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Source-linked reports with geographic coverage including Idaho.

At least 649 records · Page 36Linked to original sources
USGS1993

Statistical summaries of streamflow data for selected gaging stations on and near the Idaho National Engineering Laboratory, Idaho, through September 1990

Statistical summaries and graphs of streamflow data were prepared for 13 gaging stations with 5 or more years of continuous record on and near the Idaho National Engineering Laboratory. Statistical summaries of streamflow data for the Big and Little Lost Rivers and Birch Creek were analyzed as a requisite for a comprehensive evaluation of the potential for flooding of facilities at the Idaho National Engineering Laboratory. The type of statistical analyses performed depended on the length of streamflow record for a gaging station. Streamflow statistics generated for stations with 5 to 9 years of record were: (1) magnitudes of monthly and annual flows; (2) duration of daily mean flows; and (3) maximum, median, and minimum daily mean flows. Streamflow statistics generated for stations with 10 or more years of record were: (1) magnitudes of monthly and annual flows; (2) magnitudes and frequencies of daily low, high, instantaneous peak (flood frequency), and annual mean flows; (3) duration of daily mean flows; (4) exceedance probabilities of annual low, high, instantaneous peak, and mean annual flows; (5) maximum, median, and minimum daily mean flows; and (6) annual mean and mean annual flows.

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USGS1993

Effects of well discharges on hydraulic heads in and spring discharges from the geothermal aquifer system in the Bruneau area, Owyhee County, southwestern Idaho

Demand for ground water in the 600- square-mile Bruneau study area has increased since 1954 because of agricultural development. Declining flow at Indian Bathtub Spring is adversely affecting a unique species of snail that inhabits the spring. The Bruneau study area is underlain by sedimentary and volcanic rocks that form a regional geothermal aquifer. Sedimentary rocks range in thickness from zero in the southern part of the study area to more than 3,000 feet in the northeastern corner. Volcanic rocks underlie the entire study area and extend southward to the Jarbidge Mountains. In the central part of the study area, the volcanic rocks are probably 2,000 to 3,000 feet thick. For purposes of study, the regional geothermal aquifer system was divided into sedimentary- and volcanic-rock aquifers. Ground water flows northward through the volcanic-rock aquifer to the sedimentary- rock aquifer, from areas of recharge along the Jarbidge and Owyhee Mountains into the study area, where it is discharged as spring flow or leaves the study area as underflow. Prior to extensive ground-water development, about 10,100 acre-feet was discharged by springs. Ground-water discharge from wells began in the late 1890's. From the 1890's through 1951, annual discharge was less than 10,000 acre-feet. From 1952 to 1978, annual discharge increased to about 40,600 acre-feet. During 1978-91, well discharge declined from the maximum of 49,900 acre-feet in 1981 to 34,700 acre-feet in 1991. Through 1991, nearly 1,400,000 acre-feet of ground water discharged from wells; about 546,000 acre-feet discharged from 1978 through 1991. Most pumped water is from the volcanic-rock aquifer. Ground-water development since the mid-1890's locally has modified the direction of water movement in both the sedimentary- and volcanic-rock aquifers. In 1989, ground water moved toward four cones of depression created by pumping two in the northern part of the study area are in the sedimentary-rock aquifer, two in the southern part are in the volcanic-rock aquifer. Pumping has caused hydraulic heads in the volcanic-rock aquifer to decline more than 30 feet in much of the area and at least 70 feet in one well. About 1 mile from Indian Bathtub Spring, the water level in one well declined about 10 feet during 1979-92, or about 0.7 feet per year. Within the past 25 years, discharge from monitored springs along Hot Creek and the Bruneau River has declined, most notably from Indian Bathtub Spring. Discharge from Indian Bathtub Spring in 1964 was about 2,400 gallons per minute, and by the summer of 1989, discharge was zero. Discharge began to decline in the mid-1960's when the rate of increase in pumpage accelerated. In contrast, discharge from Pence Hot Spring has ranged from about 700 gallons per minute to about 1,100 gallons per minute. Changes in discharge from monitored springs corresponded with changes in hydraulic head, which fluctuates seasonally, and are substantially less in late summer than in the spring. A hydraulic head/spring discharge relation was developed for two sites at Indian Bathtub Spring and a nearby test hole. The relation for Indian Bathtub Spring indicated that a spring discharge of 2,400 gallons per minute would relate to a hydraulic head of about 2,708 feet at the spring, which is about 34 feet higher than the head at zero spring discharge.

