Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
The Christina River Basin drains 565 mi2 (square miles) in Pennsylvania and Delaware. Water from the basin is used for recreation, drinking-water supply, and to support aquatic life. The Christina River Basin includes the major subbasins of Brandywine Creek, Red Clay Creek, White Clay Creek, and Christina River. The Brandywine Creek is the largest of the subbasins and drains an area of 327 mi2. Water quality in some parts of the Christina River Basin is impaired and does not support designated uses of the streams. A multi-agency water-quality management strategy included a modeling component to evaluate the effects of point and nonpoint-source contributions of nutrients and suspended sediment on streamwater quality. To assist in nonpoint-source evaluation, four independent models, one for each of the four main subbasins of the Christina River Basin, were developed and calibrated using the model code Hydrological Simulation Program—Fortran (HSPF). Water-quality data for model calibration were collected in each of the four main subbasins and in small subbasins predominantly covered by one land use following a nonpoint-source monitoring plan. Under this plan, stormflow and base-flow samples were collected during 1998 at six sites in the Brandywine Creek subbasin and five sites in the other subbasins.
The HSPF model for the Brandywine Creek Basin simulates streamflow, suspended sediment, and the nutrients, nitrogen and phosphorus. In addition, the model simulates water temperature, dissolved oxygen, biochemical oxygen demand, and plankton as secondary objectives needed to support the sediment and nutrient simulations. For the model, the basin was subdivided into 35 reaches draining areas that ranged from 0.6 to 18 mi2. Three of the reaches contain regulated reservoir. Eleven different pervious land uses and two impervious land uses were selected for simulation. Land-use areas were determined from 1995 land-use data. The predominant land uses in the basin are forested, agricultural, residential, and urban. The hydrologic component of the model was run at an hourly time step and calibrated using streamflow data for eight U.S. Geological Survey (USGS) stream-flow-measurement stations for the period of January 1, 1994, through October 29, 1998. Daily precipitation data for three National Oceanic and Atmospheric Administration (NOAA) gages and hourly data for one NOAA gage were used for model input. The difference between observed and simulated streamflow volume ranged from -2.7 to 3.9 percent for the nearly 5-year period at the eight calibration sites. Annual differences between observed and simulated streamflow generally were greater than the overall error. For example, at a site near the bottom of the basin (drainage area of 237 mi2), annual differences between observed and simulated streamflow ranged from -14.0 to 18.8 percent and the overall error for the 5-year period was 1.0 percent. Calibration errors for 36 storm periods at the eight calibration sites for total volume, low-flow-recession rate, 50-percent lowest flows, 10-percent highest flows, and storm peaks were within the recommended criteria of 20 percent or less. Much of the error in simulating storm events on an hourly time step can be attributed to uncertainty in the rainfall data.
The water-quality component of the model was calibrated using monitoring data collected at six USGS streamflow-measurement stations with variable water quality monitoring periods ending October 1998. Because of availability, monitoring data for suspended solids concentrations were used as surrogates for suspended-sediment concentrations, although suspended-solids data may underestimate suspended sediment and affect apparent accuracy of the suspended-sediment simulation. Comparison of observed to simulated loads for two to six individual storms in 1998 at each of the six monitoring sites indicate that simulation error is commonly as large as an order of magnitude for suspended sediment and nutrients. The simulation error tends to be smaller for dissolved nutrients than for particulate nutrients. Errors of 40 percent or less for monthly or annual values indicate a fair to good water-quality calibration according to recommended criteria, with much larger errors possible for individual events. Assessment of the water-quality calibration under stormflow conditions is limited by the relatively small amount of available water-quality data in the basin. Duration curves for simulated and reported sediment concentration at Brandywine Creek at Wilmington, Del., are similar, indicating model performance is better when evaluated over longer periods than when evaluated on individual storm events.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri024279","collaboration":"Prepared in cooperation with the Delaware River Basin Commission, Delaware Department of Natural Resources and Environmental Control, and the Pennsylvania Department of Environmental Protection","usgsCitation":"Senior, L.A., and Koerkle, E.H., 2003, Simulation of streamflow and water quality in the Brandywine Creek subbasin of the Christina River basin, Pennsylvania and Delaware, 1994-98: U.S. Geological Survey Water-Resources Investigations Report 2002-4279, xii, 207 p., https://doi.org/10.3133/wri024279.","productDescription":"xii, 207 p.","onlineOnly":"N","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":4620,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2002/4279/wri20024279.pdf","text":"Report","size":"17.9 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2002-4279"},{"id":179475,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2002/4279/coverthb.jpg"}],"contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
Muskellunge Lake is a productive, eutrophic lake because of high nutrient loading. Historical data indicate that water quality has only slightly degraded since the early 1970s, possibly because of phosphorus input from effluent from septic systems. A detailed phosphorus budget for the lake indicated that most of the phosphorus comes from natural sources?ground water and surface water flowing through relatively undeveloped areas surrounding the lake. Modeling results indicated that the natural input of phosphorus was sufficient to maintain the lake's eutrophic condition. Analysis of sediment cores confirmed that only small changes in nutrient and algal concentrations have occurred over the past 100 years; however, the analysis indicated that the macrophyte community has increased over this time period. The aeration system, installed to alleviate winter anoxia, maintains aerobic conditions throughout the main bays of the lake.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri034011","collaboration":"Prepared in cooperation with the Muskellunge Lake Association","usgsCitation":"Robertson, D.M., Rose, W., and Saad, D.A., 2003, Water quality and the effects of changes in phosphorus loading to Muskellunge Lake, Vilas County, Wisconsin: U.S. Geological Survey Water-Resources Investigations Report 2003-4011, vi, 18 p., https://doi.org/10.3133/wri034011.","productDescription":"vi, 18 p.","numberOfPages":"26","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":3989,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri034011/","linkFileType":{"id":5,"text":"html"}},{"id":311313,"rank":101,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/wri034011/pdf/03-4011_Musky_Lake.pdf"},{"id":171681,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"Wisconsin","county":"Vilas County","otherGeospatial":"Muskellunge Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -89.41669464111328,\n 45.92775190489084\n ],\n [\n -89.41669464111328,\n 45.97155499289284\n ],\n [\n -89.33378219604492,\n 45.97155499289284\n ],\n [\n -89.33378219604492,\n 45.92775190489084\n ],\n [\n -89.41669464111328,\n 45.92775190489084\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a07e4b07f02db5f9b3d","contributors":{"authors":[{"text":"Robertson, Dale M. 0000-0001-6799-0596 dzrobert@usgs.gov","orcid":"https://orcid.org/0000-0001-6799-0596","contributorId":150760,"corporation":false,"usgs":true,"family":"Robertson","given":"Dale","email":"dzrobert@usgs.gov","middleInitial":"M.","affiliations":[{"id":37947,"text":"Upper Midwest Water Science Center","active":true,"usgs":true}],"preferred":true,"id":236213,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rose, William J. wjrose@usgs.gov","contributorId":2182,"corporation":false,"usgs":true,"family":"Rose","given":"William J.","email":"wjrose@usgs.gov","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":236215,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Saad, David A. dasaad@usgs.gov","contributorId":121,"corporation":false,"usgs":true,"family":"Saad","given":"David","email":"dasaad@usgs.gov","middleInitial":"A.","affiliations":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"preferred":true,"id":236214,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":51618,"text":"wri024177 - 2003 - Occurrence and distribution of dissolved trace elements in the surface waters of the Yakima River basin, Washington","interactions":[],"lastModifiedDate":"2017-02-07T09:14:48","indexId":"wri024177","displayToPublicDate":"2003-07-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4177","title":"Occurrence and distribution of dissolved trace elements in the surface waters of the Yakima River basin, Washington","docAbstract":"The occurrence, distribution, and transport of dissolved (filtered-water) trace elements in the surface waters of the Yakima River Basin were assessed using data collected between 1999 and 2000 as part of the U.S. Geological Survey s National Water-Quality Assessment (NAWQA) Program. Samples were collected at 34 sites throughout the basin in August 1999, using a Lagrangian sampling design. From May 1999 through January 2000, samples also were collected weekly during the irrigation season and once per month during the nonirrigation season at three intensive fixed sites. Although the focus of this study was on 9 trace elements (aluminum, arsenic, barium, copper, iron, manganese, nickel, uranium, and zinc), 14 additional elements were analyzed in filtered water.
