snowmelt, together with
runoff from Steptoe and Duck Creeks, produced a flow of 15 cfs or
more, in the lowland at least as far north as the Cherry Creek
road.
Geoloqy and Water-Bearing character of the Rocks
consolidated rocks exposed in the mountains include clastic,
carbonate,. and intrusive and extrusive igneous rocks.
These
rocks range in age fron• Precambrian to Tertiary. unconsolidated
and some partly consolidated deposits of ouaternary.silt, sand,
and gravel underlie most of the alluvial apron and valley lowland.
·.i -~
.·· • .
I
•
As much as 12,500 feet of Precambrian and Cambrian pirtly
metamorphosed clastic rocks have been described by woodward (1964)
in the northern Egan Range and by Young (1960) in the northern
Schell Creek Range. J.\ middle Paleozoic carbonabo> section has been
described in several localities; the stratigraphic thickness is
about 21,000 feet in the southern Egan Range (Kellogg, 1966),
16,100 feet in the northern .Egan Range (Woodward, 1964), 15,000
feet in the northern Schell Creek Range (Young, 1960), and" 16,000
feet in Spruce Mountain about 20 miles north of Currie (Harlow,
1956). Woodward (1964) described 4,100 feet of shale, siltstone,
and limestone overlying the Paleozoic carbonate section in the
northern· Egan Range.
shale and limestone of early·Me.-ozoic age,
possibly exceeding 3,000 feet ·ih thickness, have been, reported by
Snelson (1955) north of currie. young (1960) .has described a
·volcanic rock assemblage of Tertiary age as much as 3,500 feet
thick, and about 1,000 feet of conglomerate which unconformably
overlies the volcanic rocks in the northern Schell Creek Range.
An unknown thickness of unconsolidated to partiy.consolidated clay,
silt, sand, and gravel of Tertiary and Quaternary age underlies
the floor of steptoe Valley. Clark and Riddell (1920, p. 22)
reported that well 19/63-.l2al, 915 feet deep, encountered prevailingly clayey deposits below 124 feet. · They interpreted these
clayey deposits as lake beds,
For hydrologic purposes, the consolidated rocks are grouped
.into four units on plate L
The Precambrian and Lower Cambrian
clastic rocks and the Cretaceous or Tertiary intrusive rocks are
'two units generally considered to be a baJ:Tier. to laterial groundwater movement. 'rhe Proocambrian and r,ower cambrian clastic rocks
PJCOVide the lower limit to ground-water circulation. The extensive
.occurrence of these clastic· rocks in the headwater tributary
streams of Duck Cre§'k undoubtedly is a significant factor in the
relatively .large runoff fion1 ·this area. Another uni't of generally
limited capacity to transmit water includes volcanic and sedimentary rocks principally of 'l'ertiary age but includes some rocks of
ll.
•
Mesozoic age north of Currie. Volcanic rocks are the most
widely distributed rocks of this unit, particularly in the Schell
Creek Range north of Duck Valley and in the Currie and Boone
Spr:Lng Hills.
The fourth unit of consolidated rocks consists mostly of
Paleozoic carbonate rocks.
In part, these rocks transmit water
slowly, especially where they are metamorphosed. However, secondary fractures or solution openings in the carbonate rocks locally transmit ;;ubsta.ntial quantities of water.
In Steptoe Valley,
as in much of eastern Nevada, ground water transmitted in carbonate rocks is the principal supply for Murry, McGill warm Springs,
and many other large springs.
The valley fill is of Quaternary age in most of the area
shown on plate 1.
It is divided into two units--older and younger.
The older valley fill includes unconsolidated to partly consolidated silt, sand, and gravel mainly forming the surface of the
alluvial apron.
The maximum thickness probably is more than 1,000
feet.. Most of the older valley fill probably has a moderate to
low permeability.
However, these deposits have a large saturated
volume and thus contain a large quantity of ground water in
storacJe.
•
•
The younger valley fill consists of Recent silt, sand, and
gravel along the valley lowland and the flood-plain segments of
tributary channels. In the wider parts of the lowland in the
north half of the valley the younger valley fill may include lacustrine clays. Limited information suggests that the younger valley
fill may not exceed 150 feet in thickness.
The saturated sand
and gravel deposits of the younger valley fill yield water freely
to wells .
12.
'0·
•
.·, >
HYDROLOGY
The water in the hydrologic system of Steptoe Valley is
supplied by pr('lcipitation. Evapo1:ation and transpil·ation are
the dominant processes by which water is removed from the valley,
although a minor amount leaves the valley either as strc:oamflow or
underflow in the gap north of Currie.
Bet.ween the tirrie of precipitation and evapotranspiration the permeability of t~e soil
and rocks provides a significant control on the distribution and
movement of both surface water and ground water in the valley.
Most of the precipitation is removed by evapotranspiration from
where it falls either immediately or after a period of temporary
storage principally as snow or soil moisture. The remainder
enters the streamflow or ground-water systems from which it is
later removed by evapotranspiration.
Precipitation
•
The distribution and amount of precipitation are influenced
significantly by topography in steptoe Valley. Average monthly
and annual precipitation for five sta.tions were given previously
in table 1. Figure 3 shows the annual trend of precipitation as
cumulative departure from average precipitation at throoe of these
stations for their respective periods of record.
The 53-year
period of record for NcGill shows two relatively wet periods--1915
to 1923 and 1935 to 1947, and two relat:ively dry periods--1925 to
1935 and 1947 to 1962" The early record for Ely indicates a wet
period from 1893 to 1900 followed by a dry period.. The shorter
Kimberly and Ely Airport records generally are consistent with
the longer McGill record for the periods of overlap,
The Ely
J;irport rec;ord is not shown on figure 3.
variation in precipitation also is shown by the tabulation of
quartile distribution and maximum and minirnum monthly and annual
precipitation for Ely Airport, Kimberly, and McGill stations in
table 3. The median and quartile values divide the period of
record into four equal parts, that is, 25 percent of the years
(or individual months) of record have values between the maximum
year and the upper quartile, between the upper quartile and
median, betwGen the median and lower guartile, and between the
lower quartile and the minimum. Thus, annual precipitation at
McGill was between 16 .. 21 inches (maximum) and 11.29 inches (upper
quartile) dfiring 25 percent of the 53 years of record.
Similarly,
precipitation was between 8.58 inches (median) and 7.01 inches
(lower quartile) during 25 percent of the 53 years of record,
Half of the annual precipitation occurs during the period
December through May. Much of the winter precipitation accumulates as Gncw "1hich, when it melts, contributes significantly to
the spring runoff,
•
The precipitation at the several stations listed in tabl~ 1
shows a general increase with altitude.
It is evident that this
13.
•
40
McGill; Average, 9.01 inches
Ely: Average, 11.59 inches
Kimberly; Average, 13.241nchas
35
30
"'
w
I
'-'
"'
25
z
ui
20
"'<(
15
.
:::J
"'
....
•
I.,.._
"w
"
w
2:
....
<(
-'
:::J
:;;
I
I
10
I
I
5
:::J
u
I
I
\
I
\ ; ... ,
,,
I
I
I A
I
I
" I
I
...
\,
I
I
I
I
0
Il
1
....
-5
-10
1888
1900
1910
1920
1930
1940
1950
1960
YEARS OF RECORD
Fig we 3.-Cumulative departure from average annual precipitation at McGill (1913-63), Ely (1888-191.2) and Kimberly (1929-57)
•
•
•
•
- - - --------·
------------------
Jun~
July
..-..-.,
3~53
Lt':l.
L55
1.12
.43
.12
Aug
Q
S 2f; t ~
Oct~
.2 .lD
1,76
~-~------------- ~--
Fcv ~
--------------------------·----·----··
;_.,i.axi mum
"';o
Up;>er 'cuartile
~
q.-:;
_. ,.,/
1,51
. :37
2J/'':
l. 21
77
L 5:>
L:z-:iin1~
,. '] . .0:.
.56
.:>7
.7(
1.12
.51
.27
o:.i7
27
-1.:-G
,07
.?7
~53
~33
Ln~r.=:r
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T
:dumber cf yec,rs
27
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0
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~:
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• 41,
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~20
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T
27
27
z . .:~s
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P..,nnual
13.52
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~15
T
2.7
27
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Dec~
.':'..7
lt:.'-~
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59
27
27
KI~mEF.LY
-------
J
Upper
.:j_U.C:.~tile
i·ieciian
LmJsr ~.{Ui0.rtil·2
•
4.-ft
1. 71
l :,r.
72
T
y
{}. ;} 7
1
00
1~2{~
0
7:J
. -::.1,
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4. )2
2 _ :::6
1.39
~ 64
.12
31
2.24
3, 35
1~ 75
1J~9
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g2t~
.'l~
o
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1.25
74
~46
.Gl
1.~~
.25
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31
.77
,,
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G
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1.2l;
• 72
13. 06
llQOS
r
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~~r
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::cGILL
2-~ )[J
liaximuru
U:r;-:>~r
~91
.:::uartile
.5.S
~-!-eci.ien
I..o;-!er quartile
iliilirlllw.
aumber d
T
:·eurs
53
2. st,
1. r)~
7.55
1.42
3.33
.72
.34
~ 0 ;~
.84
.57
.11
.35
53
53
53
3.62
l.ll,
3.)3
1.03
2,92
1.3')
.47
.!;7
.75
.22
~ 2C~
~39
,•}2
ci
13
2~15
2.14
L'J3
L29
1.9-l
JJ7
~67
.43
.24
~22
53
53
~
-
~<
~·
1.~5
16~21
l~G2
11.29
-,!
53
53
53
:-3
•
relation is not uniform. Further, variation occurs at a given
altitude due to differences of exposure, orientation, local
relief, and other factors.
However, for general purposes, the
magnitude of average precipitation can be estimated from the
precipitation map of Hardman and Mason (1949, p. 11), revised by
Hardman in 1964.
·
The average volume of precipitation on the 1,975 square-mile
drainage area of Steptoe Valley is estimated to be on the order
of 870,000 acre-feet. This is obtained by multiplying the value
for average precipitation of the several zones tlines the acreages
of the respective zones, as shown on table 7 in the section.on
ground-water recharge. Actual precipitation in a given year may
be greater or less than this amount, but the value indicates that
a substantial amount of precipitation falls on the valley.
Surface Hater
Duck and Steptoe creeks are the principal streams in,Steptoe
Valley. They drain the highest yielding part of the Schell creek
Range (pl. 1). Duck creek is diverted by pipeline to supply the
requirements for copper production at McGill, and a significant
quantity of the waste water from the plant operations reaches the
valley lowland.
steptoe Creek is perennial to the valley lowland
in the Comins Lake area. During periods of high flow, Steptoe
creek flaws northward along the valley axis and is joined by water
of Duck Creek west of McGill.