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USGS1993

Geohydrology and simulation of flow and water levels in the aquifer system in the Mud Lake area of the eastern Snake River plain, eastern Idaho

Water users rely on surface water and ground water to irrigate crops and to maintain lakes on wildlife refuges in the 2,200-square-mile Mud Lake study area. Ground-water development between the late 1970's and 1989 increased withdrawals from about 240,000 acre-feet in 1983 to about 370,000 acre-feet in 1990. Concurrent with ground-water development, change from subirrigation to sprinkler irrigation was predicted to reduce recharge by 95,000 acre-feet, according to an independent study. Of the 660,000 acre-feet total estimated recharge from precipitation and irrigation in the study area in 1980, half was in the area in which irrigation methods were changed. Water managers need the ability to evaluate the effects of water-use changes on the future supply of surface water and ground water. Basalt and rhyolite predominate on the surface and in the subsurface of the study area. Total basalt thickness is less than 4,000 feet; total sediment thickness (clay, silt, sand, and gravel) is less than 1,000 feet. Basalt and sediment interbeds contribute to confined ground-water conditions and affect movement and supply of water in parts of the aquifer system. Estimated losses from and gains to perennial streams and lakes in 1980 were each about 110,000 acre-feet. Water-table altitudes ranged from about 4,500 to 6,200 feet above sea level, and water-table gradients were 3 to 120 feet per mile. Underflow from basins tributary to the study area was estimated to be about 450,000 acre-feet in 1980; measured discharge from flowing wells was about 10,000 acre-feet. A five-layer, three-dimensional, finite-difference, numerical ground-water flow model was calibrated by trial-and-error to assumed 1980 steady-state hydrologic conditions to obtain a better understanding of the geohydrology and provide a tool to evaluate water-use alternatives. Water-level gradients simulated by the model were similar to gradients measured in 1980. Simulated underflow across model boundaries for 1980 was 932,000 acre-feet. Simulated losses from and gains to most streams and lakes were within 2 percent of estimated values. Simulated discharge from flowing wells matched measurements for 1980. An attempt to calibrate the numerical model to transient hydrologic conditions in monthly increments from 1981 to 1990 was discontinued because available data did not justify changes that were indicated by model simulations.

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USGS1993

Simulation of changes in water levels and ground-water flow in response to water-use alternatives in the Mud Lake area, eastern Snake River plain, eastern Idaho

Water users rely on surface and ground water to irrigate crops and maintain wildlife refuges in the 2,200-square-mile Mud Lake study area. Water managers need the ability to evaluate the effects of water-use changes on the future supply of surface and ground water. A five-layer, three-dimensional, finite-difference, numerical ground-water flow model, calibrated to assumed 1980 steady-state hydrologic conditions, was used to evaluate potential effects of seven water-use alternatives on ground-water levels and on losses from and gains to streams and lakes. The model was used to simulate steady-state water levels and ground-water flow for average 1980-90 hydrologic conditions and for seven water-use alternatives that represented changes from average 1980-90 conditions. Five alternatives represented reduced withdrawals from five different sets of wells, the sixth represented increased withdrawals in areas that could potentially support additional irrigation development, and the seventh represented reduced recharge in part of the study area where change from subirrigation to sprinkler irrigation is taking place. Simulated results from each alternative were compared with results for average 1980-90 conditions. Among the five water-use alternatives in which withdrawals from wells were reduced, simulated water levels were 0.1 to 40 feet higher than average 1980-90 conditions. Simulated stream and lake losses were as much as 4,700 acre-feet less and simulated gains were as much as 19,000 acre-feet greater in response to simulated water-level rises. Simulated underflow into the study area was as much as 8,200 acre-feet less and simulated underflow out of the study area was as much as 91,000 acre-feet greater. Simulated water-level declines were as great as 15 feet for the sixth alternative (increased withdrawals) and 10 feet for the seventh (reduced recharge). Simulated stream and lake losses were as much as 5,700 acre-feet greater and simulated gains were as much as 37,000 acre-feet less for stream and lake segments due to simulated water-level declines. Simulated underflow into the study area was as much as 7,200 acre-feet greater and simulated underflow out of the study area was as much as 23,000 acre-feet less.

