Recharge and Discharge Areas for the Principal Basin-Fill Aquifer, Curlew Valley, Box Elder County, Utah

RECHARGE AND DISCHARGE AREAS FOR THE PRINCIPAL BASIN-FILL AQUIFER, CURLEW VALLEY, BOX ELDER COUNTY, UTAH

by Stefan M. Kirby and Mike Lowe, Utah Geological Survey and Jason L. Kneedy, Chesapeake Energy

113°0'0"W 112°45'0"W

CASSIA COUNTY ONEIDA COUNTY IDAHO Kelton Pass BOX ELDER COUNTY 42°0'0"N Curlew UTAH 84 113°15'0"W 42 Junction 30 Snowville

Pilot Spring

RAFTR RIVER A MOUNTM F O T Coyote Spring U R N IV TAINSA E IN R S

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C p e

D Study Area Kelton 41°45'0"N Boundary Locomotive Springs

UTAH N

0 5 10

Scale in Miles

ISBN 1-55791-737-X

MAP 218 UTAH GEOLOGICAL SURVEY a division of Utah Department of Natural Resources 2005 STATE OF UTAH Jon Huntsman, Jr., Governor

DEPARTMENT OF NATURAL RESOURCES Michael Styler, Executive Director

UTAH GEOLOGICAL SURVEY Richard G. Allis, Director

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Printed on recycled paper 1/05 CONTENTS ABSTRACT ...... 1 INTRODUCTION ...... 1 Background ...... 1 Purpose and Scope ...... 1 Setting ...... 2 Physiography and Drainage ...... 2 Climate ...... 2 Land Use ...... 3 Previous Studies ...... 3 METHODS ...... 3 GEOLOGY ...... 5 Bedrock ...... 5 Unconsolidated Sediments ...... 6 GROUND WATER ...... 7 Overview ...... 7 Fractured Bedrock Aquifers ...... 8 Aquifer Characteristics ...... 8 Recharge and Discharge ...... 8 Water Quality ...... 8 Unconsolidated Basin-Fill Aquifer ...... 8 Aquifer Characteristics ...... 8 Recharge and Discharge Areas ...... 8 Water Quality ...... 9 Potential for Water-Quality Degradation ...... 9 SUMMARY AND CONCLUSIONS ...... 9 ACKNOWLEDGMENTS ...... 9 REFERENCES ...... 10 APPENDIX ...... 11

FIGURES Figure 1. Curlew Valley study area, Utah ...... 2 Figure 2. Relative water levels in wells in recharge and discharge areas ...... 4 Figure 3. Numbering system for wells in Utah ...... 5 Figure 4. Simplified geology of Curlew Valley ...... 6 Figure 5. Recharge block diagram ...... 7

TABLES Table A. Records of water wells ...... 12 RECHARGE AND DISCHARGE AREAS FOR THE PRINCIPAL BASIN-FILL AQUIFER, CURLEW VALLEY, BOX ELDER COUNTY, UTAH

by Stefan M. Kirby and Mike Lowe, Utah Geolgocial Survey and Jason L. Kneedy, Chesapeake Energy

ABSTRACT rate of movement. Because contaminants can readily enter an aquifer system in recharge areas, management The primary source of drinking and irrigation of potential contaminant sources in these areas water in Curlew Valley is ground water from the prin- deserves special attention to protect ground-water cipal basin-fill aquifer. We mapped recharge and dis- quality. Ground-water recharge-area mapping delin- charge areas for the principal aquifer to provide a tool eates these vulnerable areas. for management of potential contaminant sources to Ground-water recharge-area maps typically show: help protect ground-water quality. (1) primary recharge areas, (2) secondary recharge Curlew Valley is a roughly Y-shaped, north-south- areas, and (3) discharge areas (Anderson and others, trending valley that extends from Great Salt Lake in 1994; Lowe and Snyder, 1996). Primary recharge Utah in the south to the Sublett Range and Stone Hills areas, commonly along bedrock uplands and adjoining in Idaho in the north; this report covers only the broad portions of valley fill, do not contain thick, continuous, southern arm of the valley in Utah. The Utah portion fine-grained layers and have a downward ground- of Curlew Valley is bounded on the east by the north- water gradient. Secondary recharge areas, commonly east-trending Hansel Mountains and on the west by the valley benches, have fine-grained layers thicker than Raft River Mountains. The principal basin-fill aquifer 20 feet (6 m) and downward ground-water gradients. of Curlew Valley consists of interbedded alluvial-fan, Ground-water discharge areas are generally in valley lacustrine, and volcanic deposits. Wildcat Hills, Cedar lowlands. Discharge areas for unconfined aquifers are Hill, the mountains surrounding Curlew Valley, and the where the water table intersects the ground surface upper parts of alluvial fans along the margins of these causing springs or seeps. Discharge areas for confined uplands, make up the primary recharge areas. The aquifers are where the ground-water gradient is northern margin of Great Salt Lake is the principal dis- upward and water is discharging to a shallow uncon- charge area. Water quality is generally moderate with fined aquifer above the upper confining bed, or to a total-dissolved-solids values at or above 2000 mg/L spring or flowing well. Extent of recharge and dis- recorded across much of Curlew Valley. charge areas for an aquifer may vary both seasonally and annually due to changes in the amount of precipitation. INTRODUCTION Purpose and Scope Background The purpose of this study is to help state and local The principal basin-fill aquifer is the most impor- government officials and local residents protect the tant source of both drinking and irrigation water in the quality of ground water in Curlew Valley by delineat- Utah portion of Curlew Valley. Recharge to this un- ing areas where ground-water aquifers are vulnerable consolidated aquifer is primarily from precipitation in to contamination from land-surface sources of pollu- mountainous areas (Baker, 1974), including infiltration tion. The scope of work included a literature review of runoff from intermittent streams along the valley and analyses of drillers’ logs of water wells to define margins. Recharge areas are typically underlain by hydrogeologic conditions in Curlew Valley. Relevant fractured rock and/or coarse-grained sediment with rel- information was recorded from each water-well log atively little ability to inhibit infiltration of contaminat- (appendix) and well locations were plotted on ed water. Ground-water flow in recharge areas has a 1:24,000-scale base maps. Generalized recharge- and significant downward component and relatively fast discharge-area boundaries were then delineated and 2 Utah Geological Survey entered, along with well locations, into a geographic The valley floor ranges in elevation from 4200 feet information system database. (1300 m) along the shore of Great Salt Lake to about 4800 feet (1460 m) along the foothills of the adjoining Setting mountain ranges. The generally uniform north to south slope of the valley floor is interrupted in the southern Curlew Valley is a roughly Y-shaped, north-south- part of the valley by a line of low hills and knolls, trending valley that extends from Great Salt Lake in including Cedar Hill and Wildcat Hills (figure 1) northern Utah in the south to the Sublett Range and (Bolke and Price, 1969). Stone Hills in southern Idaho. The valley covers an Indian Creek and Deep Creek are the two largest area of about 1200 square miles between latitude streams in the Utah portion of Curlew Valley (figure 1) 40°41′ and 42°30′ north, and longitude 112°30′ and (Baker, 1974). Except during rare flood episodes, both 113°20′ west (3100 km2) (figure 1). This report covers streams dry completely before reaching Great Salt only the broad southern arm of the valley in Utah, with Lake (Bolke and Price, 1969). All other drainages are emphasis on the approximately 550 square-mile (1420 intermittent or ephemeral (Baker, 1974). km2) valley floor. Climate Physiography and Drainage The climate of Curlew Valley, as measured at The Curlew Valley drainage basin is in the Basin Snowville, is semi-arid with moderately cold winters and Range physiographic province (Stokes, 1977). and warm, dry summers (Bolke and Price, 1969). The Utah portion of Curlew Valley is bounded on the Temperatures in the valley range from a maximum of east by the northeast-trending Hansel Mountains and about 90°F (32°C) to a minimum of about 10°F on the west by the east-west-trending Raft River (-12°C); the maximum daily temperature variation is Mountains, with peaks in the drainage basin reaching greatest in the summer when fluctuations can be as elevations of 6300 to 9000 feet (1900 to 2700 m) above much as 40°F (22°C) (Ashcroft and others, 1992). sea level (Bolke and Price, 1969). Mean annual temperature was 45.4°F (7°C) from 1948