Bassett Lake, about 6 miles northwest of McGill, is formed
by a small dam across the valley lowland. The lake is supplied by
water from Steptoe Creek, Duck creek, outflow from the McGill
plant, McGill springs, and springs in the lowland west of McGill.
Outflow from the lake in part is diverted to a ditch along the
east side of the lowland for irrigation.
under favorable runoff conditions,outflow from Bassett Lake
may flow northward to Goshute Lake. This flow may be augmented
from tributary flow north of Bassett Lake. Flow through the gap
north of Currie generally is derived from runoff generated in the
north end of the valley. The amount ordinarily is not large and
may average on the order of 1,000 acre-feet per year.
Several small streams, partly maintained by springs in the
Schell Creek Range between Duck Creek and Schellbourne Pass,
supply ranch needs in that area. Their flows may reach the valley
lowland during spring runoff.
•
McDermitt and Goshute Creeks are the principal streams
draining parts of the Cherry creek Mountains at the north end
of the valley. Egan Creek drains a small high tributary valley
between the north end of the Egan Range and the south end of the
Cherry Creek Range. Most of the low flow of Egan Creek is sustained by flow from a mine adit. Elsewhere, streamflow largely
1 ,.
-·-;)
.
·~-
•
••
·. · .r --
.-··-..
is limited to seasonal runoff in the spring or for short periods
after high-intensity rainfall •
Springs supply significant quantities of water for irrigation
along the west side of the valley in several areas northward from
Cherry Creek, southward from Steptoe, and in the Comins Lake area.
Murry Springs in Murry canyon south of Ely are the principal
source of public supply for Ely and East Ely. unused or waste
water from the public-supply system discharges to the lowland
northeast of Bly where it is used, at least in part, for irrigation, McGill Warm Springs (inside cover photograph) provide water
for a municipal swimming pool and part is used for copper production; the unused part discharges to the valley lowland. Smaller
springs occur elsewhere and are used for irrigation, livestock,
or ranch supplies.
Available Records
Miscellaneous discharge measurements of streams and springs
made during this investigation are listed in table 4. The locations of the 53 points are shown on plate 1. Clark and Riddell
(1920) measured streams and springs at 36 points during their
investigation in 1918. These miscellaneous measurements were used
in estifuating runoff from the mountains within the drainage area
of steptoe Valley.
In 1966 a gaging station was installed on
Steptoe creel<.
Some additional records of flow have been obtained for operational purposes.
Thus, the flow of Murry springs has been recorded at various times. Figure 4 shows the general flow of
Murry Springs during an interval of good control. A partial
record of flow of Steptoe Creek was obtained during the period
1961-64 by R. W. Millard and Associates, Inc., in a water-use
study for the CCC Ranch.
Records of flow of Duck Creek, which includes that of its
principal tributaries, Berry and Timber creeks, have been kept for
some 30 years in connection with plant operations at JYJcGilL
Generally, flow in excess of 20 cfs (cubic feet per second) is
diverted past the point of measurement just upstream from Duck
creek Reservoir. Much of the low flow of Duel: creek tributaries,
such as Timber Creek shown in the cover photograph, is carried in
pipelines across the alluvial fans to reduce low-flow losses. Thus,
the record only approximately represents natural flow conditions"
lG.
•
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•
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P~ec pitation a~ MeG ill
i
./"'-"
1--.
1'\
/
.......
~Cum ulati-.. e
departure from
1
_)..-- 1901·59 m ean
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---- --..-....._ r- ...... ......
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(Srid line f(lr priods of re-cot)
192G
1925
193()
~
-- r---- --"-..;,
Discharge of Murry Springs at El~ __ ............
191tJ.-
vv-
I
1940
1935
Figure 4.-Hydrogr.aph o-f Murry Springs at
E~y.
1945
(After Thomas, 1963)
"""--
15
u
iii
Cl
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uo
10
~ ~
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5
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0
1955
Cl
Estimated Runoff from the Mountains
.·
A reconnaissance technique for estimating runoff from
mountain areas recently has been developed for areas where few
streamflow data are available,
The general method has been described by Riggs and Moore (1965, p. Dl99-D202).
By means of
short-period or miscell~neous measurements, adjustments of regiona.! values can be made to compensate for local variations in
precipitation, geology and soils, topography, and vegetation.
The estimated average annual runoff from the mountains is
78,000 acre-feet (table 5). Nearly half the runoff comes from
the drainage areas of Duck and Steptoe Creeks. About 20 percent
of the runoff is derived from the Cherry Creek Range a11d most of
this is developed in the areas drained by McDermitt and Goshute
cresks.
The above estimate is for runoff from the mountain areas
generally above 7,000 feet.
Runoff also occurs from precipitation
on the alluvial apron and valley lowland, although generally this
runoff is erratic and less susceptible to management for use. An
impressive example of lowland runoff occurred in early March 1966,
Accumulated snow on the valley lowland melted during a several-day
period of mild temperatures. The rapid melting resulted in a
large volume of water thinly spread over much of the lowland. Part
of this melt-water collected into channels as lowland runoff. Runoff so generated contributed significantly to the flow of Steptoe
and Duck Creeks in their lowland segments.
17.
•
I'
Table 5. -- Estimated average annual runoff
(Based on record at Cleve Creek near Ely extended to l g J 5-23, 1945- 65)
ivi.ount.ain segment
Estimated runoff
(Acre-feet
h:>ercent of
per year)
total runoff)
.Schell Creek Range
(including L L>Ck
Creek Range)
·west flank of mountain
above 1, 000 feet
286,000
53
a 52, 000
67
Egan Range
East flank of mountains
above 7, 000 feet
162, 000
30
ll' 000
14
Cherry Creek Range
East flank of mountains
above 7, 000 feet
95,000
17
l 5, 000
19
543, 000
iOO
78, 000
100
~
C:·
Total
'I"
Location
Area
(percent of
Acres
runoff area)
a.
this total about 3 7, 000 acre-feet is derived from the drainage area between and including Steptoe
Creek ar.d East Creek, a tributary of Duck Creek.
()f
For the most part, however, usable streamflow is derived by
runoff from the mountains. Limited data for Duck and Steptoe
Creeks indicate that most of the runoff from these mountains is
supplied from snowmelt during the spring months. This is better
illustrated by the record of Cleve creek, the nearest stream for
which published records are available. Cleve creek drains a part
of the east flank of the .Schell creek Range.
lts drainage divi.de
in part is coincident with those of Duck and Steptoe Creeks.
The monthly distribution of streamflow of Cleve creek is
given in table 6. The graphs of monthly discharge in percent of
mean annual discharge are shown in figure 5. The data show that
about 45 percent of the mean annual runoff occurs in the three
spring months, April through June. Of course, in a given year,
runoff may be distributed quite differently than for the average
conditions. Thus, mild winter temperatures may result in distributing much of the snowmelt through several months preceding
April. On the other hand, if much of the annual precipitation
occurs as summer thundershowers, a significant part of the annual
runoff may occur during the summer months.
The disposal of the indicated runoff was not measured directly for the purposes of showing the general proportions of the
hydrologic system in the budget discussed later in the report.
However, som.e of the runoff, (a) is lost by evapotranspiration as
it flows on the valley fill and as diversion to irrigate cultivated crops, wet meadow, or pasture, either directly or after a
period of retention as soil moisture, (b) recharges the groundwater reservoir and, (c) reaches the valley. lowland where it is
lost by evapotranspiration either directly or after a period of
retention as soil moisture or ground water or, to a minor amount,
becomes outflow through the gap at the no:rth end of the valley.
A general evaluation of the flow system in Steptoe Valley suggests
that the approximate average magnitude may be about 26,000,
2~.000, and 28,000 acre-feet per year for it<?m (a),
(b), and (c),
respectively. The proportionally large value of 28,000 acre-fee~
for runoff to the valley lowland results from a significant part
of the flow of Duck Creek being routed to the valley lowland and
a large part of t.he flow of Steptoe creek being used for irrigation on the valley lowland .
•
E.
..
;-
••
.•
,.
,.
,
•
Table b. -- Summary of streamflow of Cleve Creek near Ely
(Discharge in cubic feet 2er second; periods of record, l 915-1 & and 1 ·) &0- S 5}
~
Feb,
Mar.
A9r~
?.64 5• .:::.~1 &.09
7. 14
ll.
Oct.
Nov~
Average
s.
s~
Maximum month
D. 76 2.97
7.25
Minimum month
4. S·S 4. 53
4.27 4. 05
93
_:. s
Dec, Jan.
e.
OS
8.05
L~,
a.
il.verage for '''aximum recorded water year.
b.
Average for ILinimum recorded water year.
42
14.8
4.65
s
24.4
6,34
May
June
July
16. 9 16, 3
2'~.
2 27.2
8. 58 6.2-5
8, 0'}
.'
!
.J~
)_
4. 96
Aug.
Sept.
6~
5, 90
L15
Year
8, 46
8.7Si
8,23 a l 0. 7
3~9S"
3. 7 5 b
5. IS
-·
Ground-Water
The principal ground-water reservoir is in the valley-fill
deposits of Steptoe Valley. '!vater occupies the open spaces
between the individual particles of the unconsolidated to ·partly
consolidated silt, sand, and gravel. The top of the zone of
saturation or water table is 111ithin a few feet of land surface
throughout most of the valley lowland northward from McGill. It
also is shallow in the lowland near Ely and Comins Lake, but is
deeper along the valley axis southward from the comins Lake area.
The depth to water generally increases toward the 1nountains beneath the alluvial apron.
The water-level contours {see pl. l)
show the general form of the water table. The water-level gradient slopes toward the valley axis from the mountains and northward
along the axis of the valley and confortns in a subdued way to the
general slope of the land surface.
Ground water also occurs in fractures or solution openings in
the consolidated rocks, especially the Paleozoic carbonate rocks.
Ground \1/ater has been encountered extensively in drilling and
underground mining operations in the Ruth-Kimberly area. Many of
the springs in the mountains attest to the fact that ground water
occurs and is transmitted in the consolidated rocks. The large
yields of Hurry ;;lUd McGill Springs indicate that the consolidated
rocks locally transmit substantial quantities of water.
However,
water occurs in and is transmitted through only a small fraction
of the total volume o£ consolidated rocks.
Ground water in the consolidated rocks and in the valley fill
is supplied by recharge from precipitation. The higher average
precipitation in the mountains and its accumulation as snow during
the winter months is favorable for recharge to the ground-water
reservoir in the valley fill. \~ater moves from the high areas in
the mountains toward the valley lowland where most of the ground
water is discharged by evapotranspiration. The natural recharge
to a ground-water system tends to equal natural discharge during
extended periods of climatic equilibrium. Within such periods,
however, intervals occur when recharge is greater than or less
than discharge, and these will be reflected in corresponding increases or decreases in ground-water storage.