\nConcentrations of most trace elements in filtered water generally were low and there were no exceedances of the U.S. Environmental Protection Agency (USEPA) freshwater aquatic-life water-quality criteria. The USEPA drinking-water standard for arsenic (10 µg/L) was exceeded in two samples that were collected under base-flow conditions during the nonirrigation season at Granger Drain. Over 40 percent of all filtered-water samples collected during this study exceeded the USEPA health advisory level of 2.0 µg/L for arsenic. Arsenic concentrations in agricultural drains were highest when the drains were primarily fed by shallow ground water, and concentrations in the Yakima River were highest when the river was fed primarily by agricultural return flow. The USEPA secondary maximum contaminant level for manganese (50 µg/L) was exceeded in three samples collected at Granger Drain during the nonirrigation season.
\nInstantaneous arsenic loads calculated for August 1999 were similar to mean monthly loads determined in August 1989 at two intensive fixed sites located on the Yakima main stem. In August 1999, arsenic loads increased twofold between the Yakima River at river mile 72 above Satus and the Yakima River at Kiona at river mile 29.9. The dissolved arsenic loads for the Yakima River at Euclid Bridge at river mile 55 near Grandview and Yakima River at Kiona were within 13 percent of the August 1989 levels.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri024177","collaboration":"USGS National Water-Quality Assessment Program","usgsCitation":"Hughes, C.A., 2003, Occurrence and distribution of dissolved trace elements in the surface waters of the Yakima River basin, Washington: U.S. Geological Survey Water-Resources Investigations Report 2002-4177, x, 76 p. : ill. (some col.), col. maps ; 28 cm., https://doi.org/10.3133/wri024177.","productDescription":"x, 76 p. : ill. (some col.), col. maps ; 28 cm.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":86588,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2002/4177/wri02-4177.pdf","text":"Report","size":"8.1 MB","linkFileType":{"id":1,"text":"pdf"},"description":"PDF of report"},{"id":124658,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2002/4177/report-thumb.jpg"}],"contact":"Director, Oregon Water Science Center
U.S. Geological Survey
2130 SW 5th Avenue
Portland, Oregon 97201
http://or.water.usgs.gov
The Trinity aquifer, composed of Lower Cretaceous carbonate rocks, largely controls the ground-water hydrology in the study area of northern Bexar County, Texas. Discharge from the Trinity aquifer recharges the downgradient, hydraulically connected Edwards aquifer one of the most permeable and productive aquifers in the Nation and the sole source of water for more than a million people in south-central Texas. The unconfined, karstic outcrop of the Edwards aquifer makes it particularly vulnerable to contamination resulting from urbanization that is spreading rapidly northward across an \"environmentally sensitive\" recharge zone of the Edwards aquifer and its upgradient \"catchment area,\" composed mostly of the less permeable Trinity aquifer.
A better understanding of the Trinity aquifer is needed to evaluate water-management decisions affecting the quality of water in both the Trinity and Edwards aquifers. A study was made, therefore, in cooperation with the San Antonio Water System to assess northern Bexar County's vulnerability to ground-water contamination. The vulnerability of ground water to contamination in this area varies with the effects of five categories of natural features (hydrogeologic units, faults, caves and (or) sinkholes, slopes, and soils) that occur on the outcrop and in the shallow subcrop of the Glen Rose Limestone.
Where faults affect the rates of recharge or discharge or the patterns of ground-water flow in the Glen Rose Limestone, they likewise affect the risk of water-quality degradation. Caves and sinkholes generally increase the vulnerability of ground water to contamination, especially where their occurrences are concentrated. The slope of land surface can affect the vulnerability of ground water by controlling where and how long a potential contaminant remains on the surface. Disregarding the exception of steep slopes which are assumed to have no soil cover the greater the slope, the less the risk of ground-water contamination. Because most soils in the study area are uniformly thin, they have only minimal effect on the vulnerability of ground water to contamination.
The results of hydrogeologic mapping during the present study divide the outcrop of the Glen Rose Limestone into five mappable intervals, labeled (youngest to oldest) A through E. Of these intervals, only the middle (C) and the lowermost (E) generally provide appreciable permeability.
The vulnerability assessment provided herein was determined by combining the presumed effects of selected natural features (with individual vulnerability ratings ranging from 0 through 35) using a grid-based, multilayer system of digital datasets and geographic information system analysis. The resulting vulnerability map comprises composite vulnerability ratings that range from 26 through 104. The relatively less vulnerable areas those containing no faults, sinkholes, or caves occupy about 92 percent of the study area. The most vulnerable areas are those containing both a fault and one or more caves. The distribution of the most vulnerable areas which trend from southwest to northeast, roughly parallel to the Balcones fault zone occur mainly where faults intersect caves.
The Ogallala and Arikaree aquifers are important water resources in the Rosebud Indian Reservation area and are used extensively for irrigation, municipal, and domestic water supplies. Continued or increased withdrawals from the Ogallala and Arikaree aquifers in the Rosebud Indian Reservation area have the potential to affect water levels in these aquifers. This report describes a conceptual model of ground-water flow in these aquifers and documents the development and calibration of a numerical model to simulate ground-water flow. Data for a twenty-year period (water years 1979 through 1998) were analyzed for the conceptual model and included in steady-state and transient numerical simulations of ground-water flow for the same 20-year period.
A three-dimensional ground-water flow model, with two layers, was used to simulate ground-water flow in the Ogallala and Arikaree aquifers. The upper layer represented the Ogallala aquifer, and the lower layer represented the Arikaree aquifer. The study area was divided into grid blocks 1,640 feet (500 meters) on a side, with 153 rows and 180 columns.
Areal recharge to the Ogallala and Arikaree aquifers occurs from precipitation on the outcrop areas. The recharge rate for the steady-state simulation was 3.3 inches per year for the Ogallala aquifer and 1.7 inches per year for the Arikaree aquifer for a total recharge rate of 266 cubic feet per second.
Discharge from the Ogallala and Arikaree aquifers occurs through evapotranspiration, discharge to streams, and well withdrawals. Discharge rates in cubic feet per second for the steady-state simulation were 184 for evapotranspiration, 46.8 and 19.7 for base flow to the Little White and Keya Paha Rivers, respectively, and 11.6 for well withdrawals from irrigation use. Estimated horizontal hydraulic conductivity used for the numerical model ranged from 0.2 to 120 feet per day in the Ogallala aquifer and 0.1 to 5.4 feet per day in the Arikaree aquifer. A uniform vertical hydraulic conductivity value of 6.6x10-4 feet per day was applied to the Ogallala aquifer. Vertical hydraulic conductivity was estimated for five zones in the Arikaree aquifer and ranged from 8.6x10-6 to 7.2x10-1 feet per day. Average rates of recharge, maximum evapotranspiration, and well withdrawals were included in the steady-state simulation, whereas the time-varying rates were included in the transient simulation.
Model calibration was accomplished by varying parameters within plausible ranges to produce the best fit between simulated and observed hydraulic heads and base-flow discharges from the Ogallala and Arikaree aquifers. For the steady-state simulation, the root mean square error for simulated hydraulic heads for all wells was 26.8 feet. Simulated hydraulic heads were within ±50 feet of observed values for 95 percent of the wells. For the transient simulation, the difference between the simulated and observed means for hydrographs was within ±40 feet for all observation wells. The potentiometric surfaces of the two aquifers calculated by the steady-state simulation established initial conditions for the transient simulation.