113°0'0"W 112°45'0"W

CASSIA COUNTY ONEIDA COUNTY IDAHO Kelton Pass BOX ELDER COUNTY 42°0'0"N Curlew UTAH 84 113°15'0"W 4422 Junction 30 Snowville

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UTAH N

Figure 1. Curlew Valley study area, Utah. Background is 0 5 10 false color Landsat image available from the Intermountain Region Digital Image Archive Center (2005). Scale in Miles Recharge and discharge areas for the principal basin-fill aquifer, Curlew Valley, Box Elder County, Utah 3 to 1991 (Ashcroft and others, 1992). The growing sea- ed by Riding and Quilter (2004). Atkin (1998) sum- son (the number of consecutive frost-free days) in marized ground-water quality conditions. Oaks (2004) Curlew Valley averages 99 days, with a low of 41 and examined recharge to Locomotive Springs and basin- a high of 198 days (Ashcroft and others, 1992). wide ground-water flow and quality. The U.S. Geolog- The valley averages less than 8 inches (20 cm) of ical Survey has monitored ground-water levels and precipitation annually, the higher mountain ranges chemistry at several wells in Curlew Valley since the receive up to 35 inches (89 cm) (Bolke and Price, early 1960s (Burden and others, 2003). 1969), mostly as snow during the winter. At Snow- ville, mean annual precipitation was 12.8 inches (32.5 cm) and mean annual evapotranspiration was 46.2 METHODS inches (117.3 cm) from 1948 to 1991 (Ashcroft and others, 1992). Precipitation by snowfall is common in In this study, we used the methods of Anderson and Curlew Valley from November through April, but others (1994) as modified by Snyder and Lowe (1998) snowstorms are not uncommon as late as May (Ash- for identifying confining layers, and delineating croft, 1992). recharge and discharge areas for basin-fill aquifers; much of the text in this section is from Snyder and Land Use Lowe (1998). To delineate recharge and discharge areas, we evaluated both the principal aquifer and local Curlew Valley is sparsely populated, but, like most overlying shallow unconfined aquifers (figure 2). The areas in Utah, is experiencing an increase in popula- principal aquifer is the most important source of tion. The population of Snowville increased to 251 by ground water, and may be confined or unconfined. The 1990 and 277 by 2000 (Demographic and Economic principal aquifer begins at the mountain front along the Analysis Section, 2000). The population of Snowville valley margins where coarse-grained alluvial-fan and is projected to continue to increase 2% annually over nearshore lacustrine sediments predominate and the next 30 years; by 2030 the population of Snowville ground water is generally unconfined. Away from is expected to be 497 (Demographic and Economic bedrock exposures, fine-grained silt and clay may form Analysis Section, 2000). The population may also confining layers above and within the principal aquifer. increase slightly in outlying parts of Curlew Valley Water in sediments above the upper confining layer is (Demographic and Economic Analysis Section, 2000). in a shallow unconfined aquifer. Shallow unconfined The economy is dominated by agriculture, mainly aquifers are generally not an important source of drink- cultivation of irrigated crops and livestock grazing ing water. (Bolke and Price, 1969). Raising livestock is the pre- We used drillers’ logs of water wells to delineate dominant enterprise, with most cultivated land devoted primary and secondary recharge areas and discharge to raising hay and small grains for feed (Baker, 1974). areas, based on the presence or absence of confining Cultivated land is irrigated mostly by water wells, a layers and relative water levels in the principal and practice that began in the Kelton area in 1953 (Bolke shallow unconfined aquifers. Well-log information is and Price, 1969). Surface water is locally used for irri- shown in the appendix. The use of drillers’ logs re- gation along Deep Creek from Snowville northward quires careful interpretation because of the variable (Baker, 1974) and near the old town of Kelton through quality of the logs. Correlation of geology from water- the diversion of Indian Creek (Baker, 1974). Dry well logs is difficult because lithologic descriptions are farming of small grains is common at higher altitudes, generalized and commonly inconsistent among various mainly where average annual precipitation exceeds 16 drillers. The use of water-level data from water-well inches (40 cm) (Baker, 1974). logs is also problematic because levels in the shallow unconfined aquifer are commonly not recorded, and Previous Studies because water levels were measured during different seasons and years. Previous studies of ground-water conditions in the Confining layers are defined as any fine-grained Utah portion of Curlew Valley include Carpenter (clay and/or silt) layer thicker than 20 feet (6 m) (1913), Bolke and Price (1969), Baker (1974), and (Anderson and others, 1994). Some logs note both Atkin (1998). Baker (1974) estimated basin-fill thick- clay and sand in the same depth interval, without giv- ness from gravity surveys by Cook and others (1964) ing relative percentages; these are not classified as and Peterson (1974). Geologic mapping by Hurlow confining layers (Anderson and others, 1994). If both (2004) covered the entire study area. Davis (1984) clay and sand are checked and the word "sandy" is examined the low-temperature geothermal potential written in the remarks column, then the layer is for Curlew Valley and adjacent areas. Ground-water- assumed to be a primarily clay confining layer (Ander- quality data, periodically collected since 1996 by the son and others, 1994). Sometimes a driller will mark Utah Department of Agriculture and Food, are present- clay and gravel, cobbles, or boulders; these units also 4 Utah Geological Survey are not classified as confining layers, although in parts Ground-water discharge areas are at lower eleva- of Curlew Valley, they may behave as confining layers. tions than recharge areas. In discharge areas, the water The primary recharge areas for the principal in confined aquifers discharges to the land surface or to aquifer are the bedrock uplands surrounding and with- a shallow unconfined aquifer (figure 2). For this to in the valley, and basin fill lacking thick clay layers, happen, the hydraulic head in the principal aquifer generally along valley margins (figure 2). Ground- must be higher than the water table in the shallow water flow in primary recharge areas has a significant unconfined aquifer. Otherwise, downward pressure downward component. If present, secondary recharge from the shallow aquifer will exceed the upward pres- areas begin where clay layers are thicker than 20 feet sure from the confined aquifer, creating a net down- (6 m) and the hydraulic gradient is downward. Areas ward hydraulic gradient indicative of secondary of secondary recharge extend toward the valley center recharge areas. Flowing (artesian) wells are marked on until the hydraulic gradient is upward (figure 2). The drillers’ logs and commonly shown on U.S. Geological hydraulic gradient is upward when the potentiometric Survey 7.5′ quadrangle maps. Wells with potentiomet- surface of the principal aquifer is higher than the water ric surfaces above the top of the confining layer can be table in the shallow unconfined aquifer (Anderson and identified from water-well logs. Surface water, others, 1994). Water-level data for the shallow uncon- springs, or phreatophytic plants (wetlands) can also fined aquifer are not common, but are recorded on indicate ground-water discharge. In some instances, some water-well logs. Where confining layers extend however, this discharge may be from a shallow uncon- to the ground surface, secondary recharge is mapped fined aquifer. It is necessary to understand the topog- when the potentiometric surface in the principal aqui- raphy, surficial geology, and ground-water hydrology fer is below the ground surface. before using these wetlands to map discharge from the