The extensive spring area along the west side of the lo\Jland
in Campbell Embayment has given rise to speculation that some or
most of the water of the springs is supplied from Butte Valley to
the west. Data and estimates obtained in this investigation suggest there is sufficient recharge within the drainage area of
Steptoe Valley to supply the estimated discharge; indeed, the
recharge estimate is higher than the natural discharge estimate.
The altitude of the vmter level in the valley-fill reservoir of
Butte Valley is roughly 6,125 feet at the topographically low
part of the valley floor in T. 21 N., R. 61 E. This altitude is
only slightly high-er than the approximate 6,100-foot altitude of
the western line of springs in Campbell Embayment in Steptoe
Valley. The distance between the two areas is at least 12 miles.
The indicated potential gradient between these two areas toward
2l.
•
300
w
<.0
"'<>:
"'u
"'
"'....<>:
Quartiles
200
----
Median
:::J
•
z
z
<(
z
<(
w
:;<
"-
0
f-
100
zw
------ --
u
"'"-w
0
OCT
NOV
AUG
Figure 5.-Monthly discharge in percent of mean annual discharge ot Cleve Creek
•
SEPT
.,.
'
Steptoe Valley, is very low. Further, the Egan Range, which is
between the two areas, receives moderate precipitation. The
proportionally small runoff from the range suggests that gr.o:.lndwater recharge may be proportionally high.
Thus, Egan Range is
inferred to represent an hydraulic high, and be an effective
barrier to ground-water flow between the valley-fill ground-water
reservoirs in Butte and Steptoe valleys.
Estimated Average Annual Recharge
An empirical method has been used (Eakin and others, 1951) to
estimate ground-water recharge.
Precipitation is assumed generally to increase With altitude, and the proportion of precipitation
re.aching the ground-water reservoir is assumed generally to increase with increased precipitation. The lowest zone in which
effective precipitation occurs is considered to be the middle to
upper segments Of the alluvial apron"
The precipitation map of
Nevada (Hardman and Mason, 1949, p" 10) modified by Hardman in
1964 is used for delineation of the precipitation zones" Areas
of the precipitation zones are determined approximately at altitude
increments of 1,000 feet. The area of these zones times the average precipitation times the assumed percentage of recharge equals
the estimated recharge from precipitat.ion in that zone.
The sum
for the several zones then gives the average annual recharge for
the valley. Table 7 gives the pertinent values. The estimated
average annual recharge to steptoe Valley of 85,000 feet is 7
percent of the total precipitation, this is somewhat higher than
the percentages for most valleys in this part of the State, which
commonly average about 5 percent. This in turn suggests that the
estimate of recharge may be high •
••
2?..
,.
••
•
•'.
Table 7. --Estimated average annual precipitation and ground-water recharge
Precipitation
range
(inches)
Approximate
equivalent
altitude zone
(feet)
> 2.0+
N
"'
Effective area
r epre sente d
by this z.o·~1. 2
(acres)
Average annual )_Jrecipitation
Estimated recharge
(feet)
(acre feet)
: Percentage of
: precipitation
(acre -feet
per year)
above 9,000
57' 000
l. 7 5
100,000
2.5
25,000
l 5 to 20
8, 000 to 9, 000
150, 000
l. 46
230,000
15
34,000
12. to 15
7, 0 00 to 8, 0 00
a 26&,000
l. 12
300, 000
7
2.1,000
8 to 12
6, 000 to 7, 000
b 213,000
0.83
180,000
3
5,400
<8
below 6, 000
573, 000
0.6
340,000
Total {rounded)
1' 265, 000
( l, 97 5 sq. mi.)
1, 2.00, 000
85, 000
a. About 2.9, 000 acres of the zone was shifted to the 6, 000-to 7, 000 -foot zone for computing recharge on
the basis that the next lower zone was more typical of recharge conditions; additionally, about
184, 000 acres of this zone were considered to have essentially no effective recharge and thus
were shifted to the lowest zone for computing valley area.
b. About 3 40, 00 0 acres of this zone are on the lower part of the alluvial apr on and were cons ide red out
of the to;Jographic position of assumed effective recharge; the area was shifted to the less -than6, 000-foot zone for purposes of computing valley area.
Estimated Average Annual Discharge
Ground water is discharged naturally from the valley-fill
reservoir almost entirely by evapotranspiration in the lowland of
Steptoe Valley. Only a small amount may be discharged by underflow or surface flow through the gap north of currie,
The estimated discharge, summarized in table 8, is about 70,000 acre-fc-oet
a year
Spring di.scharge in the valley lowland is estimated to be
about 22,000 acre-feet, which in turn is lost by evapotranspi.ration largely. from the wet-meadow and sal tg·rass area listed in
table 8. Some ground water. is discharged from springs in the
mountains in addition to that: discharged from the valley 1owliwd.
For the most part, spring discharge in the mountains becomes a
part of the streamflow or is removed by evapotranspiration in the
mountain canyons. Ground water discharged in the moun·tains is not
included in ·the estimates in table 8.
o
In addition to ground water discharged by evaporation and
transpiration from the valley lowland, surface watEor supplied by
overland runoff from the mountains, by snowmelt on the valley
lowlands, and by occasional high-intensity showers also is evaporated or transpired from the valley lowland.
Storage
The volume of ground water stored in the valley fill of
Steptoe Valley is many times the volume annually recharged ·to and
discharged from the ground-wa·ter reservoir.
Although the total
volume of ground water in storage is not known, the following calculation illustrates that the quantity is very large..
On the
assumption tha·t the average drainable pore space (specific yield)
of the upper part of the saturated valley fill is 15 percent, the
volume of ground water in storage in t.he saturated upper 100 feet
beneath a one-township area (about 23,000 acres) is about 35,000
acre-feet.
Beneath the 143,000-acre evapotranspiration area,
indicated in table 8 and shown on plate l, the volume of ground
water stored in the upper 100 feet of saturated valley fill would
be about 2.1 million acre-feet. ,As the depth to water below land
surface generally is less than 20 fec·t, the indicated 2.1 million
acre-feet of stored water is within 120 feet of .land surface in
most of the evapotranspiration area.
Perennial Yield
•
The perennial yield of a ground-water system may be taken as
the amount of water that can be withdrawn from the syst.,,m for an
indefj_nite period without causing continuing depletion of storage
or a deterioration of the water quality beyond the limits of
economic recovery. Economic feasibility involves factors other
than those of ·the hydrologic system. However, based on the hydrologic system, the perennial yield may be taken to be a quantity of
water equivalent tothe average annual natural recharge to or
2··.:."
·'
-
'
~
.. -,
,. '
•
Table 8. --Estimated average annual ground-water discharge
by evapotranspiration in the valley lowland
Assumed average
rate of
evapotranspiration eva potrai1spiratio!l
(acre-feet)
(feet)
Estihiaied'
Phreatophyte
Area
(acres)
Wet-meadow and saltgras s
a.reas, including lowland
spring areas. Water table
generally at or near land
surface
18,000
•
1.5
27,000
Saltgrass, rabbitbrush,
some greasewood, and
playa areas, including
Goshute Lake playa.
Water table generally
less than 10 feet below
land surface
50,000
. 5
25,000
Greasewood-rabbitbrush
areas with some saltgrass; coinm(')nly
marginal to the first
two areas above. Water
table generally less than
20 feet below land su1·face
53, 000
•3
16,000
Scattered saltgrass,
rabbitbrush, and
greasewood area.
Water table generally
less than 12 feet below
land surface
22. 000
. l
2,200
----------Total (rounded)
•
143, 000
25.
70,000
discharge from that system, based on a one-time use of the s·tored
water.
In effect this can be accomplished most efficiently by
developing ground water in or adjacent to areCls of natural
discharge.
In Steptoe valley, the average annual recharge and natural
discharge were estimated to be 85,000 and 70,000 acre-feet per
year, respectively (tables 7 and 8). Because as previously Inentioned, the estimated recharge may be somewhat high and because
the estimated natural discharge is considered to be better controlled, the perennial yield provisionally may be taken to be
about 70,000 acre-feet.
Effects of Pumping in the Valley-Fill Reservoir
Withdrawals from wells in areas of natural discharge permit
direct salvage of that discharge and impose a minimum effect on
the ground-water system.
The greater the distance the wells are
from natural discharge areas the greater the percentage of pumred
water that comes from storage and the less the salvage of· natln-al
discharge.
'ro date, sufficient data are not available to demon·strate fully the effects of pumping from wells in steptoe Valley.
However, aquifer response to pumping varies with the quantity
pumped, the duration of pumping, the distribution of wells, :md
the storage and transmissive characteristics of the aquifer. The
effects of varying some of these factors can be illustrated by
assuming certain conditions that might reasonably Joe expected to
occu:t· i.n this area.
Assume that pumping rates are 1, 000 gallons a minute;· the
upper part of the saturated valley fill qeHerally has coefficients
of storage between 0.1 and 0.2 and transmissibility values between
10,000 and 100,000 gallons per day per foot.
By further assuming
·that the valley-fill ground-water rese:t·voir grossly functions as
an_approximate equivalent o£ a thick, unbounded, and relatively
un1£orm aquifer, the :J:>l>eis non-equilibrium formula ('l'heis, 1935,
and Theis _i_n, BcaLall and others, 1965) can be used for illust.rative compu·tation.
Table 9 illustrates the effects on drawdown and
radius of influence resulting from successively varying several of
the factors.
26.
••
Table 9. -- Effects of pumping hom an unbounded aquifer
a.
Effect of varying coefficient of storage (5). }:__/
(Assume T"' 50, 000; (~ = l, 000; t"' 10,000 (27.4 years))
-Appt:oximate________ _
CueJficient
of
storage
Drawdown(s), in feet, at
distance from well
.__::d:,:i.::s;:ta::n=c::.e__:(~r:-!)_;f:_:r:.:o:::n::;1:_;:w:_:e::_::l~l...,...._ _ _ _ _ _w.:::_:h e r c d r a wdown = 0 ft.
l ft
r = 10ft
r = 100ft
mile$
feet
----;:-=
0. l
48.3
47.4
46.7
0. 15
o. 2
~---·
70,000
58,000
53, 000
27.4
26.5
25.8
37.9
37. 0
3 6. 3
13.25
ll
10
--------~~--
b.
Effect of varying coefficient of transmissibility (T}.
(Assume 5 = 0. 15; Q = l, 000; t = 10, 000)
-----ApproJ<in•ate
Coefficient
of
transmissibility
10,000
ooo
113. 5
26. 5
100, 000
14,0
50,
c.
Drawdown(;;}, in feet,
at l 00 feet from well
distance from well
where drawdown = 0 ft.
-feet
miles
,.....:..
__
29,000
58, 000
80,000
5. 5
ll
15
Effect of varying rate of pumping (Q),
(Assume T = 50, 000; S = 0. 15; t = 2, 000 (5. 48 years))
Rate of
pumping G,
in ~12m
I,
000
Z, 000
4,000
8,000
16, 000
Lrilwdown(s), in feet, at
distm>ce·(T) from well
r =: 1 .ft
·r=lOft
1", =: 100ft
43.6
87.2
174
348
33.2
6S, 4
266
696
532.