A sensitivity analysis was used to examine the response of the calibrated steady-state model to changes in model parameters including horizontal and vertical hydraulic conductivity, evapotranspiration, recharge, and riverbed conductance. The model was most sensitive to recharge and horizontal hydraulic conductivity.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri034043","usgsCitation":"Long, A.J., Putnam, L.D., and Carter, J.M., 2003, Simulated ground-water flow in the Ogallala and Arikaree aquifers, Rosebud Indian Reservation area, South Dakota: U.S. Geological Survey Water-Resources Investigations Report 2003-4043, vi, 69 p., https://doi.org/10.3133/wri034043.","productDescription":"vi, 69 p.","costCenters":[],"links":[{"id":178313,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":407732,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_55304.htm","linkFileType":{"id":5,"text":"html"}},{"id":4637,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri034043/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"South Dakota","otherGeospatial":"Ogallala and Arikaree aquifers, Rosebud Indian Reservation area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -101.2833,\n 43.5\n ],\n [\n -100.25,\n 43.5\n ],\n [\n -100.25,\n 42.9569\n ],\n [\n -101.2833,\n 42.9569\n ],\n [\n -101.2833,\n 43.5\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b23e4b07f02db6ae0db","contributors":{"authors":[{"text":"Long, Andrew J. 0000-0001-7385-8081 ajlong@usgs.gov","orcid":"https://orcid.org/0000-0001-7385-8081","contributorId":989,"corporation":false,"usgs":true,"family":"Long","given":"Andrew","email":"ajlong@usgs.gov","middleInitial":"J.","affiliations":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true},{"id":562,"text":"South Dakota Water Science Center","active":true,"usgs":true}],"preferred":true,"id":242508,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Putnam, Larry D. ldputnam@usgs.gov","contributorId":990,"corporation":false,"usgs":true,"family":"Putnam","given":"Larry","email":"ldputnam@usgs.gov","middleInitial":"D.","affiliations":[],"preferred":true,"id":242509,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Carter, Janet M. 0000-0002-6376-3473 jmcarter@usgs.gov","orcid":"https://orcid.org/0000-0002-6376-3473","contributorId":339,"corporation":false,"usgs":true,"family":"Carter","given":"Janet","email":"jmcarter@usgs.gov","middleInitial":"M.","affiliations":[{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true},{"id":562,"text":"South Dakota Water Science Center","active":true,"usgs":true}],"preferred":false,"id":242507,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":69694,"text":"mf2412 - 2003 - Geologic map of the Ponca quadrangle, Newton, Boone, and Carroll Counties, Arkansas","interactions":[],"lastModifiedDate":"2012-02-10T00:11:34","indexId":"mf2412","displayToPublicDate":"2003-07-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2412","title":"Geologic map of the Ponca quadrangle, Newton, Boone, and Carroll Counties, Arkansas","docAbstract":"This digital geologic map compilation presents new polygon\r\n (i.e., geologic map unit contacts), line (i.e., fault, fold\r\n axis, and structure contour), and point (i.e., structural\r\n attitude, contact elevations) vector data for the Ponca 7 1/2'\r\n quadrangle in northern Arkansas. The map database, which is at\r\n 1:24,000-scale resolution, provides geologic coverage of an\r\n area of current hydrogeologic, tectonic, and stratigraphic\r\n interest. The Ponca quadrangle is located in Newton, Boone,\r\n and Carroll Counties about 20 km southwest of the town of\r\n Harrison. The map area is underlain by sedimentary rocks of\r\n Ordovician, Mississippian, and Pennsylvanian age that were\r\n mildly deformed by a series of normal and strike-slip faults and\r\n folds. The area is representative of the stratigraphic and\r\n structural setting of the southern Ozark Dome. The Ponca\r\n quadrangle map provides new geologic information for better\r\n understanding groundwater flow paths and development of karst\r\n features in and adjacent to the Buffalo River watershed.","language":"ENGLISH","doi":"10.3133/mf2412","usgsCitation":"Hudson, M., and Murray, K., 2003, Geologic map of the Ponca quadrangle, Newton, Boone, and Carroll Counties, Arkansas (Version 1.0): U.S. Geological Survey Miscellaneous Field Studies Map 2412, 49 x 39 inches, https://doi.org/10.3133/mf2412.","productDescription":"49 x 39 inches","costCenters":[],"links":[{"id":110428,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_55146.htm","linkFileType":{"id":5,"text":"html"},"description":"55146"},{"id":191926,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6367,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/mf/2003/mf-2412/","linkFileType":{"id":5,"text":"html"}}],"scale":"24000","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -93.36749999999999,36 ], [ -93.36749999999999,36.1175 ], [ -93.25,36.1175 ], [ -93.25,36 ], [ -93.36749999999999,36 ] ] ] } } ] }","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aeee4b07f02db691280","contributors":{"authors":[{"text":"Hudson, Mark R. 0000-0003-0338-6079 mhudson@usgs.gov","orcid":"https://orcid.org/0000-0003-0338-6079","contributorId":1236,"corporation":false,"usgs":true,"family":"Hudson","given":"Mark R.","email":"mhudson@usgs.gov","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"preferred":true,"id":280912,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Murray, Kyle E.","contributorId":31825,"corporation":false,"usgs":true,"family":"Murray","given":"Kyle E.","affiliations":[],"preferred":false,"id":280913,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":47764,"text":"wri024282 - 2003 - Ground-water contamination from lead shot at Prime Hook National Wildlife Refuge, Sussex County, Delaware","interactions":[],"lastModifiedDate":"2012-02-02T00:10:23","indexId":"wri024282","displayToPublicDate":"2003-07-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4282","title":"Ground-water contamination from lead shot at Prime Hook National Wildlife Refuge, Sussex County, Delaware","docAbstract":"Prime Hook National Wildlife Refuge is located in southeastern Delaware in coastal lowlands along the margin of Delaware Bay. For 37 years, the Broadkiln Sportsman?s Club adjacent to the refuge operated a trap-shooting range, with the clay-target launchers oriented so that the expended lead shot from the range dropped into forested wetland areas on the refuge property. Investigators have estimated that up to 58,000 shotgun pellets per square foot are present in locations on the refuge where the lead shot fell to the ground.\r\n\r\nAs part of the environmental risk assessment for the site, the U.S. Geological Survey (USGS) investigated the potential for lead contamination in ground water. Results from two sampling rounds in 19 shallow wells indicate that elevated levels of dissolved lead are present in ground water at the site. The lead and associated metals, such as antimony and arsenic (common shotgun pellet alloys), are being transported along shallow ground-water flowpaths toward an open-water slough in the forested wetland adjacent to the downrange target area. Water samples from wells located along the bank of the slough contained dissolved lead concentrations higher than 400 micrograms per liter, and as high as 1 milligram per liter. In contrast, a natural background concentration of lead from ground water in a well upgradient from the site is about 1 microgram per liter. Two water samples collected several months apart from the slough directly downgradient of the shooting range contained 24 and 212 micrograms per liter of lead, respectively.\r\n\r\nThe data indicate that lead from a concentrated deposit of shotgun pellets on the refuge has been mobilized through a combination of acidic water conditions and a very sandy, shallow, unconfined aquifer, and is moving along ground-water flowpaths toward the surface-water drainage. Data from this study will be used to help delineate the lead plume, and determine the fate and transport of lead from the source area.","language":"ENGLISH","doi":"10.3133/wri024282","usgsCitation":"Soeder, D.J., and Miller, C.V., 2003, Ground-water contamination from lead shot at Prime Hook National Wildlife Refuge, Sussex County, Delaware: U.S. Geological Survey Water-Resources Investigations Report 2002-4282, v, 26 p. : col. ill., col. maps ; 28 cm., https://doi.org/10.3133/wri024282.","productDescription":"v, 26 p. : col. ill., col. maps ; 28 cm.","costCenters":[],"links":[{"id":4090,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri02-4282/","linkFileType":{"id":5,"text":"html"}},{"id":124630,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_2002_4282.