PRIMARY RECHARGE AREA

Explanation

Water level in well valley fill aquifer Well with perforated intervals

Direction of ground-water frracturedactured bedrockbedrock flow

SECONDARY RECHARGE AREA

confining layer shallow aquifer

confining layer principal aquifer

principal aquifer

DISCHARGE AREAS, CONFINED AQUIFER

flowing well

shallow aquifer confining layer

confining layer

principal aquifer

Figure 2. Relative water levels in wells in recharge and discharge areas (modified from Snyder and Lowe, 1998). Recharge and discharge areas for the principal basin-fill aquifer, Curlew Valley, Box Elder County, Utah 5 principal aquifer. southeastern quarter of the northeastern quarter of sec- 1 1 We generally did not map small discharge areas tion 9, Township 14 North, Range 8 West (NW ⁄4SE ⁄4 1 defined by single well logs where surrounded com- NE ⁄4 section 9, T. 14 S., R. 8. W.) Salt Lake Base Line pletely by secondary recharge. Contaminants entering and Meridian. the aquifer system above these wells may be less likely to affect the principal aquifer than in the surrounding areas of secondary recharge. GEOLOGY The numbering system for wells in this study is based on the U.S. government cadastral land-survey Bedrock system that divides Utah into four quadrants (A-D) separated by the Salt Lake Base Line and Meridian Bedrock in the Curlew Valley records a varied and (figure 3). The study area is entirely within the north- complex tectonic history of episodic compression and west quadrant (B). The wells are numbered with this extension. Basin-margin mountain ranges including quadrant letter B, followed by township and range, the Hansel Mountains and the eastern Raft River enclosed in parentheses. The next set of characters Mountains consist primarily of Paleozoic- through indicates the section, quarter section, quarter-quarter Mesozoic-age carbonate and clastic rocks cut and fold- section, and quarter-quarter-quarter section designated ed by mainly west-directed thrust faults of the Creta- by letters a through d, indicating the northeastern, ceous through early Tertiary Sevier fold and thrust belt northwestern, southwestern, and southeastern quad- (figure 4) (Miller and others, 1983; Allmendinger and rants, respectively. A number after the hyphen corre- others, 1984). Syn- and post-thrusting extension, pri- sponds to an individual well within a quarter-quarter- marily during the Tertiary, along low- and high-angle quarter section. For example, the well (B-14-8) 9adb- normal faults further deformed existing bedrock, form- 1 would be the first well in the northwest quarter of the ing basins that filled with locally derived clastics and

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Figure 3. Numbering system for wells in Utah (see text for additional explanation). 6 Utah Geological Survey volcanic deposits (Miller and others, 1983; Miller and for the basin fill flooring much of the study area and others, 1995). Quaternary-age tectonism is locally comprising the principal aquifer (Doelling and others, characterized by occasional seismic slip on high-angle 1980). normal faults, periodic volcanism, and continued sub- sidence and filling of existing basins (Miller and oth- Unconsolidated Sediments ers, 1995). Paleozoic-age carbonates and younger volcanic Unconsolidated basin fill consists primarily of units comprise locally important bedrock aquifers interbedded alluvial, lacustrine, and volcanic deposits along valley margins and where basin-fill is thin (fig- of late Tertiary through Quaternary age (Bolke and ure 4) (Bolke and Price, 1969; Baker, 1974; Doelling Price, 1969; Baker, 1974; Doelling and others, 1980; and others, 1980). Structures including faults, folds, Oaks, 2004). The uppermost basin-fill deposits com- and a variety of fracture types likely exert strong con- prise the principal basin-fill aquifer and consist of sand trol on ground-water movement and availability in the and gravel with lesser but important fine-grained clay bedrock aquifers (Baker, 1974). Exposed bedrock in and silt layers and volcanic deposits (Bolke and Price, Curlew Valley is also an important source of sediments 1969). Fine-grained clay and silt deposits are locally