Z2. 6
45.2
90.4
181
362
133
(table continued)
27.
Approximate
distance fTOrrl well
when' drawdown = 0 ft,
rnile s
feet
29,000
29,000
29, 000
29,000
29,000
5. 5
5. 5
5 . .5
5. 5
5.
s
Table 9. -- Continued
d.
0
Effect of varying duration of continuous pumping (t}.
(Assume T " 50, 000; S "' 0. 15; Q " 1, 000}
Duration
Approximate
of
Drawdown( s}, in feet, at
distance from well
pumping
distance (r} from well
where drawdown "' 0 ft.
days
years r " l ft
feet
miles
r "' 1 00 ft
r " 10 ft
-'-;-=--'--c~...:;..,::-;:;---;;":.__:_.,cc~=-----=-~~-=------;5;",~5o·~---1---100
• 27
37. 0
15.8
26. 5
500
1. 37
13, 000
2. 5
40.2
19. 5
29. 6
1, 000
2.74
21,000
4
42.2
21. 2
31. 6
2, 000
5.48
43.6
22.6
29,000
5.5
33.2
. •!5. 8
5, 000 13.7
35.;4
39,000
7.4
24.7
10, 000 27,4
58,
000
ll
26.5
47.4
37. 0
18, 000 49.3
70,000
13.2
26. ~.
48.0
37.8
e.
Effect of cyclic pumping, 100 days per year.
(Assume T" 50, 000; S" 0. 15; Q" 1, 000}
- - - --·--·--·-·-
Pumping for l 00 days a year,
begir1ning with the day
pumping began
At end of
Do.
Do.
Do.
Co.
Do.
a.
1>.
l.
.,
Dr a wdown( s }, in feet,
where radius " l 00 feet
a 15. 8
100 days
360 days (1 year}
720 days (2 years}
1, 080 days (3 yea1·s)
l, 440 days (4 yea.rs}
1, BOO days (5 years)
•7
.9
1.0
b
1.1
l. 1
Refer otlso to item 1 in table 9d above.
After 4 years, maximurrl effect of cyclic pumping in antecedent
ye«rs is reached ;~t this radius.
Notations for table <;,
T " The coefficient of transmissibility, in gallons per day per foot
(gpd per ft} of the aquifer;
S "' The coefficient of storage of the aquifer, a di,-nensionless ratio;
Q = The rate of di,.cha.rge in gallons per rninute (gprn). of the pumped
well;
s = The water-level drawdown, in feet, in the pumped well, in an
observation well, or ;~t any point in the vicinity of the pur,pcd
well;
r
The
dist<>nce, in feet, from the purnped well to ;J.n' obse1·vation well
"'
or to a point fo•· which the drawdown is to be determined;
t = The tirrieJ in dayH
since pun1ping began.
1
28.
••
Table 9a indicates that, other things being equal, the lower
the value of the; coefficient of storage, the greater the drawdown
and the greater t.he radius of influence that is required to yic'ld
the same amount of water from storage.
Initial responses to
pumping fron, valley-fill deposits, such as occur in steptoe valley,
commonly indicate that the ground water is under artesian conditions. That is, apparent values of the coefficient of st.orage
are significantly smaller than those used in the examples. For
the same pumping rates, the early periods of pumping probably
would develop larger drawdowns than are indicated by the examples
herein. However, over long pumping periods the apparent coefficient of st.orage gradually would increase to values characteristic
of unconfined conditions, such as those used as examples in this
report,
Table 9b shows that low values of transmissibility result in
large drawdowns with a small radius of in:ElucZ>nce, whereas for
large values of transmissibility drawdowns are small but t.he radius
of influence is very large.
Increasing the pumping rate results
in larger drawdowns within the same areas of influence as those
shown in table 9c"
IncrCJasing the duration of pumping increases
both the drawdown and the radius of influence, as shown in table
9d, where water is derived entirely from storage and other fac·tors
remain constanto
The effect of noncontinuous pumping is illustrated in table
where a cyclic pumping pattern of 100 days a year is used" 'rhus,
after 100 days of pumping the drawdown at 100 feet from the well
is shown as 15,8 feet; at the end of one year, or 260 days after
pumping ceased the residual drawdown is shown as 0" 7 foo·to The
residual drawdown due to pumping in antecedent years increases to
a maximum of about lol feet at a radius of 100 feet at the end of
four years. For example, at the end of the sixth pumping cycle
(1900 days) the drawdown at 100-foot radius would be .15.8 feet
{as at the end of the first pumping cycle) plus the residual drawdown from antecedent pumping (1 01 feet.) or a total drawdown of
about 17 feeL
'rhis may be compared with the 22"6-foot drawdown
at a radius of 100 feet for the 2,000-day continuous pumping period shown in table 9.
Thus, a cyclic or intermittent pumping
schedule results in less drawdown at the 100-foot radius than
would occur had the pumping been continuous.
9c
•
From the information in table 9, it is evident the<t the area
of influence of individual wells would overlap somewhat between
wells in irrigated areas, where well-spacing of \- to ~-mile is
common, This can result in a pattern of drawdown and area of
influence that is difficult to identify accurately in detaiL However, a general pattern can be described that illustrates the
magnitude of effect of pumping sever<J.l wells at the same time.
Assume that there are 16 wells spaced on ':-mile centers forming a
square of four rows of four wells each, as would occur with wells
in the center of one-quarter sections in a 4-square-mile area .
Assume further, that each well is pumped at the rate of 1,000
?t'
... - . .,.
~·
gallons a minute continuously for 10 1 000 days {27.4 years).
The
combined pumping rate for the 16 wells is equivalent to " with··
drawal· of about 25,000 acre- feet per year. -The assumed ac•uifer
characte1:istics are T ~ 50,000 ;s;nd S - 0.15, the same as gencerally
assumed for computations in table S. Under thase conditions at
the end of 10,000 days of pumping, the distance to :;oero dra1.vdown
would be about 12 miles from the center of pumping. Closer to the
well field, drawdown would be about 5 1 10, 10, 50, 75, and 100
feet at disti.l.nces £rom the center o:C pumping of about S, 7. 75,
3-BS, 3.3, 2.3, ·and 1.5 miles, respectively. Drawdowns oi about
160 feet would occur adjacent to the wells at the corners of the
well field, and drawdowns on the o:r:der of 190 feet would occur
adjacent to the four inside wells nf the well field.
These effects, as noted above, are for continuous pumping.
If the same annual ~uantity (about 25,000 acre-feet)were pumped
under a 100-day per -year cyclic pattern, about 58 lilells pun1ping at
the rate of 1, 000 gpm would be rec.<uircd. Using the same spacing
as in the previous exacnplc ~-mile centers, the well field would
occupy a l<(\-s<JUare mile area. ?,nalysis of this cyclic pat.tern is
more difficult than in the previous example. Generally, though, a
larger proportion of water vmuld be withdra,,;n from t.he lar9er are"of the well field, and the radius of influence would be somewhat
less than half the 12 miles computed tor the continuous pumping
patterns, both patterns being for 10, 000-day, elapsed-time perio(;s.
Further, j_f ·tlL• "''all fic.old and co.rco.•,-· of GJigniticont pul'Jping influence are in an area of natural discharge by evapotranspiration,
the drawdowns Houlcl be r•aduced in proportion to the umount of salvage of the natural discharge. After the amount of salvage is
w-;u·"-1 to the net a(oount of wat:.o'r pumped, the dr<~wdowns and area of
influence will be only of the magnitude necessdry to divert the
amount of water salvaged through the wells. Thus, in this use the
w11ter withdrawn by the wells is supplied by recharge to the nrea of
pumping- influenca rather than from storage within the area of in-·
fluence as j,n the circumstances previously assumed.
It should be recognized that the chemical quality of water
obtained in areas of natural discharge may not be as good as in
ot.her parts of the ground-water systen1; it m"'y in fac·t be unsuitable for the intended use.
However, develop1uen·t in or closely
adjacent to the areas o:i' natural dischurge would result in a minimum effect on the ground-\/ater system.
;
Drawing upon the illustrative co1uputations of the effects
of pumping discussed above, ~tre may consider briefly the effects
o:i' particular pumping patterns in Steptoo Valley.
For this pur~
pose, four areas are used to represent vurious segments of
Steptoe Valley;
(a) .\djacent to and east of Goshute Lake at tho
north end o:C the valley; (b) the area in and adjacent to the lowlands southeast of Cherry Creek; (c) the Duck creel~ fan and adja~
cent lowlands to the west and northwes-t; and {d) the lowland
between Ely and McGill. The gener11l assumptions used in computations for table S also serve as the reference for the discussion
30.
.....
_
,
of pumping effects for these areas; that is, T ~ 50,000, S =
0;15, 0 ~ 1,000 gpm per well, t = 10,000 days" Further, a well
field comprit>es ·either 16 wells on l:;-mile centers i.n a 4-squaremile are<'t for continuous pumping. or about 58 wells on 1.]-milEo
centers in a lL1-square-mile area for cyclic pumping· of 100 days
a year, A withdrawal of 25,000 acre~feet a year by either continu·ous or cyclic pumping also is assumed.
.•
;
The contj,nuous. pattern of pumping in areu. (a) would resul·t
in modifying the illustrat{ve e;,ampJ.e somewhat as foJ.J.ows.
As
the radius of influence expanded into fine-g·rained deposits and
volcanic bedrock, actual. values of transmissibility would be lower
than those used in the computation.
This influence would be
refl0cted in larger drawdowns, as suggested by table 9b, if the
annual quantity of w11ter withdrawn were maintained.
Drawdowns
after 10,000 days of pumping could be several tens of feet greater
than the 160 to 190 feet indicated in the illustrative eJralnples
for the idealized well field providing all water were withdrawn
from storage.
However, a large area of natural. discharg·e lies
adjacent to and west of the hypothetical well field,
As·the area
of pumping influence expanded into the area o:C natural discharge
an increasing amount of water would be salvaged,
In t.i.me, as
much as 40 percent of the amount of water pumped annually might
be supplied by salvaged water . . This is equivalent to reducing by
40 percent the draft on stored water, as suggested by table Sc,
and consequently drawdowns would be less than those in the illustrative example,
The two effects, that is, the lower value of
transmissibility and the salvage o:C natural dischargE>, would tend
to be mutually compensating' and it is probable that ·the drawdowns
in the well field would be g·enerally comparable to those given in
the illustrative example,
The radius of in{J.uence of a continuous pumping pattern in
area (a) could finally extend several miles sout,hward in the
lowland.
However, it is not likely that pumping in area (a) could
cause significant drawd~~n in area (b), about 20 miles away, before
the economic limits of pumping were reached in area (a)"
•
Area (b) is centrully located in an eJ<tensive lowland area of
n<J.tural ground-water discharge.