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USGS1992

Chapter 4: Cretaceous thrusting and Neogene block rotation in the northern Portneuf Range region, southeastern Idaho

The Putnam thrust has long been recognized as an important Mesozoic structure in the northern Portneuf Range, southeastern Idaho. At most localities, the thrust places Ordovician rocks above Permian and Pennsylvanian rocks, although near its southeastern extent, it ramps laterally downsection to the southeast. At its southeasternmost exposures, Cambrian rocks are juxtaposed above Mississippian rocks. New work indicates that the hanging wall of the Putnam thrust contains three imbricate thrust slices or subplates, which are, from structurally lowest to highest (and generally from north to south), the Lone Pine subplate, the Narrows subplate, and the Bear Canyon-Toponce subplate. The steeply south-dipping, east-trending Narrows thrust overlies the Lone Pine subplate, underlies the Narrows subplate, and is a lateral ramp that merges eastward into the Putnam thrust. Where exposed, the Narrows thrust places Late Proterozoic quartzite of the Brigham Group over Ordovician and Cambrian rocks. The Bear Canyon thrust overlies the Narrows subplate and underlies the Bear Canyon-Toponce subplate, dips eastward along the west side of the Portneuf Range, and places lower Brigham Group quartzite above Cambrian limestone and Cambrian and Late Proterozoic upper Brigham Group quartzite and argillite. At its northern extent, the Bear Canyon thrust curves to the east, where it merges with the Putnam thrust. On the east side of the range, the intensely folded Toponce thrust places upper Brigham Group quartzite above Ordovician rocks; the Toponce is believed to be an eastward extension of the Bear Canyon thrust. East-dipping rocks within the Lone Pine subplate were not strongly deformed during Cretaceous thrusting, in contrast to rocks within the Narrows subplate, where east-vergent recumbent folds, cleavage directions that fan about northerly strikes, and tectonic thickening and thinning of beds indicate intense, thrust-parallel shear. The deformation and thrust geometry within the Narrows subplate suggest that the Narrows subplate actually consists of several horses within a foreland-dipping duplex. Late Miocene and younger basin deposits occur in north-trending valleys adjacent t o the northern Portneuf Range and, to the west, the Bannock and Pocatello ranges. At most places, the Neogene deposits dip to the east by as much as 35°, indicating that late Miocene and younger extension and down-to-the-east rotation occurred along mostly west-dipping listric faults that are inferred to merge on at least one regional detachment. Although range-bounding faults account for a large component of extension and rotation, an additional large component was contributed by numerous, relatively small-displacement normal faults within mountain ranges.

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USGS1992

Estimation of wildlife population ratios incorporating survey design and visibility bias

Age and sex ratio statistics are often a key component of the evaluation and management of wildlife populations. These statistics are determined from counts of animals that are commonly plagued by errors associated with either survey design or visibility bias. We present age and sex ratio estimators that incorporate both these sources of error and include the typical situation that animals are sampled in groups. Aerial surveys of elk ( Cervus elaphus ) in northcentral Idaho illustrate that differential visibility of age or sex classes can produce biased ratio estimates. Visibility models may be used to provide corrected estimates of ratios and their variability that incorporates errors due to sampling, visibility bias, and visibility estimation.

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USGS1992

Geohydrologic and chemical data from wells in the Mud Lake area, eastern Idaho, 1988-91

Well information, results of test drilling, water-level measurements in observation wells, and chemical and isotopic constituents in ground-water samples were among the data collected as part of a study of the availability of ground water from the eastern Snake River Plain aquifer system in the Mud Lake area of eastern Idaho. Data from about 1,200 wells were stored in the National Water Information System ground-water data base. Test holes were drilled at eight sites. Water levels were measured in 594 wells in April or May 1989 and in 470 wells in August or September 1989. Hydrographs of water levels were constructed for 99 observation wells. Water samples were collected from nine irrigation wells and were analyzed for nutrients, common dissolved ions, stable isotopes of hydrogen and oxygen, trace elements, herbicides, insecticides, and polychlorinated compounds.

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USGS1992

Water resources data, Idaho, water year 1991: Volume 1. Great Basin and Snake River Basin above King Hill

Water resources data for the 1991 water year for Idaho consist of records ofstage, discharge, and water quality of streams; stage, contents, and water qualityof lakes and reservoirs; discharge of irrigation diversions; and water levels andwater quality of ground water. The two volumes of this report contain dischargerecords for 197 stream-gaging stations and 38 irrigation diversions; stage onlyrecords for 6 stream-gaging stations; stage only for 7 lakes and reservoirs;contents only for 23 lakes and reservoirs; water-quality for 50 stream-gagingstations, 400 wells, and 11 lakes; daily totals for 1 precipitation gage; andwater levels for 475 observation wells. Additional water data were collected atvarious sites not involved in the systematic data collection program and arepublished as miscellaneous measurements. These data represent that part of theNational Water Data System operated by the U.S. Geological Survey and cooperatingState and Federal Agencies in Idaho, adjacent States, and Canada.