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66d055","contributors":{"authors":[{"text":"Soeder, Daniel J.","contributorId":70040,"corporation":false,"usgs":true,"family":"Soeder","given":"Daniel","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":236185,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, Cherie V. 0000-0001-7765-5919 cvmiller@usgs.gov","orcid":"https://orcid.org/0000-0001-7765-5919","contributorId":863,"corporation":false,"usgs":true,"family":"Miller","given":"Cherie","email":"cvmiller@usgs.gov","middleInitial":"V.","affiliations":[{"id":503,"text":"Office of Water Quality","active":true,"usgs":true}],"preferred":true,"id":236184,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":51401,"text":"ofr03249 - 2003 - North Dakota aeromagnetic and gravity maps and data: A web site for distribution of data","interactions":[],"lastModifiedDate":"2021-12-20T21:11:00.280531","indexId":"ofr03249","displayToPublicDate":"2003-07-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2003-249","title":"North Dakota aeromagnetic and gravity maps and data: A web site for distribution of data","docAbstract":"The North Dakota aeromagnetic grid is constructed from grids that \r\n combine information collected in 13 separate aeromagnetic surveys \r\n conducted between 1978 and 2001. The data from these surveys are \r\n of varying quality. The design and specifications (terrain \r\n clearance, sampling rates, line spacing, and reduction \r\n procedures) varied from survey to survey depending on the purpose \r\n of the project and the technology of that time. Every attempt was \r\n made to acquire the data in digital form. Most of the available \r\n digital data were obtained from aeromagnetic surveys flown by the \r\n U.S. Geological Survey (USGS), flown on contract with the USGS, \r\n or were obtained from other federal agencies and state universities. \r\n Some of the 1980 data are available only on hand-contoured maps \r\n and had to be digitized. These maps were digitized along \r\n flight-line/contour-line intersections, which is considered to be \r\n the most accurate method of recovering the original data. Digitized \r\n data are available as USGS Open File Report 99-557. All surveys \r\n have been continued to 304.8 meters (1000 feet) above ground and \r\n then blended or merged together.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr03249","usgsCitation":"Sweeney, R.E., and Hill, P.L., 2003, North Dakota aeromagnetic and gravity maps and data: A web site for distribution of data (Version 1.0): U.S. Geological Survey Open-File Report 2003-249, HTML Document, https://doi.org/10.3133/ofr03249.","productDescription":"HTML Document","costCenters":[],"links":[{"id":4408,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2003/ofr-03-249/","linkFileType":{"id":5,"text":"html"}},{"id":393125,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_55299.htm"},{"id":178837,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"North 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1994–2000","interactions":[],"lastModifiedDate":"2022-02-14T20:41:39.273101","indexId":"wri024270","displayToPublicDate":"2003-07-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4270","title":"Changes in nutrient and pesticide concentrations in urban and agricultural areas of the South Platte River Basin, Colorado, Wyoming, and Nebraska, 1994–2000","docAbstract":"As part of the National Water-Quality Assessment (NAWQA) Program, the U.S. Geological Survey (USGS) monitored two sites on the main-stem South Platte River? an urban site in Denver and a mixed urban/agricultural site near Kersey?to determine changes in nutrient and pesticide concentrations from 1994 through 2000. Concentrations of nitrate, nitrite, ammonia, and orthophosphorus decreased at the Denver site during the study period, likely due to an increase in instream dilution of wastewater-treatment plant (WWTP) discharge and upgrades at the WWTPs. In contrast, only concentrations of orthophosphorus decreased at the Kersey site; agricultural inputs between Denver and Kersey may have offset the observed decreases in other nutrients upstream. During the extreme low-flow conditions in 1994, when there was relatively little snowmelt to dilute instream pesticide concentrations, total median pesticide concentrations at both sites were the highest of the study period. During the less extreme conditions in 1997 through 2000, greater amounts of snowmelt likely led to lower total median pesticide concentrations at both sites. Because pesticide-use data are not available, the contribution of changes in the amount and type of pesticides applied on the land to changes in the concentration of pesticides in the river is not known but likely was substantial. In general, insecticides predominated at the Denver site, whereas herbicides predominated at the Kersey site.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri024270","usgsCitation":"Sprague, L.A., and Greve, A.I., 2003, Changes in nutrient and pesticide concentrations in urban and agricultural areas of the South Platte River Basin, Colorado, Wyoming, and Nebraska, 1994–2000: U.S. Geological Survey Water-Resources Investigations Report 2002-4270, 12 p., https://doi.org/10.3133/wri024270.","productDescription":"12 p.","costCenters":[],"links":[{"id":170311,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":395932,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_54637.htm"},{"id":4087,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri024270/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Colorado, Nebraska, Wyoming","otherGeospatial":"South Platte River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -106.2250,\n 38.7583\n ],\n [\n -100.6833,\n 38.7583\n ],\n [\n -100.6833,\n 41.4458\n ],\n [\n -106.2250,\n 41.4458\n ],\n [\n -106.2250,\n 38.7583\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e5e4b07f02db5e6b45","contributors":{"authors":[{"text":"Sprague, Lori A. 0000-0003-2832-6662 lsprague@usgs.gov","orcid":"https://orcid.org/0000-0003-2832-6662","contributorId":726,"corporation":false,"usgs":true,"family":"Sprague","given":"Lori","email":"lsprague@usgs.gov","middleInitial":"A.","affiliations":[{"id":509,"text":"Office of the Associate Director for Water","active":true,"usgs":true},{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true},{"id":27111,"text":"National Water Quality Program","active":true,"usgs":true}],"preferred":true,"id":236177,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Greve, Adrienne I.","contributorId":40959,"corporation":false,"usgs":true,"family":"Greve","given":"Adrienne","email":"","middleInitial":"I.","affiliations":[],"preferred":false,"id":236178,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":69693,"text":"mf2327C - 2003 - Geochemistry, geochronology, mineralogy, and geology suggest sources of and controls on mineral systems in the southern Toquima Range, Nye County, Nevada","interactions":[],"lastModifiedDate":"2021-10-29T20:32:41.208546","indexId":"mf2327C","displayToPublicDate":"2003-06-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2327","chapter":"C","title":"Geochemistry, geochronology, mineralogy, and geology suggest sources of and controls on mineral systems in the southern Toquima Range, Nye County, Nevada","docAbstract":"Geochemistry maps showing the distribution and abundance of 18 elements in about 1,400 rock samples, both mineralized and unmineralized, from the southern Toquima Range, Nev., indicate major structural and lithologic controls on mineralization, and suggest sources of the elements. Radiometric age data, lead mineralogy and paragenesis data, and lead-isotope data supplement the geochemical and geologic data, providing further insight into timing, sources, and controls on mineralization.\r\nMajor zones of mineralization are centered on structural margins of calderas and principal northwest-striking fault zones, as at Round Mountain, Manhattan, and Jefferson mining districts, and on intersections of low-angle and steep structures, as at Belmont mining district. Paleozoic sedimentary rocks, mostly limestones (at Manhattan, Jefferson, and Belmont districts), and porous Oligocene ash-flow tuffs (at Round Mountain district) host the major deposits, although all rock types have been mineralized as evidenced by numerous prospects throughout the area.\r\nPrincipal mineral systems are gold-silver at Round Mountain where about 7 million ounces of gold and more than 4 million ounces of silver has been produced; gold at Gold Hill in the west part of the Manhattan district where about a half million ounces of gold has been produced; gold-mercury-arsenic-antimony in the east (White Caps) part of the Manhattan district where a few hundred thousand ounces of gold has been produced; and silver-lead-antimony at Belmont where more than 150,000 ounces of silver has been produced. Lesser amounts of gold and silver have been produced from the Jefferson district and from scattered mines elsewhere in the southern Toquima Range. A small amount of tungsten was produced from mines in the granite of the Round Mountain pluton exposed east of Round Mountain, and small amounts of arsenic, antimony, and mercury have been produced elsewhere in the southern Toquima Range.\r\nAll elements show unique distribution patterns that suggest specific sources and lithologic influences on deposition, as well as multiple episodes of mineralization. Principal episodes of mineralization are Late Cretaceous (molybdenum and tungsten in and near granite; silver at Belmont and Silver Point mines), early Oligocene [tourmaline and base- and precious-metals around the granodiorite of Dry Canyon stock as well as at Manhattan(?)], late Oligocene (gold at Round Mountain and Jefferson), and Miocene (gold at Manhattan). Most likely principal sources of molybdenum, tungsten, silver, and bismuth are Cretaceous granites; of antimony, arsenic, and mercury are intermediate-composition early Oligocene intrusives; and of gold are early and late Oligocene and early Miocene magmas of the volcanic cycle. Lead may have been derived principally from Cretaceous granitic magma and Paleozoic sedimentary rocks.