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Figure 4. Simplified geology of Curlew Valley (simplified from Hurlow, 2004). Recharge and discharge areas for the principal basin-fill aquifer, Curlew Valley, Box Elder County, Utah 7 greater than 60 feet (18 m) thick and, where present, for contamination of bedrock aquifers is generally high act as confining layers. For the purposes of recharge- (Anderson and others, 1994). type mapping, most of the Quaternary-age consolidated volcanic rocks of Curlew Valley are considered part of the basin fill. Volcanic sections of the basin fill are Overview variable and include basalt flows and associated vol- Recharge to the principal aquifer occurs in frac- caniclastic deposits (Miller and others, 1995). Local tured mountain bedrock and in the basin fill along val- thickness of volcanic deposits can be greater than sev- ley margins not containing thick, fine-grained confin- eral hundred feet; portions of Curlew Valley are domi- ing layers (figure 5). Indian Creek and Deep Creek nated by volcanic flows and deposits overlying and interbedded with unconsolidated basin fill (Miller and enter the northern part of Curlew Valley. Both streams others, 1995; Oaks, 2004). Normal faults in the un- are entirely depleted of water before reaching Great consolidated basin fill may exert strong control on Salt Lake, by diversion for irrigation, by evaporation, ground-water movement and availability (Oaks, 2004). or by a small amount of seepage contributing to recharge (Baker, 1974; Oaks, 2004). The total average annual volume of recharge from precipitation in the GROUND WATER Utah part of Curlew Valley was estimated to be about 3600 acre-feet (4 hm3), only 5% of the 75,000 total Ground water resides in both bedrock and uncon- acre-feet (93 hm3) throughout the entire Curlew Valley solidated deposits beneath Curlew Valley. The princi- surface-water basin (Bolke and Price, 1969). Baker pal aquifers currently in use in Curlew Valley are in (1974) estimated that recharge to Curlew Valley confined and unconfined portions of the unconsolidat- aquifers in Utah is 54,000 acre-feet per year (67 hm3/y) ed basin fill. This map does not address potentially via underflow in three distinct flow systems: Kelton, important bedrock ground-water resources. Potential Juniper-Black Pine, and Holbrooke-Snowville systems,

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Figure 5. Recharge block diagram. Schematic block diagram showing geography and recharge type for Curlew Valley. Black arrows show general direction of ground-water movement. Ground water flows generally southward along the valley axis to discharge areas in the south. 8 Utah Geological Survey that generally flow south from Idaho into Utah. Cur- Discharge from fractured-bedrock aquifers occurs rent recharge is likely less than this amount due to along mountain fronts and adjoining sections of increased ground-water pumping in the Idaho portion Curlew Valley where basin fill is thin. Other discharge of Curlew Valley (Oaks, 2004). occurs as localized springs and reaches of gaining The primary discharge area for the Curlew Valley streams within contiguous areas of bedrock exposure. basin-fill aquifer is in the southern portion of the val- Bedrock in the Idaho portion of Curlew Valley dis- ley (figure 5). Locomotive Springs, in the southeast charges south into basin fill along the Utah-Idaho state part of the valley, had an average annual discharge of line (Baker, 1974; Oaks, 2004). approximately 24,000 acre-feet (30 hm3) in 1972 (Baker, 1974). For the period 1993 to 1996, Atkin Water Quality (1998) calculated a vastly reduced discharge for Loco- Ground-water quality in the bedrock aquifers is motive Springs of 9500 acre-feet per year (12 hm3/y). likely generally better than that in the unconsolidated Discharge to the Great Salt Lake occurs along the basin fill. Higher rates of recharge and generally faster southern margin of the study area, but is difficult to ground-water movement may improve ground-water estimate (Bolke and Price, 1969). An additional 12,000 quality of bedrock aquifers. Water quality in bedrock acre-feet (15 hm3) of water is discharged by evapotran- aquifers along the margins of Curlew Valley is largely spiration annually within the study area (Baker, 1974). unconstrained. Ground water flows generally southward across the study area from the Idaho portion of Curlew Valley Unconsolidated Basin-Fill Aquifer (Baker, 1974; Oaks, 2004). Several cones of depression produced by ground-water pumping west and Aquifer Characteristics southwest of Snowville near the center of Curlew Val- The Curlew Valley basin fill is composed of allu- ley modify an otherwise south-sloping potentiometric vial, lacustrine, and volcanic deposits up to 5000 feet surface (Oaks, 2004). Elevation of ground water de- (1520 m) thick, and is typically saturated with water creases across much of the southern portion of Curlew for much of this thickness (Baker, 1974). Discontinu- Valley toward regional discharge areas along the north- ous layers of clay and silt form confining layers ern edge of Great Salt Lake (Baker, 1974; Oaks, 2004) throughout portions of the study area. Confined (figure 5). aquifers are typical of central Curlew Valley in Utah (Baker, 1974). Confined aquifers shallower than 800 Fractured Bedrock Aquifers to 1000 feet (240-310 m) are heavily exploited for use in domestic and farming practices (Baker, 1974). Sta- Aquifer Characteristics tic water levels recorded in wells within the valley average 153 feet (47 m) below the surface. Uncon- Bedrock aquifers in Curlew Valley are complex fined aquifers are present along the Raft River and and include volcanic, carbonate, clastic, and metamor- Hansel Mountains, which form the drainage-basin phic rocks. Along the western margin of Curlew Val- boundary, and across southern Curlew Valley including ley, bedrock of the eastern Raft River Mountains con- the Wildcat Hills and Cedar Hill. Ground water in the sists primarily of structurally disrupted Precambrian Utah part of Curlew Valley generally flows toward the and Paleozoic clastic and carbonate sedimentary and axis of the valley, then south toward Great Salt Lake metamorphic rocks (Baker, 1974; Miller and others, where it is discharged naturally in the form of springs, 1983; Hurlow, 2004). Folded and faulted carbonates seepage into the lake, or by phreatophyte or salt pan comprise the Hansel Mountains along the eastern mar- evapotranspiration (Bolke and Price, 1969; Baker, gin of Curlew Valley, and other portions of Curlew Val- 1974). Ground-water pumping for agriculture has ley are underlain by fractured volcanic rocks (Bolke locally modified this pattern, producing several dis- and Price, 1969; Hurlow, 2004). Secondary permeabil- crete cones of potentiometric depression (Oaks, 2004). ity along fractures, particularly joints, likely controls Transmissivity varies for the valley-fill aquifer. ground-water movement in consolidated bedrock Baker (1974) reported a range of 20,000 to 34,000 across the study area. square feet per day (1860-3160 m2/day) for wells in unconsolidated deposits near Kelton. Near Snowville Recharge and Discharge a single pump test of the unconsolidated basin fill gave a transmissivity value of 19,000 square feet per day Recharge of fractured-bedrock aquifers occurs in (1770 m2/day) (Baker, 1974). uplands surrounding Curlew Valley, including the Hansel and Raft River Mountains, and beneath uncon- Recharge and Discharge Areas solidated valley fill. Local bedrock recharge amounts are controlled by precipitation, rock type and fracture Much of the Utah portion of Curlew Valley con- characteristics (Baker, 1974). sists of primary recharge areas without significant con- Recharge and discharge areas for the principal basin-fill aquifer, Curlew Valley, Box Elder County, Utah 9 fining layers. Primary recharge occurs along the west- contamination sources in valley primary recharge areas ern margin of the valley, around the Wildcat Hills, and are possible and can degrade water quality. A large along a low series of hills, including Cedar Hill in the part of Curlew Valley is mapped as primary recharge east-central part of Curlew Valley. Areas of secondary and has no significant hydrogeologic barriers to con- recharge with a downward ground-water gradient and tamination of the principal aquifer by pesticides or thick confining layers cover most of the central and other water-borne contaminants. Care must be taken in northern portions of the study area and extend south- siting potential contaminant sources, such as feed lots ward toward discharge areas along Great Salt Lake. and septic tanks, especially in primary recharge areas. Southwest of the Hansel Mountains, well logs indicate The widespread clay layers in the center of Curlew secondary recharge along the eastern study-area Valley may provide some protection to the principal boundary. aquifer. Lateral continuity of confining layers is, how- We mapped discharge zones across the southern ever, not constrained. Ground water in discharge areas boundary of the study area along the northern shoreline along the southern part of Curlew Valley is least sus- and salt pans of Great Salt Lake. This zone of dis- ceptible to potential contaminants. Further study is charge encompasses the system of springs at Locomo- required to make specific evaluations of sources and tive Springs in the east and Kelton flowing well to the fate of contaminants. west. Two smaller but locally important zones of discharge are located around Pilot and Coyote springs in the west-central portion of Curlew Valley. Discharge SUMMARY AND CONCLUSIONS at these springs may be at least partially controlled by subsurface faults. The principal basin-fill aquifer of Curlew Valley consists of interbedded alluvial, lacustrine, and vol- Water Quality canic deposits. Confined and unconfined portions of the principal aquifer provide both culinary and agricul- The chemical quality of water from the basin-fill tural water. Most ground water resides in confined aquifer differs across the Utah part of the Curlew Val- portions of the principal aquifer across the central por- ley (Bolke and Price, 1969; Baker, 1974; Riding and tion of Curlew Valley. The mountains that surround Quilter, 2004). Total dissolved solids (TDS) range Curlew Valley, the uppermost parts of alluvial fans from below 500 mg/L to over 11,000 mg/L, and parts along the margins of the valley, and areas without thick of Curlew Valley have ground water with TDS values confining layers within Curlew Valley make up the pri- above 2000 mg/L (Baker, 1974; Davis, 1984; Atkin, mary recharge areas. Secondary recharge areas, which 1998; Riding and Quilter, 2004). Oaks (2004, figure contain clay or silt confining layers greater than 20 feet 8) showed two areas of high relative TDS, west of thick, cover the central part of Curlew Valley. Dis- Snowville and east of Cedar Hill. TDS generally charge from the principal aquifer occurs along the increases southward across Curlew Valley, except near southern end of Curlew Valley. Ground-water flow is Locomotive Springs, where TDS is low relative to sur- generally from the mountains toward the center of the rounding areas (Oaks, 2004, figure 8). Recent ground- valley, and then south toward discharge areas along the water quality data from Riding and Quilter (2004) northern shore of Great Salt Lake. Water quality is gen- included 51 wells in Curlew Valley. Two wells had erally moderate, with moderate TDS values across arsenic levels exceeding minimum EPA drinking-water most of Curlew Valley, and coliform contamination of standard and 27 of 51 wells tested positive for coliform several wells. bacteria (Riding and Quilter, 2004, p. 20).