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USGS1992

Water resources data, Idaho, water year 1991: Volume 2. Upper Columbia River Basin and Snake River Basin below King Hill

Water resources data for the 1991 water year for Idaho consist of records of stage, discharge, and water quality of streams; stage, contents, and water quality of lakes and reservoirs; discharge of irrigation diversions; and water levels and water quality of ground water. The two volumes of this report contain discharge records for 197 stream-gaging stations and 38 irrigation diversions; stage only records for 6 stream-gaging stations; stage only for 7 lakes and reservoirs; contents only for 23 lakes and reservoirs; water-quality for 50 stream-gaging stations, 400 wells, and 11 lakes; daily totals for 1 precipitation gage; and water levels for 475 observation wells. Additional water data were collected at various sites not involved in the systematic data collection program and are published as miscellaneous measurements. These data represent that part of the National Water Data System operated by the U.S. Geological Survey and cooperating State and Federal Agencies in Idaho, adjacent States, and Canada.

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USGS1992

Aquifer-test results, direction of ground-water flow, and 1984-90 annual ground-water pumpage for irrigation, lower Big Lost River Valley, Idaho

The study area (see index map of Idaho), part of the Big Lost River drainage basin, is at the northern side of the eastern Snake River Plain. The lower Big Lost River Valley extends from the confluence of Antelope Creek and the Big Lost River to about 4 mi south of Arco and encompasses about 145 mi 2 (see map showing water-level contours). The study area is about 18 mi long and, at its narrowest, 4 mi wide. Arco, Butte City, and Moore, with populations of 1,016, 59, and 190, respectively, in 1990, are the only incorporated towns. The entire study area, except the extreme northwestern part, is in Butte City. The study area boundary is where alluvium and colluvium pinch out and abut against the White Knob Mountains (chiefly undifferentiated sedimentary rock with lesser amounts of volcanic rock) on the west and the Lost River Range (chiefly sedimentary rock) on the east. Gravel and sand in the valley fill compose the main aquifer. The southern boundary is approximately where Big Lost River valley fill intercalates with or abuts against basalt of the Snake River Group. Spring ground-water levels and flow in the Big Lost River depend primarily on temperature and the amount and timing of precipitation within the entire drainage basin. Periods of abundant water supply and water shortages are, therefore, related to the amount of annual precipitation. Surface reservoir capacity in the valley (Mackay Reservoir, about 20 mi northwest of Moore) is only 20 percent of the average annual flow of the Big Lost River (Crosthwaite and others, 1970, p. 3). Stored surface water is generally unavailable for carryover from years of abundant water supply to help relieve drought conditions in subsequent years. Many farmers have drilled irrigation wells to supplement surface-water supplies and to increase irrigated acreage. Average annual flow of the Big Lost River below Mackay Reservoir near Mackay (gaging station 13127000, not shown) in water years 1905, 1913-14, and 1920-90 was about 224,600 acre-ft; average annual flow of the Big Lost River near Arco (gaging station 13132500; see map showing water-level contours) in water years 1947-61, 1967-80, and 1983-90 was about 79,000 acre-ft (Harenberg and others, 1991, p. 254-255). Moore Canal and East Side Ditch divert water from the Big Lost River at the Moore Diversion, 3 mi north of Moore (see map showing water-level contours) and supply water for irrigation near the margins of the valley. When water supply is average or greater, water in the Big Lost River flows through the study area and onto the Snake River Plain, where it evaporates or infiltrates into the Snake River Plain aquifer. When water supply is below average, water in the Big Lost River commonly does not reach Arco; rather, it is diverted for irrigation in the interior of the valley, evaporates, or infiltrates to the valley-fill aquifer. This report describes the results of a study by the U.S. Geological Survey, in cooperation with the Idaho Department of Water Resources, to collect hydrologic data needed to help address water-supply problems in the Big Lost River Valley. Work involved (1) field inventory of 81 wells, including 46 irrigation wells; (2) measurement of water levels in 154 wells in March 1991; (3) estimation of annual ground-water pumpage for irrigation from 1984 through 1990; and (4) analysis of results of an aquifer test conducted southwest of Moore. All data obtained during this study may be inspected at the U.S. Geological Survey, Idaho District office, Boise.