\r\nSeveral areas prospective for undiscovered mineral deposits are suggested by spatial patterns of element distributions related to geologic features. The Manhattan district in the vicinity of the White Caps mine may be underlain by a copper-molybdenum porphyry system related to a buried stock; peripheral high-grade gold veins and skarn deposits may be present below deposits previously mined. The Jefferson district also may be underlain by a copper-molybdenum porphyry system related to a buried stock, it too with peripheral high-grade gold deposits. The Bald Mountain Canyon belt of small gold veins has potential for deeper deposits in buried porous ash-flow tuff similar to the huge Round Mountain low-grade gold-silver deposit. Several other areas have potential for a variety of mineral deposits.\r\nAltogether the geochemical, geochronologic, mineralogic, and geologic evidence suggests recurring mineralizing episodes of varied character, from Late Cretaceous to late Tertiary time, related to a long-lived hot spot deep in the crust or in the upper mantle. Granite plutons of Late Cretaceous age were minerali","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf2327C","usgsCitation":"Shawe, D., Hoffman, J.D., Doe, B.R., Foord, E.E., Stein, H., and Ayuso, R.A., 2003, Geochemistry, geochronology, mineralogy, and geology suggest sources of and controls on mineral systems in the southern Toquima Range, Nye County, Nevada (Version 1.0): U.S. Geological Survey Miscellaneous Field Studies Map 2327, https://doi.org/10.3133/mf2327C.","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":110421,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_54745.htm","linkFileType":{"id":5,"text":"html"},"description":"54745"},{"id":191925,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6366,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/mf/2003/mf-2327-c/","linkFileType":{"id":5,"text":"html"}}],"scale":"48000","country":"United States","state":"Nevada","county":"Nye County","otherGeospatial":"southern Toquima Range","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -117.125,38.5 ], [ -117.125,38.75 ], [ -116.75,38.75 ], [ -116.75,38.5 ], [ -117.125,38.5 ] ] ] } } ] }","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ee4b07f02db6a9eb0","contributors":{"authors":[{"text":"Shawe, Daniel R.","contributorId":91448,"corporation":false,"usgs":true,"family":"Shawe","given":"Daniel R.","affiliations":[],"preferred":false,"id":280910,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hoffman, James D. jhoffman@usgs.gov","contributorId":243,"corporation":false,"usgs":true,"family":"Hoffman","given":"James","email":"jhoffman@usgs.gov","middleInitial":"D.","affiliations":[],"preferred":true,"id":280906,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Doe, Bruce R.","contributorId":87554,"corporation":false,"usgs":true,"family":"Doe","given":"Bruce","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":280909,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Foord, Eugene E.","contributorId":96319,"corporation":false,"usgs":true,"family":"Foord","given":"Eugene","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":280911,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Stein, Holly J.","contributorId":46959,"corporation":false,"usgs":true,"family":"Stein","given":"Holly J.","affiliations":[],"preferred":false,"id":280908,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Ayuso, Robert A. 0000-0002-8496-9534 rayuso@usgs.gov","orcid":"https://orcid.org/0000-0002-8496-9534","contributorId":2654,"corporation":false,"usgs":true,"family":"Ayuso","given":"Robert","email":"rayuso@usgs.gov","middleInitial":"A.","affiliations":[{"id":387,"text":"Mineral Resources Program","active":true,"usgs":true},{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":280907,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":50890,"text":"wri034051 - 2003 - Hydrogeology and Ground-Water Quality of Brunswick County, North Carolina","interactions":[],"lastModifiedDate":"2018-05-08T13:41:55","indexId":"wri034051","displayToPublicDate":"2003-06-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2003-4051","title":"Hydrogeology and Ground-Water Quality of Brunswick County, North Carolina","docAbstract":"Brunswick County is the southernmost coastal county in North Carolina and lies in the southeastern part of the Coastal Plain physiographic province. In this report, geologic, hydrologic, and chemical data were used to investigate and delineate the hydrogeologic framework and ground-water quality of Brunswick County. The major aquifers and their associated confining units delineated in the Brunswick County study area include, from youngest to oldest, the surficial, Castle Hayne, Peedee, Black Creek, upper Cape Fear, and lower Cape Fear aquifers.
All of these aquifers, with the exception of the Castle Hayne aquifer, are located throughout Brunswick County. The Castle Hayne aquifer extends across only the southeastern part of the county. Based on available data, the Castle Hayne and Peedee confining units are missing in some areas of Brunswick County, which allows direct hydraulic contact between the surficial aquifer and underlying Castle Hayne or Peedee aquifers. The confining units for the Black Creek, upper Cape Fear, and lower Cape Fear aquifers appear to be continuous throughout Brunswick County.
In examining the conceptual hydrologic system for Brunswick County, a generalized water budget was developed to better understand the natural processes, including precipitation, evapotranspiration, and stream runoff, that influence ground-water recharge to the shallow aquifer system in the county. In the generalized water budget, an estimated 11 inches per year of the average annual precipitation of 55 inches per year in Brunswick County is estimated to infiltrate and recharge the shallow aquifer system. Of the 11 inches per year that recharges the shallow system, about 1 inch per year is estimated to recharge the deeper aquifer system.
The surficial aquifer in Brunswick County is an important source of water for domestic supply and irrigation. The Castle Hayne aquifer is the most productive aquifer and serves as the principal ground-water source of municipal supply for the county. The upper part of the Peedee aquifer is an important source of ground-water supply for domestic and commercial use. Ground water in the lower part of the Peedee aquifer and the underlying aquifers is brackish and is not known to be used as a source of supply in Brunswick County. Most of the precipitation that recharges the surficial aquifer is discharged to local streams that drain into the Waccamaw River, Cape Fear River, and Atlantic Ocean. Recharge to the Castle Hayne aquifer occurs primarily from the surficial aquifer. Recharge to the Peedee aquifer occurs primarily from the surficial and Castle Hayne aquifers, with some upward leakage of water also occurring from the underlying Black Creek aquifer. Discharge from the Castle Hayne and Peedee aquifers occurs to local streams, the Cape Fear River, and the Atlantic Ocean.
Evaluation of water-level data for the period January 1970 through May 2002 indicated no apparent long-term temporal trends in water levels in the surficial and Castle Hayne aquifers and in the upper part of the Peedee aquifer. The most significant water-level trends were noted for wells tapping the lower part of the Peedee aquifer and tapping the Black Creek aquifer where water levels have declined as much as 41 and 37 feet, respectively. These ground-water-level declines are attributed to regional ground-water pumping in areas outside of Brunswick County. Water-level data for Brunswick County wells tapping the upper Cape Fear and lower Cape Fear aquifers tend to fluctuate within a fairly uniform range with no apparent temporal trend noted. Analysis of vertical hydraulic gradients during this same period primarily indicate downward flow of ground water within and among the surficial, Castle Hayne, and Peedee aquifers. The vertical flow of ground water in the Black Creek aquifer is upward into the overlying Peedee aquifer. Upward flow also is noted for the upper and lower Cape Fear aquifers.
Historic and recent analytic data were evaluated to better understand the sources of water contained in Brunswick County aquifers and the suitability of the water for consumption. Based on analytical results obtained for recent samples collected during this study, ground water from the surficial aquifer, Castle Hayne aquifer, and upper part of the Peedee aquifer appears to be generally suitable for drinking water. Although concentrations of iron and manganese commonly exceeded the drinking-water standards, the concern generally associated with the occurrence of these analytes in a water supply is one of aesthetics. In all samples, nitrate, nitrite, and sulfate were detected at concentrations less than drinkingwater standards.