Accordingly, the effects of
salvag·e of:· natt,ral discharge would begin early in the pumping
period, although initial withdrawals from stox·age would be rE;quired
before the natural discharge could be diverted through .the wells.
Under the continuous pumping pattern as· discussed for area (a),
the proportion of pumped water derived from salvage could be s·o
percent or·more. Under the cyclic pumping pattern, the much
larger well field· and the area of significant drawdovm would be
distributed largely within the area of natural discharge,
If the
pumping season coincided with or immediately prooceded the seasonal
period of principal natural discharge, the proportion of salvaged
ground water would be greateJC than under the continuous pumping
pattern .
The ground water directly salvaged from natural evapotranspiration may be of inferior chemical quality for use.
The
31.
,.
~,···.
. ;_
'
.
suitability of the water for the intended use becomes increasingly
important as the proportion of salvaged watsr to total withdrawal
increascos,
I'urthe_r, if the water is used f:or irrigation within
the area of the well field, a part of the water spread on ·ths
fields will re·turn to the ground-water reservoir by deep infilt.ration,
This recycled water will have a higher concentration than
the initially pumped water,
In time, w<lter recycled in the well
field may supply a significant percentage of the amount of water
pumped. ·'•S ·this percentage increasss the pumped supply would
deteriorate further.
This should not negate the possibil.ity of
development for irrigLJ.tion, but i·t does indicate that possible
changes of chemical quality with time should be considered.
Area (c) occupies the lower part. of the Duck Creek fan
northwest of !VlcGill.
The adjacent lowland area is relatively we·t,
being· supplied with water fron1 the la:~:·ge spring area south from
steptoe, and from Steptoe Creek, Duck creek, and McGill Spring
through Bassett Lake.
Long-time pumping in area (c) would expand
ths area o£ influence to the lowland area of natural discharge by
evapotranspiration.
After the initial period of withdrawal from
storage, lo,..tering of water levels in the natural discharge area
would begin to salv<~ge some natural losses,
Further lowering of
water levels in the lowland area would induce recharge from overland runoff in the lowlands supplied by springs south of s·teptoe,
outflow from Bassett Lake, and perhaps from loc2l.l runoff.
If
significant drawdowns were achieved in the natural discharge area,
water obtained by salvage, induced recharge, and recycling could
provide a large fraction of the annual withdrawal.
If the cyclic
pattern of pumping w<~re used, the w·ater stored beneath the larger
area of the~ well field would supply most o:2 the water pumped for
many years bofore the salvaged water becawe a significant proportion of the total pumpage.
The radius of measurable pumping influence would be restricted on the northwest, west, and south by
the wet lo•!lland which finally would act as a recharge boundary to
the area of puu1ping"
on the east the bedrock which crops out in
the mountains would function as a partial barrier boundary due to
lower transmissibili·ty of the bedrock.
J:n area (d), between Ely and l'icGill, natural discharge of
ground water by evapotranspiration is sm<~ll compared t.o that in
area (c). Most of the water withdrawn under a continuous pumping
pa·ttern would be from storage, consolidated rocks of relatively
low .transmissibility are at the surface within about three mj.les
of the center of pumping, As the areu Of influence reached rocks
of lower transn1issibility, withdrawals could be maintained only by
increased drawdown.
The cyclic pattern of pumping with its much
larger well-field area, would obtuin a larger percentage of its
supply from stor<1ge beneath thE' well-fisld area
The intervals of
nonpumping would permit partial recovery of water l,evels within
the well field, by recharge frow underflow and runoff from the
southern or upgradient part of Steptoe Valley.
Finally, if the
<1nnual withdrawal were 15,000 acre-feet a year instead of the
25,000 acre-feet used in the computat:ion, the rate of drawdown
o
~•
would be reduced and pumping could be sustained over a longer
period of time.
The assumed conditions, computations, and their application
to selected parts of Steptoe Valley discussed above generally
indicate the response to pumping that might be expected, These
responses may be summarized as follows;
{1)
The early years of pumping would tend to have greater
drawdowns than indicated in the examples; because initial apparent
coefficients of storage would be less than those determined after
long-time periods of pumping;
(2)
The water pumped would be withdrawn largely from storage during the early years of pumping. As water levels were
drawn down in areas of natural discharge, an increasing proportion
of water pumped would be supplied by salvage of natural discharge.
Perhaps salvaged water would approach half of the total withdrawals
after 10 to 20 years of pumping;
(3)
The degree to which natural discharge of ground water
can be salvaged by pumping is dependent upon the effectiveness
with which pumping can lower water levels in the areas of natural
discharge,
Direct salvage of ground water by pumping in the area
of natural evapotranspiration discharge may not be entirely desirable if the water in the area of evapotranspiration is of poor
chemical quality;
(4}
Pumping centers adjacent to natural discharge areas with
the initial withdrawals largely from storage would minimi2e the
potential problem of chemical suitability of salvaged water and
permit a gradual increase in the proportion of salvaged water
should that prove satisfactory; otherwise there would be some
latitude to shift the pumping somewhat farther away to maintain
the quality;
(5) The pumping distribution used for illustration in
steptoe Valley is partly dictated by practical problems of development.
The use ot several centers of pumping would distribute
total withdrawal through the valley, consequently, drawdowns in
the well fields ,.,ould be less than if purnping were cencentrated
in a single field"
Using similar reasoning, wide spacing of wells
within centers of pumping would reduce the interference among
\~ells and help to keep drawdowns nominal; and,
(6)
The combined withdrawal of the illustrative examples
is 90,000 acre-feet a year. A reduction of 5,000 acre-feet a
year in the pumping from each center of pumping would result in a
withdrawal of about 70,000 acre-feet of water a year, equivalent
to the preliminary estimate of perennial yield.
The effect of a
lesser quantity of water withdrawn would be a proportional reduction of the drawdown from those of the examples.
However, the
33.
calculations suggest that pumping at an annual rate oi about
70,000 acre-feet could be ·maintained for several tens of years at
least if ·-pumping were distributed in several centers in the valley.
l?rovisional Budget for the Valley-Pill Hydrologic System
The budget for the valley-fill hydrologic system given in
table 10 is provisional in that it represents a general evaluation
of gross conditions. Time was not available in this investigation
to make direct determinations or field controlled estimates of
details of certain items of the budget, Thus, the amount of
precipitation, streamflow, and ground water consumptively used for
irrigated crops was not determined. Rather, these losses were included in the broader categories o:f evapotranspiration from different sources (budget items 4, 5, and 6, table 10), Excess water
in the mountains and alluvial apron moves downgradient toward the
lowland, either as runoff or infiltration into the ground-water
system. Thus, most of the water loss represented by each of tbe
outflow budget items occurs in the valley lowland, whether or not
the water is beneficially used.
'.-
--
~-i-~
.._·
-
The relatively large value for estimated subsurface inflow to
the ground-water reservoir (item 3, table 10) is supported indirectly by the fact that many large springs in the valley issue
from or adjacent to consolidated rocks. These springs occur both
in the mountains and in the valley lowland. They indicate that
the consolidated rocks, particularly the carbonate rocks are
capable of transmitting significant quantities of water.
In this
case it is inferred that usually most of the ground-water recharge
to the valley-fill system is supplied by water moving through the
consolidated rocks and into the valley fill below land surface.
The relative balance between the inflow and outflow items in
table 10 is due largely to the fact that several items are obtained by difference, in the absence of appropriate data. However,
though the items may be in error to a degree, it is believed that
the estimates provide a reasonable quantitative distribution of
the major elements of the hydrologic system. Thus, the estimates
provide an initial hydrologic framework from which the potential
for development may be evaluated.
/ .... :.;
__
•
·-' -.
>1.
•
Table 10. -- Provisional budget for valley-fill hydrologic system
Estimated average annual
amount of acre-feet
per year
INFLO\IV:
( 1) Precipitation on valley fill , , . . . . . .
(table 7 - equivalent of lower two zones)
{2) Runof£ from mountains
(table 5)
. .
.
~
~
....
52.0, 000
78,000
(3) Ground-water inflow across subsurface
contact of consolidated rock and valley
fill [item 6 below minus 24, 000 acrefeet of estimated recharge from runoff
to the valley-fill (see section on runoff)
and minus 5, 400 of recharge from precipitation on the valley fill (table 7,
recharge from lower two :.ones) 1
41' 000
639,000
OUTFLOW:
(4) Evapotranspiration from precipitation
on the valley fill (precipitation on
valley fill (item l above) minus
estimated (5, 400 ac~:e-feet) recharge
from precipitation on valley fill (table
7, recharge from lower two zones)j, .
(5) Evapotranspiration from runoff . . .
..
515,000
54,000
(see section on runoff)
(6) Evapotranspiration from ground water.
(table 8)
70,000
(7} Discharge through gap north of Currie.
1,000
IMBALANCE: Outflow greater than inflow
35.
640,000
1,000
•
CHEMICAL QUALITY
Twenty water samples were analyzed to provide information on
the chemical quality of water and for a generalized appraisal of
suitability of water for use. Table 11 lists the results of the
analyses.
According to the Salinity Laboratory Staff, U.S. Department
of Agriculture (1954, p. 69), the most significant factors with
regard to the chemical suitability of water for irrigation are
diss~lved-solids content, the relative proportion of sodium to
calcl-um and magnesium, and the concentration of elements and compounds that are toxic to plants. Dissolved-solids content commonly is expressed as "salinity hazard," and the relative proportion of sodium to calcium and magnesium as "alkali hazard."
The Salinity Laboratory Staff suggests that salinity and
alkali hazards should be given first consideration when appraising
the quality of irrigation water, then consideration should be given
to boron or other toxic elements and bicarbonate, any one of which
may change the quality rating.
,.'
Table 12 indicates the relative characteristics of the water
analyzed.
The reported values fo:t: RSC (residual sodium carbonate)
are well below the marginal values Of 1.25 to 2.5, which are reported to be unsuitable for irrigation (Eaton, 1950) •
The public water supplies for the principal communities
have been used for many years and apparently are generally acceptable.
However, the analyses indicate that the water is hard. Two
of the analyses indicate sulfate content above the 250 ppm value
which is the upper limit for that constituent suggested by the
u.s. Public Health Service (lg62).
1'7ater QUality and its Relation to the Ground-Water System
The concentration of dissolved chemical constituents generally tends to increase as water woves from areas of recharge to areas
of discharge. The concentration of individual constituents is
cont:t:olled in part by their :t:elative solubility and the kinds of
rock through which the water moves.
Temperatu:t:e and pressure of
the system also affect the degree to which the constituents are
dissolved in the water.
For the most part the samples of water
from steptoe Valley have low to moderate concentrations as indicated by the specific conductance.
•
sample 19/63-35bl has the highest values (1,710) for specific
conductance.