Potential for Water-Quality Degradation ACKNOWLEDGMENTS The potential for ground-water contamination We thank Hugh Hurlow, Janae Wallace, Robert based solely on recharge-type mapping is moderate Ressetar, and Kimm Harty, Utah Geological Survey for across much of Curlew Valley. Much of the water in their comments and reviews. Justin Johnson and Kim the principal basin-fill aquifer comes from bedrock Nay assisted with preparing the map and figures used uplands where few pollutants enter the system, but in this report. 10 Utah Geological Survey

REFERENCES

Allmendinger, R.W., Miller, D.M., and Jordan, T.E., 1984, Hurlow, H.A., 2004, Interim geologic map of the Curlew Known and inferred Mesozoic deformation in the hin- Valley drainage basin, Box Elder County, Utah, and terland of the Sevier Belt, Northwest Utah, in Kerns, Cassia County, Idaho: Utah Geological Survey, Open- G.J., and Kerns, R.L. Jr., editors, Known and Inferred file Report 435, 34 p., 2 plates. Mesozoic Deformation in the Hinterland of the Sevier Intermountain Region Digital Image Archive Center, 2005, Belt, Northwest Utah: Utah Geological Association, State of Utah mosaic, available online at http://earth. publication 13, p. 21-34. gis.usu.edu/statemosaic.html, accessed August 10, 2005. Anderson, P.B., Susong, D.D., Wold, S.R., Heilweil, V.M., Lowe, M., and Snyder, N.P., 1996, Protecting ground water and Baskin, R.L., 1994, Hydrogeology of recharge at its source through recharge-area mapping: Utah Geo- areas and water quality of the principal aquifers along logical Survey, Survey Notes, v. 28, no. 1, p. 6-7. the Wasatch Front and adjacent areas, Utah: U.S. Geo- logical Survey Water-Resources Investigations Report Miller, D.M., Armstrong, R.L., Compton, R.R., and Todd, 93-4221, 74 p., scale 1:100,000. V.R., 1983, Geology of the Albion Raft River-Grouse Creek Mountains area, northwestern Utah and southern Ashcroft, G.L., Jensen, D.T., and Brown, J.L., 1992, Utah Idaho: Utah Geological and Mineral Survey, Special climate: Utah Climate Center, Utah State University, Study 59, p. 1-62. 127 p. Miller, D.M., Nakata, J.K., Oviatt, C.G., Nash, W.P., and Atkin, W.H., 1998, Hydrologic data for Curlew Valley, Utah: Feisinger, D.W., 1995, Pliocene and Quaternary volcan- Utah Division of Water Rights Hydrologic Data Report ism in the northern Great Salt Lake area and inferred 2, 43 p. volcanic hazards: in Lund, W.R., editor, Environmental Baker, C.H., Jr., 1974, Water resources of the Curlew Valley and Engineering Geology of the Wasatch Front Region: drainage basin, Utah and Idaho: Utah Department of Utah Geological Association Publication 24, p. 469- Natural Resources Technical Publication No. 45, 91 p. 482. Bolke, E.L., and Price, Don, 1969, Hydrologic reconnais- Oaks, R.Q., Jr., 2004, Source of ground water to Locomotive sance of Curlew Valley, Utah and Idaho: Utah Depart- Springs, southeastern Curlew Valley, Box Elder County, ment of Natural Resources Technical Publication No. Utah: in Spangler, L.E., editor, Ground Water in Utah: 25, 40 p. Resource, Protection, and Remediation: Utah Geologi- Burden, C.B., 2003, Ground-water conditions in Utah, cal Association Publication 31, p. 77-106. spring of 2003: Utah Division of Water Resources Co- Peterson, D.L., 1974, Bouguer gravity map of the northern operative Investigations Report no. 44, 120 p. Lake Bonneville Basin, Utah and Idaho: U.S. Geologi- Carpenter, Everett, 1913, Ground water in Box Elder and cal Survey Miscellaneous Field Study MF-627, 1 plate, Tooele Counties, Utah: U.S. Geological Survey Water scale 1:250,000. Supply Paper 333, 90 p. Riding, R., and Quilter, M.C., 2004, 2004 State of Utah Cook, K.L., Halverson, M.O., Stepp, J.C., and Berg, J.W., Ground-Water Program: Salt Lake City, Utah Depart- Jr., 1964, Regional gravity survey of the northern Great ment of Agriculture and Food report, 147 p., available Salt Lake Desert and adjacent areas in Utah, Nevada, online at http://www.ag.state.us/conservation/gw_re- and Idaho: Geological Society of America Bulletin, v. port.pdf, accessed August 10, 2005. 75, no. 8, p. 715-740. Snyder, N.P., and Lowe, M., 1998, Map of recharge and dis- Davis, M.C., 1984, Evaluation of low-temperature geother- charge areas for the principal valley-fill aquifer, Sanpete mal potential in north-central Box Elder County, Utah: Valley, Sanpete County, Utah: Utah Geological Survey Logan, Utah State University, M.S. thesis, 130 p. Map 174, 21 p., scale 1:125,000. Demographic and Economic Analysis Section, 2000, Utah Stokes, W.L., 1977, Subdivisions of the major physiograph- data guide, summer 2000: Salt Lake City, Utah Gover- ic provinces in Utah: Utah Geology, v. 4, no. 1, p. 1-17. nor’s Office of Budget and Planning, 16 p. Utah Division of Water Rights, 2005, Water well drilling Doelling, H.H., Campbell, J.A., Gwynn, J.W., and Perry, database, available online at http://www.waterrights. L.I., 1980, Geology and mineral resources of Box Elder utah.gov/wellinfo/default.htm, accessed August 10, County, Utah: Utah Geological and Mineral Survey 2005. Bulletin 115, 251 p., 3 plates, scale 1:125,000. Recharge and discharge areas for the principal basin-fill aquifer, Curlew Valley, Box Elder County, Utah 11