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USGS1992

Seasonal changes in ground-water quality and ground-water levels and directions of ground-water movement in southern Elmore County, southwestern Idaho, including Mountain Home Air Force Base, 1990-91

The study area is located in southern Elmore County, southwestern Idaho, and includes the Mountain Home Air Force Base located approximately 10 mi southwest of the city of Mountain Home. Chemical analyzes have been made periodically since the late 1940's on water samples from supply wells on the Air Force Base. These analyses indicate increases in specific conductance and in concentrations of nitrogen compounds, chloride, and sulfate. The purposes of this report, which was prepared in cooperation with the Department of the Air Force, are to describe the seasonal changes in water quality and water levels and to depict the directions of ground-water movement in the regional aquifer system and perched-water zones. Although data presented in this report are from both the regional ground-water system and perched-water zones, the focus is on the regional system. A previous study by the U.S. Geological Survey (Parliman and Young, 1990) describes the areal changes in water quality and water levels during the fall of 1989. During March, July, and October 1990, 141 wells were inventoried and depth to water was measured. Continuous water-level recorders were installed on 5 of the wells and monthly measurements of depth to water were made in 17 of the wells during March 1990 through February 1991. Water samples from 33 wells and 1 spring were collected during the spring and fall of 1990 for chemical analyses. Samples also were collected monthly from 11 of those wells during April to September 1990 (table 1). Selected well-construction and water-use data and measurements of depth to water for 141 wells are given in table 2 (separated sheets in envelope). Directions of ground-water movement and selected hydrographs showing seasonal fluctuations of water levels in the regional ground-water system and perched-water zones are shown on sheet 2. Changes in water levels in the regional ground-water system during March to October 1990 are shown on sheet 2.

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USGS1991

Lead accumulation and osprey production near a mining site on the Coeur d'Alene River, Idaho

Mining and smelting at Kellogg-Smelterville, Idaho, resulted in high concentrations of lead in Coeur d'Alene (CDA) River sediments 15–65 km downstream, where ospreys ( Pandion haliaetus ) nested. Adult and nestling ospreys living along the CDA River had significantly higher blood lead concentrations than those at Lake Coeur d'Alene (intermediate area) or Pend Oreille and Flathead Lakes (reference areas). Lead concentrations in fish collected from the study areas paralleled those found in ospreys. Inhibition of blood δ-aminolevulinic acid dehydratase (ALAD) activity and elevation of protoporphyrin concentration provided evidence of lead exposure. In adult ospreys, ALAD activity was negatively correlated with lead in blood (r=−0.57), whereas protoporphyrin was positively correlated with lead in blood (r=+0.40). Neither hemoglobin nor hematocrit was adversely affected by the relatively modest lead concentrations found in the blood. Pronounced accumulation of lead by adults or young could ultimately result in behavioral abnormalities or death, both of which would reduce productivity of the nesting osprey population. We did not observe death related to lead, behavioral abnormalities, or reduced productivity during this 1986–87 study. Despite some lead-induced biochemical changes in blood parameters, ospreys produced young at nearly identical rates in the three study areas; these rates were among the highest ever reported in the western United States. Post-fledging survival of ospreys exposed to lead early in life remains an unknown. Lead does not biomagnify in the food chain as do organochlorine pesticides and mercury and several osprey behavior traits reduce the potential for the species to accumulate critical levels of lead. Swans, which feed at a lower trophic level, continue to die from environmental lead in the region.

Idaho↗
USGS1991

Lead toxicosis in tundra swans near a mining and smelting complex in northern Idaho

Die-offs of waterfowl have occurred in the Coeur d'Alene River system in northern Idaho since at least the early 1900's. We investigated causes of mortality and lead and cadmium contamination of 46 tundra swans ( Cygnus columbianus ) from 1987 to 1989; an additional 22 swans found dead in 1990 were not examined. We necropsied 43 of the 46 birds found from 1987 to 1989; 38 of these were from the Coeur d'Alene River system, which has been contaminated with mining and smelting wastes for a century, and the other 5 were from a nearby, relatively uncontaminated area. Of the 36 livers of swans from the contaminated area that were analyzed, 32 contained lethal levels of lead (6 to 40 μg/g, wet weight) and all birds exhibited several symptoms of lead poisoning, notably enlarged gall bladders containing viscous, dark-green bile. Only 13% of the lead-poisoned birds (10% when data were included from other studies of swans in the area) contained shot, compared to 95% of lead-poisoned swans in studies outside northern Idaho. Lead concentrations in blood samples from 16 apparently healthy swans (0.5 to 2.3 μg/g, and 4 lead-poisoned birds found moribund (1.3 to 9.6 μg/g) indicated that tundra swans accumulated high levels of lead from ingestion of sediment that contained up to 8,700 μg/g of lead and plants that contained up to 400 μg/g. The swans spend only a few weeks in the area staging during the spring migration. The five tundra swans from the uncontaminated area had low levels of lead and essentially no symptoms of lead poisoning. Based on the conventional standard of 0.5 μg/g in whole blood as an indicator of lead poisoning, all of the swans in the Coeur d'Alene River system were either lead-poisoned or at risk of developing plumbism.

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