It is water flowing f:t:om Bassett Lake which is supplied to a considerable e~~tent by waste water from the McGill
operations. The increased concentration is largely due to increases in calciuw, magnesium, and sulfate. Other relatively
high specific conductance values were obtained for samples
16/63-lOal, and lOdl, which include waste v;ater from Ely.
36.
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,-,.·;11-io'{
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7-:>.'J-(,1,
l.a>; I~Ci
1.~~ l!ii!J~
5,9~0
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5 ,9J9
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lur
l.r.
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7 ,ooo
6,960
1'.'/~.:.::-lc
17 /lr'i-1 hr·
7H.h
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3-11,.]1; 1rr!:
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11/!.-1-lb
1-:.!':1-~~
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1-1
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(!£;:.1:1 Nyc:~)
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11ro·o:1
11
1167
4U/
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t-,'C'I:' 4U/
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17 /lrlo-~h1
Du~ ;,•ell
Dws, well
Du11, well
~.99S
ri"
.H
1"(.
,6
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!:!
lo?
11-r.lo
7-.'!11-!,-:
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•
RobC:l:t C~\O.Jt
Lattc•· DJ.y :;.::1nt~
N. K, ::;~i)dl:UC
16
121
6,100
Du;<, well
16
204
Nr::Vold;:o No1:thern
l'u~l11.'hcd
i'-:lll-lr'>
M
r-:w-1r~
1-:llHi~
I-~
l-~li-lr]
8
Du;<, well
',-111-lll
1.;:;:> 4G I
-.~
1'1:
23-102
Du~ we-ll
1963
TC
24-30
l'\>bli~hl'd ·..:~.~­
5 ,1381)
'167
Jo~<::ph
!\. '.-l.:.lcutt
LcRoy H;:o,u>1••8
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1964
108
1%:J
LJ4
87-10[1
92.-93
1~6:J
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93-9~
11u~ well
i'r1.1'r
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r.:1l.~ q'J.Jl"tl.'r
----·----··---~----------··-·
Some increas~ in concentration is indicated in water from
discharge areas, such as samples from wells 20/64-6al and
23/63-2bl. However, these concentrations are. not as high as would
ordinarily be expected in natural dischax·ge areas.
This probably
results from local recharge by season<tl flooding with fresh water
of the lowland in these areas and partial removal of some of the
salts accumulated at the surface during hot summer months .
•
37.
., '
•
USE OF Wl\TER
Present Use
-::
. ,,,'
••••
•'
T·Jater currently is uoed for public. supply, industry, agr i-, ·
culture, livestock, and recreation in Steptoe Valley. Information
for most wells is listed in tables 12 and 13,
Municipal supplies for Ely, East Ely, McGill, and Ruth ure
obtained from springs and vJells. Annual use may bG on the order
of 1, 200 acre- feet. Murry Springs, fed by wa'ter from carbonate
rocks, suppliGs most o£ the rGquirements o:~ Ely and East Ely. The
average flow of the springs is estimated to be 6 to 8 cfs, roughly
2,700 to 3,600 gallons per minute, but in recent years appears to
have been considerably less.
Some variation in flow is expected,
but well-controlled measurements are not easily made to ·verify the
full characteristics of the spring flow,
In recent years, wells
have been pumped during peak demand periods. 'l'he McGill municipal
supply is provided by a well in town.
Public-supply requirements ·
for the Ruth area have been met partly from springs several miles
to thto south and high on the west side of the Egan Range. lvater
from these springs is brought to the Ruth area by pipeline. Water
pumped ·from the underground mines in that area previously was us~'d
to some· extent for public supply or mining requiren1ents .
Mining and processing of copper ore is the principal industrial use of water in steptoe Valley, Water is supplied for plant
operations at McGill from Duck creek, McGill Springs, and water
recirculated from settling ponds and tailings disposal (Holmes,
1966, p. 17 and fig,· 10), An averi'ige of about 15 cfs is supplied
from the Duck Creek system, and 5 cfs (of 10 cfs flow.) is supplied
from McGill Springs, Thus, 20 cfs, or an average of about 14,500
acre-feet of. new water a year, may· ·be used in the overall operations at McGill. Additionally, much water is recirculated in the
plant. For example, about 131> cfs is recirculated through the
concentrator and·about 67 cfs is recirculated as cooled condensing
water.
·The Silver King Mines, Inc., north of Ely, uses the
Lackawanna Springs, discharge about 0.3 cfs, for milling operations,
Other industrial use of water is relatively s1nall and
largely depends on the municipal supply of Ely for its requirements.
Agricultural needs for water are supplied principally from
streams and springs. Most of this water .has been used to irrigate
meadow hay and pasture. However, irrigation of cultivated crops
is increasing.
Some ground water has been pumped for irrigation
for many years from a few scattered wells in the Ely-McGill part
, of the valley.
This pumpage probably has· not averaged more than
about 1,000 acre-.feet a year.
In recent years the number of wells
has increased and consequently pumpage has increased to about
3,000 acre-feet a year.
-· '--•
r-
~·.:
.
The release of Federal land under the Desert Land Act is
stimulating additional irrigation development south of Warm
Springs Station, and in the north part of the valley east of
Goshute Lake.
Potential use
Increased requirements for water in steptoe Valley can be
supplied by additional ground-water development, by increasing the
efficiency of use of water, and by reuse of water, The means by
which increased water requirements <>re met commonly <>re controlled
by the degree of need <>nd economics.
In Steptoe valley, the efficiency in the use of water will
increase as the need for w<>ter increases. Thus the need for water
to maintain plant operations at McGill led to an increase in the
efficiency and a substantial re-use of water to meet requirements,
Also, some of the waste w<>ter from the Ely public r<upply is reused
for irrigation,
However, much additional ground water can be developed, As
previously discussed, ground-water withdrawals <>t the rate of about
70,000 acre-feet a year could be maintained for several dec<>des;
however, the manner in which withdrawals were distributed in the
valley would be an i1nportant factor in determining how lcong that
amount of withdrawal could be maint<>ined,
If all the wa·ter were
withdrawn from a single localized area, W<>ter levels probably
would be lowered beyond economic limits within 10 ye<>rs, However,
if withdrawals were distributed in the four areas described in the
valley, withdrawals of 70,000 acre-feet a year probably could be
maintained for 50 years or moreo
•
•
••
'
.
DESIGNATION OF WELLS AND SPRINGS
'rhe numbering system for wells and springs ;Ls based on the
r·,ctangular subdivision of public lands, and in Nevada is referenced to the Mount Diablo base line and meridian. The nmnber
consists of three units; the first is the township north of the
base line; the second unit, separated from the first by a slant,
is the range east of the meridian; and the third unit, separated
from the second by a dash, designates the section number. The
section number is followed by one or two letters. 'l'he first letter designates the quarter section, the letters a, b, c, and d
respectively designate the northeast, northwest, southwest, and
southeast quarter sections.
In a similar manner, if a second letter is shown, it designates the quarter-quarter section location.
Following the letter, a number indicates the order in which the
well or spring was recorded within the quarter section. For example, well 19/63-12al is the first weli recorded in the northeast
quarter of sec. 12, T. 19 N,, R. 63 E,, Mount Diablo base line and
meridian.
•
Hell numbers on plate 1 only give the section number, quarter
section letter (some also g·ive quarter-quarter section letters),
and final number by the well symbol. The township and range numbers are shown along the margins of the valley area on plate 1.
t_I_.Q •
---
Table 13. ·--l:rillers'
lo"~ of s<>lectcd
............... ~--~
nesn
t.ll?r-:>::~
S..H'-~ ~;rav~l
GO
,._ .;
5
111:
sc
5
O;•
135
140
Silt
..
~'
1_1•/ 64-36~-- _2_kl
Soil
15/64··17bc
3
2.27
:~a.ncl1 -~o.•_
C···IJ
Silt
Gravel
Gravel. cemented
~
3
c.
;·
L' •
.<:
23?.
2(-lJ
Sand aHd gravel
31
2
265
Gravel~
l3
2T3
:lilt
Gravel
Gravel; c.ei-::.1enteU
Silt
Silt, cemented
Gravel
(
2CL!
Cement
Grave.l.
cem.e:n.teC~
Sand a11d zr.:1vsl
Saild ar1J. gr,r:l.vsl~ cem.enteJ
Sn.nd
ce.r::.c:~1.teC::.
an(~ p;ra.v(~.l
23CJ
25
5
sn
'•0
Top3oil
-Cr.~-ve.l,
••
l·~ard
,. cernente.t:;
Gravel .. ce:rn~-Llte.J~ little
t.Jhite clc:ty
Gravel,, cemcntet""J
Cl;;y, t<m _ r;ravel
Gru.vel ceme.l·~te.t.
Gravel, cenented ,. little
".-1hite clay
GravHl cerr.~utaU little
tai> clay
Gravel .a-::-!d tau clay
Gravel~
Gr~1.vel
Gr,-l.vel ~
ceme-;;:~te:d
a.1i.d. ta.n. cla.y
ce~1en tc=J
Gravel &nd tBn. clay
Limestone. very ~1ard
Clay,, tan r;rave 1
Gravel, ce.l!l.C:·nted
f..oc!t
Clay, t?n. gravel
Gravel, cemented little.
tan clay
Gr~tvel: c:emented ·' hard.,
tan clay
G1',:1vel" cemented
GrfJ.Vel, CG.T~lente.d · soft c.L:iy
Gravel.\ cem.e.nted
1
l:.5
,,
t,c
5()
1 ,,
73
75
93
15
103
23
2
?"
-~
7
13!1
137
34
3
171
?0
~;')3
·--36!;:;
5~;:
LJ
1''·'
21c5
263
2'11
1
2i,~2
.J ..1< ~
33
37!1
2f~
24
4:)6
l;3C
75
5,15
4l.
25
30
5'''·'
35
115
15
5
eo
130
135
5
11>0
5
25
145
170
175
195
·.".1
203
Hine dump fill
Silt
vall¢y loam
clilt and li~ht: zrcwel
10
5
15
li)
Gr~1vel_. waS~leJ
50
4
15
3:)
GO
84
iJtate Fish '-~B.-4- Gawg..Jd._q_rf!t!lis~A'?..ll
2oil
Gravel,. cemented
Sand and ?,ravol
3
72
3
75
21
96
3
77
UQ
;;arvey~J.i.,....'l.o;>Yflll
rl.oil
Gravel cemented
~and ,':lnci. 3r~.:vel
Clay
Se.nd and gravel
31·5
5
15
l_C./ G3·2db
"l,, ,...
25
130
l.!~)j53,:.2a
2391:.-i
eo
120
5
5
Lim.e.s tone
171,
')'
·~ \)
37
Silt and clay
Gravel
Gravel ond silt
Gravel
Gravel £end silt
1
25
30
Lend & Cut tle .f.o_,_
Silt
14}_(2:Qb.c_ _ }.L,H_
De£}th
!ater.~lL _________ li_c:._~0__ (f a€.JcL
1_5/64· 17ba
J
·•····
Cept'!'','.