APPENDIX

Records of Wells, Curlew Valley, Utah Site number: See plate 1 for well location. Wells not used to define recharge and discharge areas are not plotted.

Local well number or spring name: See text for explanation of well numbering system; spring names and locations from the Utah Division of Water Rights.

Elevation: In feet above sea level.

Well depth: In feet below land surface.

Water level: In feet below land surface; F, flowing well.

Recharge type: P, primary recharge area; S, secondary recharge; D, discharge area.

Top of confining layer: Depth to first confining layer, in feet below land surface.

Bottom of confining layer: Depth to bottom of first confining layer, in feet below land surface.

--, no data available Table A. Records of water wells and springs used to delineate recharge and discharge areas in Curlew Valley. Data are from Utah Division of Water Rights (2005) and Baker (1974). Site Local well Northing Easting Year Elevation Total Water Recharge Top of Bottom of # number or well (ft) depth level type confining confining spring name drilled (ft) layer (ft) layer (ft) 1 (B-12-11) 5bab 4629952 323270 1983 4358 335 92 S 14 37 2 (B-12-11) 5bac 4629714 323283 1979 4353 220 143 S 1 23 3 (B-12-11) 6abb 4629936 322138 1955 4406 278 185 P – – 4 (B-12-11) 6bab 4629958 322537 1980 4389 400 173 P – – 5 (B-12-11) 7abb 4628392 322008 1955 4344 250 105 S – – 6 (B-12-11) 8aba 4628356 323985 1971 4301 224 88 S 0 90 7 (B-12-11) 8abd 4629726 323855 1963 4341 275 92 S 0 25 8 (B-12-11) 8dbc 4628360 324043 1971 4300 224 88 S 0 90 9 (B-12-11) 8bbb 4628399 322801 1954 4324 350 95 P – – 10 (B-12-10) 1aaa 4629652 340585 1996 4397 240 175 S 1 25 11 (B12-10) 18bca 4626371 330864 1972 4233 283 252 S 70 90 12 (B-12-10) 22cbd 4623721 335935 1972 4222 162 23 S 0 23 13 (B-12-9) 5bcb 4629134 342313 1971 4414 250 190 P – – 14 (B-12-9) 6abb 4629488 341467 1993 4422 220 190 P – – 15 (B-12-9) 9cca 4626536 344163 1981 4318 160 120 P – – 16 (B-12-9) 10abb 4627831 346313 1981 4397 220 178 P – – 17 (B-12-9) 16acc 4625505 344569 1977 4292 300 – P – – 18 (B-12-9) 16bba 4626286 344163 1995 4310 183 120 P – – 19 (B-12-9) 17add 4625664 343651 1995 4287 140 86 P – – 20 (B-13-11) 18ddc 4625042 322540 1999 4254 295 240 P – – 21 (B13-11) 18ccc 4634845 330823 1953 4824 179 119 P – – 22 (B-13-11) 33bbb 4631565 324326 1992 4387 260 152 S 0 25 23 (B-13-10) 25ddd 4631572 330666 1971 4473 251 180 P – – 24 (B13-9) 1adc 4638389 350797 1967 4572 420 343 P – – Site Local well Northing Easting Year Elevation Total Water Recharge Top of Bottom of # number or well (ft) depth level type confining confining spring name drilled (ft) layer (ft) layer (ft) 25 (B13-9) 11abc 4637203 347923 2001 4613 523 428 P – – 26 (B-13-9) 24ccc 4632751 348748 1998 4582 500 378 S 200 235 27 (B13-8) 10dcc 4636049 356081 1972 4690 465 345 S 0 165 28 (B-13-8) 21dcd 4632717 354540 1971 4605 362 320 S 0 120 29 (B-14-12) 12daa 4646941 321326 1979 5162 215 162 P – – 30 (B-14-11) 5acb 4648849 323963 1987 5013 304 233 P – – 31 (B-14-11) 10baa 4647546 327053 1971 4841 345 220 S 145 175 32 (B-14-11) 11acc 4646816 328658 2000 4792 280 130 S 0 120 33 (B-14-11) 22caa 4643661 326773 2000 4733 320 183 P – – 34 (B-14-10) 1dca 4647762 340349 1994 4403 343 202 S 24 56 35 (B-14-10) 1dca 4647771 340349 1951 4404 208 168 S 33 120 36 (B-14-10) 5baa 4649057 333320 1958 4706 276 82 S 80 116 37 (B-14-10) 5bba 4649102 332945 1959 4732 303 105 S 105 220 38 (B-14-10) 14cbc 4644717 337536 1970 4409 400 182 S 0 30 39 (B-14-10) 14acd 4645087 338784 1970 4391 350 170 S 0 190 40 (B-14-10) 15ccd 4644341 336304 1979 4432 505 196 S 22 74 41 (B-14-10) 34bcc 4640367 335802 1979 4386 350 210 S 158 350 42 (B14-10) 34bbb 4639468 335810 1969 4381 365 250 S 73 110 43 (B-14-9) 1dda-1 4647564 350310 1955 4463 360 170 S 154 188 44 (B-14-9) 1ddd-1 4647509 350361 1955 4463 312 135 S 104 140 45 (B-14-9) 1ddd-1 4647512 350467 1956 4467 255 166 S 5 34 46 (B-14-9) 3aaa 4649152 345814 1964 4415 205 170 S 12 120 47 (B-14-9) 4bcc 4648308 344115 1978 4401 345 190 S 80 140 48 (B-14-9) 4ccc 4647541 344091 1964 4393 360 186 S 8 43 49 (B-14-9) 5abb 4649063 343286 1999 4416 395 220 S 2 180 50 (B-14-9) 5aaa 4649049 344115 1962 4413 275 188 S 8 43 Site Local well Northing Easting Year Elevation Total Water Recharge Top of Bottom of # number or well (ft) depth level type confining confining spring name drilled (ft) layer (ft) layer (ft)