Based on historic analytical data, the brackish water in the lower part of the Peedee aquifer and in the Black Creek, upper Cape Fear, and lower Cape Fear aquifers is classified as a sodium-chloride type water. The presence of brackish water in these deeper systems combined with upward vertical gradients presents the potential for upward migration of brackish water into overlying aquifers, or upconing beneath areas of pumping. The current (2001) location of the boundary between freshwater and brackish water in Brunswick County aquifers is unknown.
","language":"English","publisher":"U.S Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri034051","collaboration":"Prepared in cooperation with the Brunswick County, North Carolina","usgsCitation":"Harden, S.L., Fine, J.M., and Spruill, T.B., 2003, Hydrogeology and Ground-Water Quality of Brunswick County, North Carolina: U.S. Geological Survey Water-Resources Investigations Report 2003-4051, Report: vi, 90 p.; 9 Plates, https://doi.org/10.3133/wri034051.","productDescription":"Report: vi, 90 p.; 9 Plates","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":353461,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051_BrunswickPlate8.pdf","text":"Plate 8","size":"4.93 MB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"- Plate 8. Maps Showing Altitude of Top of Aquifer and Confining Unit, and Thickness of Confining Unit for the (A-C) Castle Hayne, (D-F) Peedee, and (G-I) Black Creek Aquifers in Brunswick County, North Carolina"},{"id":353462,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051_BrunswickPlate9.pdf","text":"Plate 9","size":"3.82 MB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"- Plate 9. Maps Showing Altitude of Top of Aquifer and Confining Unit, and Thickness of Confining Unit for the (A-C) Upper Cape Fear, (D-F) Peedee, and (G-I) Lower Cape Fear Aquifers , and (G) The Alktitude of Basement Rocks in Brunswick County, North Carolina"},{"id":353458,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051__BrunswickPlate5.pdf","text":"Plate 5","size":"1.10 MB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"- Plate 5. Hydrogeologic Section E-E', Brunswick County, North Carolina"},{"id":353459,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051_BrunswickPlate6.pdf","text":"Plate 6","size":"1.49 MB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"- Plate 6. Hydrogeologic Section F-F', Brunswick County, North Carolina"},{"id":353460,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051_BrunswickPlate7.pdf","text":"Plate 7","size":"1.31 MB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"- Plate 7. Hydrogeologic Section G-G', Brunswick County, North Carolina"},{"id":86378,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051.pdf","text":"Report","size":"7.80 MB ","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2003-4051"},{"id":353454,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051_BrunswickPlate1.pdf","text":"Plate 1","size":"742 KB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"- Plate 1. Hydrogeologic Section A-A', Brunswick County, North Carolina"},{"id":353455,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051_BrunswickPlate2.pdf","text":"Plate 2","size":"905 KB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"- Plate 2. Hydrogeologic Section B-B', Brunswick County, North Carolina"},{"id":353456,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051_BrunswickPlate3.pdf","text":"Plate 3","size":"891 KB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"- Plate 3. Hydrogeologic Section C-C', Brunswick County, North Carolina"},{"id":353457,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2003/4051/wri20034051_BrunswickPlate4.pdf","text":"Plate 4","size":"1 MB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"- Plate 4. 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U.S. Geological Survey
720 Gracern Road
Columbia, SC 29210
The relations among stream habitat and hydrologic conditions were investigated in the Usquepaug–Queen River Basin in southern Rhode Island. Habitats were assessed at 13 sites on the mainstem and tributaries from July 1999 to September 2000. Channel types are predominantly low-gradient glides, pools, and runs that have a sand and gravel streambed and a forest or shrub riparian zone. Along the stream margins, overhanging brush, undercut banks supported by roots, and downed trees create cover; within the channel, submerged aquatic vegetation and woody debris create cover. These habitat features decrease in quality and availability with declining streamflows, and features along stream margins generally become unavailable once streamflows drop to the point at which water recedes from the stream banks. Riffles are less common, but were identified as critical habitat areas because they are among the first to exhibit habitat losses or become unavailable during low-flow periods. Stream-temperature data were collected at eight sites during summer 2000 to indicate the suitability of those reaches for cold-water fish communities. Data indicate stream temperatures provide suitable habitat for cold-water species in the Fisherville and Locke Brook tributaries and in the mainstem Queen River downstream of the confluence with Fisherville Brook. Stream temperatures in the Usquepaug River downstream from Glen Rock Reservoir are about 6°F warmer than in the Queen River upstream from the impoundment. These warmer temperatures may make habitat in the Usquepaug River marginal for cold-water species.
Fish-community composition was determined from samples collected at seven sites on tributaries and at three sites on the mainstem Usquepaug–Queen River. Classification of the fish into habitat-use groups and comparison to target fish communities developed for the Quinebaug and Ipswich Rivers indicated that the sampled reaches of the Usquepaug–Queen River contained most of the riverine fish species that would have been expected to occur in this area.
Streamflow records from the gaging station Usquepaug River near Usquepaug were used to (1) determine streamflow requirements for habitat protection by use of the Tennant method, and (2) define a flow regime that mimics the river's natural flow regime by use of the Range of Variability Approach. The Tennant streamflow requirement, defined as 30 percent of the mean annual flow, was 0.64 cubic feet per second per square mile (ft3/s/mi2). This requirement should be considered an initial estimate because flows measured at the Usquepaug River gaging station are reduced by water withdrawals upstream from the gage. The streamflow requirements may need to be revised once a watershed-scale precipitationrunoff model of the Usquepaug River is complete
and a simulation of streamflows without water withdrawals has been determined.