(fe"tLif coet;)______
Sand ct>:menteJ :,
S ::'l..i."J.d. <'lll~J. ;:;re:.vel
Clay, srmJy
Saud un.J. gravel
~<ells
5
30
5
3
35
115
120
•
Tabl" 13. ·····Continued
'!'hi.~k-
T~1ic1~.-
'
.
.
nc.ss
i·'(ateri""a'"'l~-~-·--·-- (feet)
16/63-Ziicl
and s:ravel
16/63-2dc2
40
10
20
Gr-rtvel
_16/li3.-,<Jc:r.... Tam"'$ ''atsaro?.
SoilJ s.undy
Gravel
Gravel) ccmenteU
Gravel, cemented, small
streaks of -;:.,J;;,:lter
Hud and sand
s treal-:.:s of water
!~/63-llab
137
13
15
150
165
Gravel. c:~:mented.
Sand and gravel
cemented
Sand anci gravel
••
Clay End loam
Gravel fine; and Sj.nd
Clay
Gravel, fine, sand
Silt and $C"!.I1d
Saud and r~ravel
:iilt and sand
S~1nd and gravel
Silt D.nd sand.
Sand
Silt nnd sand
Sand
Silt and sand
SanJ and fine gravel
Clay on d. sand layers
Grnvel fil1e. sand
105
160
,16 I §.:Jo,-:),_!ta2__::L:J.1U .~ut Goodl_!l?-n
100
26C
3
57
10
1
Soil
Clay,, gray
Santl and gravel
Clay
Sand n.ncl. grrntel
Clay
Sand and grave I
Clay
A.-:111d M:nd r.:r.avel
Clay
Sand
Cby
30
~C)
100
120
5
1,s
10
Clay
15
Cl8.y and gruvel
Snnd and gravel (••ater)
C1uy
Sand'" gruveL. and HatrJ.r
15
55
70
85
~~ilt
5
35
5
4'.1
5
00
5
5
95
lJO
15
5
115
120
42.
(feet)J.t~et)
··-·--····
,,
60
70
--·-- -.
Dep tb
Goodrn;;.n
4''
55
29
Gr.avel J cemented
Silt
wanu' and r;ravel (~Cater)
Clay and gravel mi><ed
S:;1nd and gravel
(\1)1
65
17
10}.63-llL_ '!iJJJ_<;C/!._Q.qp..sl11'!'!:!
('-
lli 11 i
17
12
36
C, F. 3<1ain
Soil
Gr.;~\l'"el_.
210
137
Gravel, cemented. small
•.•
14')
lWJ
l<JO
J. t. Doutre
Sand
Cl<ly
)_'f+Jerbl _____ ,____
;l6/63-14ul
140
Sand
.S~'lnd
.!)er.Jtb
Ueet)
Jam<m "" Duvall
Sand
Clay
n~-~;.s
21
12
21
33
I,
37
11
48
37
85
1
86
"2
90
92
95
3
4
99
6
105
2
7
3
2
107
114
11
117
119
130
5
24
1:)
5
29
39
9
2
50
!~3
20
79
2
27
l
81
108
109
120
121
12C
11
1
7
Table 13.--Continued
Hate rid
J...§f63-15ba
City of JUy, NunidP.flJ.
\Inter
~ravel
J6/6J .. l6cc2
52
2
54
4
SE
1
59
6
l.
65
66
72
52
cemented
6
cemented
1
9
cemented
1
3
cemented
1
10
97
2
99
9
108
1
109
ce::aented
16
l
125
126
cemc.l'lted
27
2
153
cemented
15
cern<Onted
19
155
17;)
171
190
1
191
cemented
9
0l'"ave.l.: cemented
21
200
204
225
~ravel
, Gravel
. Gravel,
•
Gravel
-· 1 GraveL
Gravel
Gravel
Gravel
GraveL
Gravel
cemeuted
1
:16/63 16ccl
ness Depth
(feet) (!'_e_~
Di~J:Jict
Gravel, cemented
Gravel and ~later
Grave.l cemente~.
G·r.avel
Gravel, cemented
Gravel
9ravel
pravel,
Gravel
Gravel
Sravel
Gravel .
Gravel
Gravel;
Gravel
Thidt:.-~
Thick-··
ne<'s
Depth
(feet) (feet)
4
73
p'"}
'~
83
G6
87
City of Ely, tcunicipal
\:Later Dhtr!S'.I:.
Silt
GraveL cemented
Gravel ~-Ji tl1 '>lfatGr
Gravel; ceinentecl.
Gravel witl1 ~"later
Gravel.~ cemented
Gravel ,.,ith Pater
Gravel_, cemented
Gravel
Gravel. cemented
c.-avel
Gravel, cemel.1te.d
Gravel and sand
Silt
• . Grwel_ cemented., gravel,
-streaks of tJater
Silt
Gravel, loose
Grav-el~ cemented
Topsoil
C!Hy
Sand
Clay and gravel
Gravel
:J.6/64-6dc
p
/63·-1bc
4·1
20
60
1
()1
4
ss
5
70
h)
go
l.
El
5
·DG
'•
']0
8
0('1
.u
1
13
112
6
lUl
17
135
165
30'1
66
4
8
12
4
5
17
41
58
6
64
275
275
10
2G5
306
21
5
5
114
119
31
36
57
61
lt8
12'•
31
128
176
300
Robert C'W_<!,I:_
Topsoil, b ro.on
Grevel loose dry
Saud~ grClveL. cobhle:::
Clay -, b roun
Sa.nd Hncl gravel, cer1;ented
Gravel. looDO'
43.
20
4.,____,L_Jil01-1~
Soil s,ndy
Gravel
Clay and gravel
Cby and silt
Clay ,.,itt. gravel seams
9'l
20
46
}'!_,__]_,__ \Jri,;ht
Soil
Gravel
_l7/63-7ab
20
26
ilLU
Gt·i:vel. cemented
Gravel
Gravel, cemented
17 /64-Gbc
4·)
City of Ely, Nunicipal
I.Lat~r Distr:J,£t_
'•
24
.74
"
22
102
12
lll!
3
117
121
I,
..•
Tr!b lc l3.- -·Continued
Thid~-
-.
ness
--~~~'~'<~,t~e~.r~i~a=l~~~--~<.fcct)
17/64--·Sbal
ll.
tc.
1
Cemeut
Gravel
Clay
Cement
Cl&y
/64-19ca
cei.'~Lerrted
-Cetnen t
Gravel and sand
l
47
86
f'.7
39
1
11
OS:•
1
4
1
99
46
l
103
104
lYJ
151
152
18
204
184
1G6
.ss
22
37
21
lOi:l
L,
L,
83
1
93
13/63--36cc
9~~
2
6
2
100
106
108
7
115
1J
134
3
3
93
1_8/(.t,;3oc
J
cemented
90
1
2
2
7
5
3
1
')6
?0
105
110
ll3
114
4-4.
(>
6
14
10
24
19
43
64
8
21
55
6
119
5
130
'I,•
4
8
30
125
22
~
0
38
7
45
5
so
7
7
26
57
64
76
102
5
225
230
12
t!rs. Hat'"'l FielcJ..?_
Soil
Boulders: cemented
Sand and 3ravel
t.ioulders ce~ented
94
6
2
Pescio :Gros.
Soil
F.arcpan
Grr!vel c.oarse water
Silt lir,ht clay
2ilt' clay, and gravel mixed
Gruvel . meclium coarse ·Hater
Clay
Gravel coarse..' t-rater
Cl.'-Y
".:.-.an(l.., coarse WP..ter
92
5
~...;rater-~be.rJ.ring
Clay, sa.nO. yellow
Gravel and sand.> water ..bearing
sand and gravel; miJ<cd uith
clay, wat:er··bearing
Clay, sand; yellou
Clay, sandy
Gravel) 'f.rlate.r·~bearing
Clay
"'
1
1
32
2
Albert Rome,Q_
Clay
Gravel>
I:arl :l. \iilliall)S_
Soil
Sand and gravel
Grnvel
Ce:tnent
Gravel
Cement
r:ravel
Cement
Gravel
•
5
46
Leleoy :·:an""'f!g_
Soil
Sand and gravel
Gravel
Cement
Gravel
Cement
Gravel
_:1,_7 /64-- ):Jhc!
5
41
22
. • Gravel, loose '·•ater-bearing
17 /64--·30ba
lH/63- 36al.
J. R. Valcutt.
Gravely soil
Gravel.,
Hatert_'!],_ ___ ~-------_0-'"'-"-~-tl--
(fe~t)
Sur.druc\_
Soil
Sand and gravel., c:emel.1ted
Cr<>vel
S<md and. gravel ceraented
Gravel
Clny
Gravel
Sand and cravel, cemented
Gravel
Clay
p
TL.iclc--·
ness Depth
Depth
5
40
270
40
310
.•
Table !).·-,.Continued
:
•
Thickness
ljg~el."bl
(£eg}
_20/64 -20a aoel Hilliams . Jr.
Topsoil
2
Uarrlpan
4
;clay and gravel
14
Gravel, cemented
4
Clay anfi grav(~.l
23
Gravel
2
Clay and gravel
1
,Gravel
2
Clay and 8ravel
5
Clay
3
Gravel, hard
2
Clay and gravel
6
Gravel, some clay
2
Clay and gravel (lots of clay) 17
Gravel
4
clay and gravel layers
9
Clay
2
Clay and gravel
3
Clay
2
Clay and Gravel
6
pay
10
Gravel
2
Clay and gravel
6
crave!
2
Clay and gravel
2
Clay
7
Gravel
'2•
pay al"id gravel
Gravel
Clay and gravel
21/63-35c
3
7
30
5
10
Boulders
•
(fe~:tl
Gravel fine
Clay and gravel,
Gravel, medium
Clny and gruvel,
Gravel~ snrJ.dy
Gravel:~ fine
Clay and gravel,
Gravel, fine
Gravel_. sandy
Gravel .. medi=
GraveL. fine
Clay and gravel,
Gravel, fine
Clay and gravel
5
fine
fine
2
6
fine
49
50
52
57
60
62
102
105
107
113
fine
6
45
3
12
GO
s
48
65
ll. Coats
Sand.~ yellm•
Cl3y, hlue uith gravel and
clay layers
Clay, lake bottOl'l
15
15
430
445
15
460
Silver State Constructio.!!__£9_,_
.25/65-31a
Sand and gravel, cemented
Gravel and water
Clay, sandy
?6/64-·28<11
50
50
2
168
52
220
Cordano Et·os.
Soil
125
131
133
Sand." gravel_; water
27
3
27
30
Clay
15
45
2
47
75
76
135
11;2
11!6
148
151
153
30
35
45
50
70
llS
5
12')
15Q
155
25
6
3')
123
15
20
10
15
15
J.