51 (B-14-9) 5cca-1 4647694 342839 1955 4399 355 180 S 113 179 52 (B-14-9) 5bb-1 4649063 342493 1955 4420 300 188 S 2 26 53 (B-14-9) 6ccc 4647566 340869 1984 4400 375 195 S 40 65 54 (B-14-9) 10cbb 4646638 345644 1979 4384 400 132 S 0 47 55 (B-14-9) 11bcb-1 4646847 345843 1953 4386 245 170 S 3 31 56 (B-14-9) 13abb-1 4645657 349706 1949 4444 75 – S 1 29 57 (B-14-9) 16aba 4645834 345141 1998 4376 153 153 S 73 99 58 (B-14-9) 16aaa 4645818 345629 1979 4377 230 130 S 1 25 59 (B-14-9) 16add 4645029 345629 1979 4370 242 122 S 0 30 60 (B-14-9) 17cab 4645043 342983 1974 4371 385 168 S 0 158 61 (B-14-9) 18bdd 4645102 341566 1967 4369 400 150 S 0 60 62 (B-14-9) 20acc 4643473 343178 1979 4360 305 144 S 2 45 63 (B-14-9) 36bcb 4640377 348789 1995 4493 490 185 S 41 62 64 (B-14-8) 1ccb 4647152 358774 1968 4570 140 80 S 6 30 65 (B-14-8) 2ddb 4647468 358292 1999 4537 61 57 S 5 30 66 (B-14-8) 2ddb 4647398 358312 1999 4538 59 56 S 0 30 67 (B-14-8) 2ddb 4647487 358292 1999 4537 59 56 S 5 59 68 (B-14-8) 2ddb 4647432 358293 1999 4538 61 57 S 5 30 69 (B-14-8) 2ddb 4647414 358293 1999 4538 61 61 S 5 30 70 (B-14-8) 2bbb 4648799 357098 1977 4558 170 90 S 70 90 71 (B-14-8) 2adb 4648219 358446 1979 4535 110 40 S 25 48 72 (B14-8) 2daa 4647967 358570 1960 4540 240 48 P – – 73 (B-14-8) 2ddb 4647450 358293 1999 4537 61 57 S 5 30 74 (B-14-8) 2dab 4647912 358430 1994 4538 70 29 P – – 75 (B-14-8) 3dcb 4647491 356624 1965 4532 63 40 P – – 76 (B-14-8) 3ccc 4647429 355615 1997 4593 207 0 P 18 97 Site Local well Northing Easting Year Elevation Total Water Recharge Top of Bottom of # number or well (ft) depth level type confining confining spring name drilled (ft) layer (ft) layer (ft) 77 (B-14-8) 5bac 4648544 352648 1972 4577 550 280 S 230 280 78 (B-14-8) 6aca 4648402 351741 1971 4500 295 195 S 0 80 79 (B-14-8) 6acd 4648258 351664 1973 4490 660 210 S 1 86 80 (B-14-8) 6dad 4647959 342406 1998 4401 485 365 S 3 26 81 (B-14-8) 8abb 4647203 353050 1973 4498 174 93 S 3 54 82 (B-14-8) 8aaa 4647245 353734 1973 4510 203 85 S 1 62 83 (B-14-8) 10aac 4646946 356734 1999 4519 75 63 P – – 84 (B-14-8) 10aac 4646940 356713 1999 4519 75 64 P – – 85 (B-14-8) 10aac 4646944 356716 1998 4519 72 63 P – – 86 (B-14-8) 10aac 4646946 356722 1999 4519 75 68 S 8 28 87 (B-14-8) 11abc 4646966 357946 1971 4530 92 50 S 0 70 88 (B-14-8) 11dcc 4645545 357879 1971 4590 200 130 S 0 25 89 (B-14-8) 12cbd 4646135 358915 1971 4634 245 165 S 0 30 90 (B-14-8) 15ddd 4643983 356991 1974 4582 500 169 P – – 91 (B-14-8) 20ccc 4642424 352080 1977 4528 453 290 P – – 92 (B-14-8) 28bbb 4642356 353791 1967 4539 650 276 S 0 20 93 (B-14-8) 32aaa-1 4640803 353660 1949 4557 330 306 S 3 50 94 (B-15-12) 34ddd 4649516 318171 1987 5411 235 165 S 151 191 95 (B-15-11) 31ddd 4649559 323050 1967 5093 410 280 P – – 96 (B-15-11) 36ccc 4649457 329504 1967 4936 320 248 P – – 97 (B-15-10) 33dda 4649426 335841 1967 4559 355 252 S 167 233 98 (B-15-10) 34bbc 4650052 336028 1979 4558 350 210 S 158 200 99 (B-15-10) 36bbb-1 4650743 339330 1956 4463 613 167 S 50 110 100 (B-15-10) 36bcb 4650348 339389 1994 4457 300 187 S 35 62 101 (B-15-10) 36bdd 4649961 340112 1980 4441 423 220 S 40 120 102 (B-15-10) 28cbc 4651163 344175 1991 4452 436 203 S 154 182 Site Local well Northing Easting Year Elevation Total Water Recharge Top of Bottom of # number or well (ft) depth level type confining confining spring name drilled (ft) layer (ft) layer (ft) 103 (B-15-9) 28ddd-1 4650853 345454 1977 4449 450 265 S 220 305 104 (B-15-9) 29dbc 4651209 343344 1966 4453 405 228 P – – 105 (B-15-9) 31abc 4650395 341720 1969 4442 407 215 S 0 172 106 (B-15-9) 32ccc 4649081 342524 1979 4420 295 200 S 60 80 107 (B-15-9) 32adb 4650143 343725 1979 4433 400 228 S 1 32 108 (B-15-9) 33ccb 4649442 344115 1980 4421 410 240 S 60 90 109 (B-15-9) 33ddc 4649064 345320 1991 4414 465 203 S 30 52 110 (B-15-9) 34bbc 4650435 345876 1994 4443 620 238 S 2 53 111 (B-15-9) 35abb 4650475 348238 1968 4477 404 182 S 0 98 112 (B-15-9) 35abb 4650478 348238 1969 4477 220 172 P – – 113 (B-15-9) 36cad 4649511 349757 1972 4492 255 195 S 0 70 114 (B-15-8) 30ddd-1 4650437 360318 1939 4560 100 17 S 0 39 115 (B-15-8) 34dac 4649236 356939 1993 4598 365 180 P – – 116 (B-15-8) 35cbc 4649232 357052 1981 4584 204 140 S 60 90 117 (B-15-8) 36daa 4649565 360116 1997 4563 260 30 D 68 169 118 (B-15-8) 36cbc 4649270 358763 1980 4540 110 38 S 23 47 119 (B-15-8) 36add 4649632 360132 1979 4562 68 27 S 6 30 120 (B-15-7) 25cbc 4650918 360435 1936 4560 228 12 S 0 154 121 (B-15-7) 32aca 4649890 363933 1967 5000 315 20 P – – 122 (B-15-7) 32aba 4650347 362515 1972 4665 262 90 S 77 105 123 (B-15-7) 32aba 4650345 362955 1971 4716 400 90 D 130 180 124 (B-14-9) 6dcc 4647390 341650 2005 4412 250 180 P – – 125 (B-14-10) 5ddd 4647615 334200 2003 4620 460 318 S 65 100 126 W. Locomotive Spring 4620639 339320 – 4216 – – D – – 127 Bar M Spring 4619077 340185 – 4215 – – D – – 128 Teal Slough 4617961 339951 – 4211 – – D – – Site Local well Northing Easting Year Elevation Total Water Recharge Top of Bottom of # number or well (ft) depth level type confining confining spring name drilled (ft) layer (ft) layer (ft) 129 Teal Spring 4617836 340120 – 4211 – – D – – 130 Off Spring 4617445 342357 – 4213 – – D – – 131 Sparks Spring 4618386 342351 – 4220 – – D – – 132 Coyote Spring 4640420 334216 – 4431 – – D – – 133 Pilot Spring 4645252 330164 – 4650 – – D – – 134 Kelton Flowing Well 4623599 324821 – 4222 – F D – – Recharge and Discharge Areas for the Principal Basin-Fill Aquifer, Curlew Valley, Box Elder County, Utah By Stefan M. Kirby, Jason L. Kneedy, and Mike Lowe Digital Compilation by Justin Johnson 113° W R R 112° 45' R 1 1 R 1 1 0 9