The subsurface transport of phosphorus introduced by the disposal of treated sewage effluent to ground-infiltration disposal beds at the Massachusetts Military Reservation on western Cape Cod was simulated with a three-dimensional reactive-transport model. The simulations were used to estimate the load of phosphorus transported to Ashumet Pond during operation of the sewage-treatment plant from 1936 to 1995 and for 60 years following cessation of sewage disposal. The model accounted for spatial and temporal changes in water discharge from the sewage-treatment plant, ground-water flow, transport of associated chemical constituents, and a set of chemical reactions, including phosphorus sorption on aquifer materials, dissolution and precipitation of iron- and manganese-oxyhydroxide and iron phosphate minerals, organic carbon sorption and decomposition, cation sorption, and irreversible denitrification. The flow and transport in the aquifer were simulated by using parameters consistent with those used in previous flow models of this area of Cape Cod, except that numerical dispersion was much larger than the physical dispersion estimated in previous studies. Sorption parameters were fit to data derived from phosphorus sorption and desorption laboratory column experiments. Rates of organic carbon decomposition were adjusted to match the location of iron concentrations in an anoxic iron zone within the sewage plume. The sensitivity of the simulated load of phosphorus transported to Ashumet Pond was calculated for a variety of processes and input parameters. Model limitations included large uncertainties associated with the loading of the sewage beds, the flow system, and the chemistry and sorption characteristics in the aquifer. The results of current model simulations indicate a small load of phosphorus transported to Ashumet Pond during 1965-85, but this small load was particularly sensitive to model parameters that specify flow conditions and the chemical process by which non-desorbable phosphorus is incorporated in the sediments. The uncertainties were large enough to make it difficult to determine whether loads of phosphorus transported to Ashumet Pond in the 1990s were greater or less than loads during the previous two decades. The model simulations indicate substantial discharge of phosphorus to Ashumet Pond after about 1965. After the period 2000-10 the simulations indicate that the load of phosphorus transported to Ashumet Pond decreases continuously, but the load of phosphorus remains substantial for many decades. The current simulations indicate a peak in phosphorus discharge to Ashumet Pond of about 1,000 kilograms per year during the 1990s; however, comparisons of simulated phosphorus concentrations with measured concentrations in 1993 indicate that the peak in phosphorus load transported to Ashumet Pond may be larger and moving more quickly in the model simulations than in the aquifer. The results of the three-dimensional reactive-transport simulations are consistent with the loading history, experimental laboratory data, and field measurements. The results of the simulations adequately reproduce the spatial distribution of phosphorus concentrations measured in 1993, the magnitude of changes in phosphorus concentration with time in a profile near the disposal beds following cessation of sewage disposal, the observed iron zone in the sewage plume, the approximate flow of treated sewage effluent into Ashumet Valley, and laboratory-column data for phosphorus sorption and desorption.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri034017","usgsCitation":"Parkhurst, D.L., Stollenwerk, K.G., and Colman, J.A., 2003, Reactive-transport simulation of phosphorus in the sewage plume at the Massachusetts Military Reservation, Cape Cod, Massachusetts: U.S. Geological Survey Water-Resources Investigations Report 2003-4017, v, 33 p. , https://doi.org/10.3133/wri034017.","productDescription":"v, 33 p. ","costCenters":[{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":179650,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":4623,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri034017/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Massachusetts ","otherGeospatial":"Cape Cod","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -70.7958984375,\n 41.582579601430346\n ],\n [\n -69.85107421874999,\n 41.582579601430346\n ],\n [\n -69.85107421874999,\n 42.21224516288584\n ],\n [\n -70.7958984375,\n 42.21224516288584\n ],\n [\n -70.7958984375,\n 41.582579601430346\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db6486dc","contributors":{"authors":[{"text":"Parkhurst, David L. 0000-0003-3348-1544 dlpark@usgs.gov","orcid":"https://orcid.org/0000-0003-3348-1544","contributorId":1088,"corporation":false,"usgs":true,"family":"Parkhurst","given":"David","email":"dlpark@usgs.gov","middleInitial":"L.","affiliations":[{"id":5044,"text":"National Research Program - Central Branch","active":true,"usgs":true}],"preferred":true,"id":242455,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stollenwerk, Kenneth G. kgstolle@usgs.gov","contributorId":578,"corporation":false,"usgs":true,"family":"Stollenwerk","given":"Kenneth","email":"kgstolle@usgs.gov","middleInitial":"G.","affiliations":[],"preferred":true,"id":242454,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Colman, John A. 0000-0001-9327-0779 jacolman@usgs.gov","orcid":"https://orcid.org/0000-0001-9327-0779","contributorId":2098,"corporation":false,"usgs":true,"family":"Colman","given":"John","email":"jacolman@usgs.gov","middleInitial":"A.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true},{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true}],"preferred":true,"id":242456,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":47774,"text":"wri034001 - 2003 - Two-station comparison of peak flows to improve flood-frequency estimates for seven streamflow-gaging stations in the Salmon and Clearwater River Basins, Central Idaho","interactions":[],"lastModifiedDate":"2012-12-06T12:08:05","indexId":"wri034001","displayToPublicDate":"2003-05-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2003-4001","title":"Two-station comparison of peak flows to improve flood-frequency estimates for seven streamflow-gaging stations in the Salmon and Clearwater River Basins, Central Idaho","docAbstract":"Improved flood-frequency estimates for short-term (10 or fewer years of record) streamflow-gaging stations were needed to support instream flow studies by the U.S. Forest Service, which are focused on quantifying water rights necessary to maintain or restore productive fish habitat. Because peak-flow data for short-term gaging stations can be biased by having been collected during an unusually wet, dry, or otherwise unrepresentative period of record, the data may not represent the full range of potential floods at a site. To test whether peak-flow estimates for short-term gaging stations could be improved, the two-station comparison method was used to adjust the logarithmic mean and logarithmic standard deviation of peak flows for seven short-term gaging stations in the Salmon and Clearwater River Basins, central Idaho. Correlation coefficients determined from regression of peak flows for paired short-term and long-term (more than 10 years of record) gaging stations over a concurrent period of record indicated that the mean and standard deviation of peak flows for all short-term gaging stations would be improved. Flood-frequency estimates for seven short-term gaging stations were determined using the adjusted mean and standard deviation. The original (unadjusted) flood-frequency estimates for three of the seven short-term gaging stations differed from the adjusted estimates by less than 10 percent, probably because the data were collected during periods representing the full range of peak flows. Unadjusted flood-frequency estimates for four short-term gaging stations differed from the adjusted estimates by more than 10 percent; unadjusted estimates for Little Slate Creek and Salmon River near Obsidian differed from adjusted estimates by nearly 30 percent. These large differences probably are attributable to unrepresentative periods of peak-flow data collection.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri034001","collaboration":"Prepared in cooperation with the U.S. Forest Service","usgsCitation":"Berenbrock, C., 2003, Two-station comparison of peak flows to improve flood-frequency estimates for seven streamflow-gaging stations in the Salmon and Clearwater River Basins, Central Idaho: U.S. Geological Survey Water-Resources Investigations Report 2003-4001, iii, 27 p., https://doi.org/10.3133/wri034001.","productDescription":"iii, 27 p.","numberOfPages":"31","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":262366,"rank":800,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2003/4001/report.pdf"},{"id":262367,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2003/4001/report-thumb.jpg"}],"country":"United States","state":"Idaho","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -117.0436,43.8741 ], [ -117.0436,47.1367 ], [ -112.9881,47.1367 ], [ -112.9881,43.8741 ], [ -117.0436,43.8741 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a48e4b07f02db623743","contributors":{"authors":[{"text":"Berenbrock, Charles","contributorId":30598,"corporation":false,"usgs":true,"family":"Berenbrock","given":"Charles","email":"","affiliations":[],"preferred":false,"id":236207,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47788,"text":"wri024183 - 2003 - Occurrence and transport of cadmium, lead, and zinc in the Spokane River basin, Idaho and Washington, water years 1999-2001","interactions":[],"lastModifiedDate":"2013-11-21T12:58:33","indexId":"wri024183","displayToPublicDate":"2003-05-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4183","title":"Occurrence and transport of cadmium, lead, and zinc in the Spokane River basin, Idaho and Washington, water years 1999-2001","docAbstract":"A water-quality investigation of the Clark\nFork-Pend Oreille and Spokane River Basins began\nin 1997 as part of the U.S. Geological Survey\nNational Water-Quality Assessment Program. As\npart of the investigation, selected streams in the\nSpokane River Basin were sampled for trace metals\nduring water years 1999–2001. These data,\ncombined with data collected as part of a U.S.\nEnvironmental Protection Agency Remedial Investigation/\nFeasibility Study, were used to assess the\noccurrence, loads, and transport of cadmium, lead,\nand zinc at 21 streamflow-gaging stations in the\nSpokane River Basin.