Z_5/65- Sbl
6G
100
5
5
5
Clay
5arid. and gravel
Cloy
Sand and sravel
24
47
70
87
91
100
Ken Boi:l.rton
Soil
20
20
15
15
30
Naterial
24l\,4--16c
P.ustin Flint
Gravel.
fine
'
.
Cob h lcs tone
¢tny and sravel
Thick,..
ness Depth
(feet) Cfeet)
Depth
R5
160
165
185
195
Sand~
gravel~
water
28
Clay
s ...nd and gravel
Clay
Sand and gravel
CL'Y
1
22
98
2
150
100
Clay
10
S.::md and gravel
SCJ
10
60
,~§£64•m23tl2
76/55-15
Cord,.no .e:ros.
\!illiam
Coop~r
Surfaca deposits
Gravel
Quicksand
Clay, yellow, and s.rave:l
),£165··32"1
.,
h.
225
251)
45.
10
20
30
140
200
15
15
15
30
230
260
lO
30
60
ll. Coat'!.
Clay"~ sanely
Clay,. ye11o«
Clay, blue with gravel end
clay layers
210
250
••
REFEEENCES CITED
Bauer, H. L., Jr., Coo;-,er, J. J., and Br.,itrick, Ic A., 1960, Porphyry
copper deposits in the Robinson .Mining Di~trict, Vvhite Pine County,
Nevada, in Geology of east central Nevada.: I11termountain Assoc.
Petroleu~ Geologists; ll th Ann. Field Conf., 1960 Guid.,book,
p. 220-228.
Clark, V·i. 0. , and Riddell, C. W .. , 1920, Exploratory drilling for watc>·
and use of ground water for irrigation in Steptoe Valley, Nevada:
U.S, Geol. Sm·vey, V.'ater-Supply I'"aper 467, 70 p.
Eakin, T. E., and othe_rs, 1951, Contributions to the hydrology of easte>·n
Nevada: Nevada State Engineer Wate>· Resources Bull. 12, 171 p.
Eaton, F. M., 1950, Sigai£icance of carbonates ia irrigation waters:
Sci.'
V,
Soil
69, p. 123-133.
Hardman, George, and ivlason, H, G., 19<19, h·rigated b11ds ln Nevada:
Nevada U•>iv, Agr. Expt. Sta. Bull., no, 183, 57 p.
Barlow, George, 195~, Su·atigraphy and structure of the Spruce Mountain
area, Elko County, Nev<tcia: Washington Univ. ma,.te1·' s thesis,
unpublished.
I-IolrC~es,
G, H., Jr. 1966, Water requi1·ements and uses in Nevada mine1·al
industries: U.S. Bur. Mines, Info. Circ. 82.88.
Houston, Clyde, 19 50, Consumptive use of irrigation wate1' by cr<>ps in
Nevada; Univ. Nevada Agd. Expt. Sta. and Liv. Irrigation and
'Nate1· C:onserv., Soil Conserv. Service, U.S. Dept. Agriculture
Bull, lSS, 27 p.
Kellogg, H. E., 1963, Paleozoic stratigraphy "f the Souther11 Egan Range,
Nevada: Geol, Soc. Ameri<:<t Bull., v. 74, p. 685-708.
Snelson, Sigmund, 1955, The geology of the southern Pequop Ivlountains,
Elko County, Nevada: Washington Univ. master's thesis, unpublished.
Tagg, K. M.. , and others, compilers, 19C>J•, Geologic m<tp of Nev,.da, 1n
Mineral and W<'ter resource" of Nevada: Nevada Pju1·. Mines
Bull, 65, fig. 3 opj). p. 12.
Thomas, H. E., 19:'>3; Effects of drought in basins of interior drainage:
U, S. Geol. Survey Prof. Pa 1)er 372.-E, 50 p.
•
U.S. Department of Agriculture, 1954, Diagnosis and improvement of
saline and alkali soils: Agriculture Handbook no. 60, 160 p.
U.S, Public Health Sc1·vice, 1962, Public Health Service drinking wate1·
standards 1962: Public Health Service Pub. no, 956, 61 p.
Young, J. C., 1960, StructLtre and stratigraphy in no1·th-central Schell
Creek Range, i11 Geology of east-centr«l Ncv«d<<: Inten'nountai11
Asr,oc, Petroleur::1 Geologists, llth Ann. }''ield Con£., 1960 Guidebook, p. 158-172.
Woodw,u·d, L. A,, 196'1, Structural geology of central northern ·Egan R"nge,
Nevada: An1erican Assoc. PetrolcLun Geologists .Bnll., v~ 4U;~
no. l, p. 22-39 .
•
.. ~-
•••
'~
~
'
i
47.
NEVADA
ArQa!5
c;:lcscrib1~d
prt~vio(JS r~ports
I
in
Q1
the Ground-Water
Reconnaissance Series
Are~:~ d~~~;er!bed
In this report
50ii;;iiiiii~25~=="liiiiiiiiiii2~5~=:350 Miles
•
Figure 2 .-Areas in NP.vada described in previous reports of the Water Resources
Reconnuiss21nce Sarit:~s i:ind the area described in this report
•.
LIST OF PUBLISHED REPORTS IN THE
..,"t
WATER RESOURCES - RECONNAISSANCE SERIES
Reeort
No.
l
2
10
11
12
Newark (out of print)
Pine (out of erint)
Long (out of print)
Pine Forest (out of print)
Imlay a rea (out of print)
Diamond (out of print)
Desert
lndependen<:e
Gabbs
Sartcobatus and Oa.sis
Hualapai Flat
Ralston and Stonecabin
13
14
An~1argosa
3
4
,.
~
&
7
8
9
'.,
15
lS
17
18
20
21
22
23
..
2'.\
-·
25
2&
Report
No,
Valley
27
28
29
30
31
3Z
33
34
c,ve
.Long
Surprise
1vLJ.ssacre .Lake Coleman
35
lviosquito
Guano
Bcm1der
Dry Lake and Dela.mar
Duck Lake
Garden and Coa.l
lvliddle Reese and Antelope
Black Rock De: s"rt
Granite Basin
High Rock L;:;ke
Summit Lake
Pahranagat and Pahrr><.:
Pueblo
Continental Lake
Virgin
Gridley .Lake
Dixie
Stingaree
..F"'rl.irview
Fleas ant
East gate
Cow kick
.Lake
Coyote Spring
E"'ne Spring
Iv~uddy Hive:r Springs
Edwards Creek·
48.
Lower Meadow
P~ttterson
.S 0oring {neal· Panacii)
P~naca
Clover
Eagle
Dry
Smith Creek and !one
G1·ass (near Viinncmucca)
jl/.onitor, 1-l.ntelope, iirld Eobeh
U;_Jpe1· Reese
Lovelock
Spring (neax Ely) {out of print)
Snatw {o11t of print)
Hamlin
Antelope
•::leas ant
Ferguson Dt:~sext
Huntington {ont of print)
Di:rie Flat
'~/Thitesage_
37
38
39
40
41
42
Valley
Fl.at
Eldorado - Piute v,,lley
{Nevada ,J.nd California)
Grass and .Carico Lake
{Lander and Eu1·eka Counties)
Hot Creek
Little Smoky
Little Fish Lake
Eagle Valley
{Ormsby County)·
'"-'all<er .L«ke Axea
{ )viineral, .Lyon, Churchill Counties)
Washoe V«lley
Steptoe Valley
('Hhite Fine alld Elko Counties)
.U.S. DEPARTM EN T OF THE INTERIOR
GEO LO GICA L SUR VEY
STATE C•F NEVADA
DEPARTMENT OF CONSERVAliON AND NA TUR AL RESOURCES
WA TER RESOURCES
RECO NN A ISSANCE REPORT 42 PLATE 1
f
\
1'
;>
{<?"
&"<:
_(
.,J'il'
"'"'<,_
<0\)
.
..
'I"'J
j./
(
,.
I
'
I
'r·
'
o/
'
I
EXPLANATION
/
Un conso lid ated and partly conso lidated deposits
Qyl
-1
Younger va ll ey fill
Principally Recent unconsolidated slit, sand, and gravel deposited along drainage channel s and, north of twp. 22 N, lac ustrin e clay, slit,
and sand; lo ca lly Includes dune deposits and the large tai lings dump west of McGill. Commonly severa l tens of feet thick or less , but
maximum thickness may be about 150 feE!t. Sand and gravel units yie ld water free ly where saturated
>0::
<(
z
0::
w
f--
<(
::l
0
Older valley fill
Unconsol idated to partly conso lid ated si lt, sand, and grave l su baeria l and water-laid deposits undifferentiated; general ly alluvia l fan
detritus at or nea r surface but extensive silt and clay at depth. Sand and gravel encountered in the upper few hu ndred feet yield
water freely to we ll s. Fine grain deposits contain a large vo lum e of water In sto rag e
Consolidated rocks
Vo lcanic and sed imentary rocks
Largely vo lcanic roc ks but Includes consolidated sedimentary deposits and, near Currie Mesozoic rocks; generally volcanic rocks yield
water slow ly to well s but supp ly water for numerous small springs and some streams In the mountains
0
Intru sive rocks
Genera ll y granitic rocks; limited capacity to store and transmit water In near-surface weathered zones or fractures
u
6
N
Carbonate rocks
,,,
0
w
Principally ca rbonate rock s but inc l udes some clastic and oth er undifferentiated rocks; carbonate rocks supp ly water to Murry and McGill
springs and other large sp rings, locally transmi t substantial quantities of water through fractures and solution opening s
-'
<(
0.
Clastic rocks
Upp er Precambrian through Lower Cambria n quartzose sedimentary rocks; fractured parts transm it some water principally within a few
hundred feet of land s urface In the mountains and supplies much of the late season How to tributaries of Duck Creek
Geologic contact
,,
Drainage divide
D
Princ ip al area of phreatophytes and natura l discharge of ground water; depth to water generally less than 20 feet
Water-level contour
Shows app roximate altitude of water level ; dash ed where approximate ly located; contour inte rval, 100 feet; datum is mean sea lev el
Well and lo cation number
Spring
Singl e line across channel Indicates point of measurement; doubl e lin e, indicates point of collection of water sample
Sca le 1 :250,000
i2!0!0§;;;;;;;j~~2§;;;;;l3~"l4iioo-"5~~6i;;;;;;;;;7~~B-;;;j9~~10.
MII es
Contour Interval, 200 feet; datum is mean sea leve l
1967
PLATE 1.-GENERALIZED HYDROGEOLOGIC MAP OF STEPTOE VALLEY, NEVADA
Base from: Army Map Series 1:250,000 series Elko (1962), Ely (1963), a·nd lu nd (1963)
Consolidated rock geology after Tagg and others (1964); unconsolidated
geology by J. L. Hughes (1965): Hydrology by T . E. Eakin and J . L. Hughes (1965)