99 0 104 W W 102 103 W W 120 42° N 100 105 122 123 110 114 101 107 42 98 111, 112 121 R R 95 Stone Hills 119 7 6 94 W W 96 108 84 97 115 116 36 52 49 46 113 117 50 118 s 30 37 in T15N 106 109 ta 78 70 n T14N 47 71 u 80 77 o 30 79 72 125 51 43 44 74 M 31 34, 35 45 75 l Curlew 65, 66, 67, 68, 69, 73 e Junction 53 124 48 76 s 29 n 55 81 82 83, 84, 85, 86 64 Snowville a 87 H

32 54 h 89 t 30 58 r 57 56 o 88 N 133 k 39 61 60 59 e Pilot Spring re 38 C 40 Rose Ranch Reservoir 90 33 62 Y Crystal Peak E L 91 92 s L in s ta in A n ta V u n o 84 u o M

M 93 l 132 e 41 63 s r n e Coyote Spring a iv T14N H R T13N 42

t f p a e R e D 24 41° 52' 30" Explanation

25 Wells Primary Recharge Well Bald Knoll 27 Secondary Recharge Well Black Discharge Well In Butte d y i ills le a 21 H l Spring n at a dc V Wil Areas Cedar Hill Primary recharge area Secondary recharge area 26 28 Discharge area 30 e g Bedrock a 22 23 S Stream Perennial

C W re Intermittent ek 3 4 1 E 7 112° 45' L 10 Recharge area boundary T13N 2 R 14 T12N Boundary between different recharge areas U 13 5 9 6 8 C Dashed where approximate 16 Road Interstate

15 Highway 11 R R

18 9 8 W W 19 17 20 ADMINISTRATIVE OWNERSHIP

41° 45' Kelton Flowing Well 12 113° 15' 134 41° 45'

126 Ownership T12N T11N BLM USDA Forest Service Locomotive Private 127 Springs Private/Forest Service 131 128 Sovereign Lands 129 130 State of Utah State Wildlife Reserves

113° 112° 52' 30" UTAH SCALE 1:100,000 R R 1 0 1 2 3 4 5 1 STUDY AREA LOCATION 1 2 W Miles W Kilometers 0 1 2 3 4 5 6 7 8

Horizontal Datum: North American Datum 1983 113° 7' 30" Base map derived from US Geological Survey Digital Elevation Models