\nConcentrations of dissolved and total cadmium,\nlead, and zinc varied widely both at and\namong stations. At most stations, dissolved cadmium\nand zinc composed most of the total concentrations;\ndissolved lead generally composed less\nthan 10 percent of the total lead concentration.\nFrom the South Fork Coeur d’Alene River near\nMullan downstream to the South Fork Coeur\nd’Alene River near Pinehurst, concentrations of\ntrace metals increased 2 to 4 orders of magnitude.\nThe mean flow-weighted concentrations of total\ncadmium, lead, and zinc near Pinehurst for water\nyears 1999–2001 were 5.7, 80, and 810 micrograms\nper liter (\nµg/L), respectively. On the Coeur\nd’Alene River near Harrison, downstream from the\nconfluence of the metal-enriched South Fork and\nthe relatively dilute North Fork Coeur d’Alene\nRiver, the mean flow-weighted concentrations of\ntotal cadmium, lead, and zinc were 1.6, 88, and\n240\nµg/L, respectively. Trace-metal concentrations\nwere smaller in the Spokane River than in the\nCoeur d’Alene River because of dilution and\nretention in Coeur d’Alene Lake. The mean flowweighted\nconcentrations of total cadmium, lead,\nand zinc in the Spokane River near Post Falls were\n0.32, 3.1, and 71\nµg/L, respectively.\nRegression models relating the mass transport,\nor load, of trace metals to changes in stream\ndischarge and time were successful in simulating\nthe variability in trace-metal concentrations and\nloads. The median coefficient of determination for\nthe load models for the 21 stations was largest for\ntotal lead (92 percent) and smallest for dissolved\nand total cadmium (82 percent). Whereas most of\nthe cadmium and zinc loads in the Spokane River\nBasin were derived from the South Fork Coeur\nd’Alene River, most of the lead load was derived\nfrom the Coeur d’Alene River downstream from\nthe confluence of the North and South Forks. Major\ntributary sources of trace metals to the South Fork\nCoeur d’Alene River were Canyon Creek, Ninemile\nCreek, and Government Gulch. These three\ntributaries contributed about 3,000 pounds of cadmium,\n23,000 pounds of lead, and 310,000 pounds\nof zinc annually to the South Fork Coeur d’Alene\nRiver. Erosion and transport of sediment-bound\nlead in the Coeur d’Alene River was the primary\nsource of total lead, accounting for almost\n400,000 pounds annually during water years\n1999–2000. Ground-water discharge in the area of\nthe Bunker Hill Superfund site was a major source\nof zinc in the South Fork Coeur d’Alene River,\ncontributing more than 250,000 pounds per year.\nDuring water years 1999–2000, the average\nannual loads of cadmium, lead, and zinc transported\nfrom the Coeur d’Alene, St. Joe, and St.\nMaries Rivers to Coeur d’Alene Lake were 8,900, 500,000, and 1.4 million pounds, respectively.\nThe Coeur d’Alene River accounted for more than\n99 percent of the total load of each of these three\nmetals entering the lake. About 4,600 pounds of\ncadmium, 44,000 pounds of lead, and 980,000\npounds of zinc were transported from Coeur\nd’Alene Lake into the Spokane River. Between the\nSpokane River near Post Falls, Idaho, and the Spokane\nRiver at Long Lake, Washington, there was\nan annual net loss of about 2,600, 20,000, and\n250,000 pounds of cadmium, lead, and zinc,\nrespectively. About 2,000 pounds of cadmium,\n24,000 pounds of lead, and 730,000 pounds of\nzinc were transported annually downstream from\nLong Lake toward the Columbia River.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri024183","usgsCitation":"Clark, G.M., 2003, Occurrence and transport of cadmium, lead, and zinc in the Spokane River basin, Idaho and Washington, water years 1999-2001: U.S. Geological Survey Water-Resources Investigations Report 2002-4183, vi, 37 p., https://doi.org/10.3133/wri024183.","productDescription":"vi, 37 p.","numberOfPages":"45","temporalStart":"1998-10-01","temporalEnd":"2001-09-30","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":262368,"rank":800,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2002/4183/report.pdf"},{"id":262369,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2002/4183/report-thumb.jpg"}],"scale":"1000000","country":"United States","state":"Idaho;Washington","county":"Lincoln;Stevens;Spokane;Kootenai;Benewah;Shoshone","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -118.4334,46.9464 ], [ -118.4334,48.081 ], [ -115.1853,48.081 ], [ -115.1853,46.9464 ], [ -118.4334,46.9464 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afbe4b07f02db6961ff","contributors":{"authors":[{"text":"Clark, Gregory M. gmclark@usgs.gov","contributorId":1377,"corporation":false,"usgs":true,"family":"Clark","given":"Gregory","email":"gmclark@usgs.gov","middleInitial":"M.","affiliations":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"preferred":true,"id":236238,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47779,"text":"wri034016 - 2003 - Simulation of ground-water flow and land subsidence in the Antelope Valley ground-water basin, California","interactions":[],"lastModifiedDate":"2012-02-02T00:10:41","indexId":"wri034016","displayToPublicDate":"2003-05-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2003-4016","title":"Simulation of ground-water flow and land subsidence in the Antelope Valley ground-water basin, California","docAbstract":"Antelope Valley, California, is a topographically closed basin in the western part of the Mojave Desert, about 50 miles northeast of Los Angeles. The Antelope Valley ground-water basin is about 940 square miles and is separated from the northern part of Antelope Valley by faults and low-lying hills. Prior to 1972, ground water provided more than 90 percent of the total water supply in the valley; since 1972, it has provided between 50 and 90 percent. Most ground-water pumping in the valley occurs in the Antelope Valley ground-water basin, which includes the rapidly growing cities of Lancaster and Palmdale. Ground-water-level declines of more than 200 feet in some parts of the ground-water basin have resulted in an increase in pumping lifts, reduced well efficiency, and land subsidence of more than 6 feet in some areas. Future urban growth and limits on the supply of imported water may continue to increase reliance on ground water. To better understand the ground-water flow system and to develop a tool to aid in effectively managing the water resources, a numerical model of ground-water flow and land subsidence in the Antelope Valley ground-water basin was developed using old and new geohydrologic information.\r\n\r\n\r\nThe ground-water flow system consists of three aquifers: the upper, middle, and lower aquifers. The aquifers, which were identified on the basis of the hydrologic properties, age, and depth of the unconsolidated deposits, consist of gravel, sand, silt, and clay alluvial deposits and clay and silty clay lacustrine deposits. Prior to ground-water development in the valley, recharge was primarily the infiltration of runoff from the surrounding mountains. Ground water flowed from the recharge areas to discharge areas around the playas where it discharged either from the aquifer system as evapotranspiration or from springs. Partial barriers to horizontal ground-water flow, such as faults, have been identified in the ground-water basin. Water-level declines owing to ground-water development have eliminated the natural sources of discharge, and pumping for agricultural and urban uses have become the primary source of discharge from the ground-water system. Infiltration of return flows from agricultural irrigation has become an important source of recharge to the aquifer system.\r\n\r\n\r\nThe ground-water flow model of the basin was discretized horizontally into a grid of 43 rows and 60 columns of square cells 1 mile on a side, and vertically into three layers representing the upper, middle, and lower aquifers. Faults that were thought to act as horizontal-flow barriers were simulated in the model. The model was calibrated to simulate steady-state conditions, represented by 1915 water levels and transient-state conditions during 1915-95 using water-level and subsidence data. Initial estimates of the aquifer-system properties and stresses were obtained from a previously published numerical model of the Antelope Valley ground-water basin; estimates also were obtained from recently collected hydrologic data and from results of simulations of ground-water flow and land subsidence models of the Edwards Air Force Base area. Some of these initial estimates were modified during model calibration. Ground-water pumpage for agriculture was estimated on the basis of irrigated crop acreage and crop consumptive-use data. Pumpage for public supply, which is metered, was compiled and entered into a database used for this study. Estimated annual pumpage peaked at 395,000 acre-feet (acre-ft) in 1952 and then declined because of declining agricultural production. Recharge from irrigation-return flows was estimated to be 30 percent of agricultural pumpage; the irrigation-return flows were simulated as recharge to the regional water table 10 years following application at land surface. The annual quantity of natural recharge initially was based on estimates from previous studies. During model calibration, natural recharge was reduced from the initial","language":"ENGLISH","doi":"10.3133/wri034016","usgsCitation":"Leighton, D.A., and Phillips, S.P., 2003, Simulation of ground-water flow and land subsidence in the Antelope Valley ground-water basin, California: U.S. Geological Survey Water-Resources Investigations Report 2003-4016, 118 p., https://doi.org/10.3133/wri034016.","productDescription":"118 p.","costCenters":[],"links":[{"id":3991,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri034016","linkFileType":{"id":5,"text":"html"}},{"id":171789,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b06e4b07f02db69a20d","contributors":{"authors":[{"text":"Leighton, David A.","contributorId":95493,"corporation":false,"usgs":true,"family":"Leighton","given":"David","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":236218,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Phillips, Steven P. 0000-0002-5107-868X sphillip@usgs.gov","orcid":"https://orcid.org/0000-0002-5107-868X","contributorId":1506,"corporation":false,"usgs":true,"family":"Phillips","given":"Steven","email":"sphillip@usgs.gov","middleInitial":"P.","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":236217,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}