Ground water was sampled in a 900-square-mile agricultural area in the Pasco Basin, which includes parts of eastern Benton County and western Franklin County, Washington, to determine distributions of nitrate and fluoride. Additional data were obtained to determine if fertilizers, irrigation water, septic systems, and naturally occurring nitrate are sources of nitrate in ground water. Limited sampling also was done to determine if pesticides were present in the ground water.
Nitrate concentrations in ground water ranged from less than 0.1 to 100 milligrams per liter as nitrogen, and median concentrations of nitrate nitrogen in ground water were 3.2 and 6.7 milligrams per liter for Benton and Franklin Counties, respectively. In Franklin County, where a large percentage of the land is used for irrigated agriculture, nitrate nitrogen concentrations in water from 31 percent of sampled wells were equal to or greater than the maximum contaminant level for drinking water of 10 milligrams per liter. In Benton County, nitrate concentrations in water from about 10 percent of the sampled wells exceeded the maximum contaminant level.
Nitrate concentrations in ground water at some locations in Franklin County have increased by as much as two orders of magnitude since the early 1950's. Historical data generally were not available to evaluate changes of nitrate concentrations in ground water in Benton County, except for the area around the town of Finley. A comparison of data collected during this study with data collected during 1976-77 indicate that nitrate concentrations in ground water of the Finley area probably have not changed over the intervening period.
Applied nitrogen fertilizers are a major source of nitrate in ground water at many locations in the study area. Surface water used for irrigation does not contain sufficient nitrate to cause elevated concentrations in ground water. Instead, canal seepage, which makes up about 50 percent of the ground-water recharge in the study area, tends to dilute the nitrate present in ground water.
Septic systems in the Finley area of Benton County are a source of nitrate in ground water, but analyses of data and results of a numerical model analysis of nitrate concentrations in the unconfmed ground-water system indicate that they are not the primary source of nitrate in ground water in this area.
Naturally occurring nitrate may be a source of nitrate in ground water underlying Badger Coulee in Benton County. Average masses of natural nitrate per unit volume of sediment in two boreholes in Badger Coulee were equivalent to 2,590 and 964 pounds of nitrogen, respectively, in a block of sediments 50 feet thick underlying an acre of land. At most other locations in the study area, the amount of natural nitrate in ground water is probably small compared with nitrate from anthropogenic sources.
Fluoride concentrations in ground water in the study area ranged from less than 0.1 to 4.7 milligrams per liter; the median concentration was 0.5 milligram per liter. The concentration of fluoride in water from only two of 143 wells equalled or exceeded 2.0 milligrams per liter, which is the secondary maximum contaminant level for drinking water. Both are deep wells open to the Saddle Mountains Basalt in Franklin County. Large concentrations of fluoride in deep ground waters of the Pasco Basin are apparently the result of natural conditions in the deeper basalt aquifers.
One or more pesticide compounds were detected in 10 of 29 ground-water samples, which were analyzed for selected chlorophenoxy acid herbicides, triazine herbicides, carbamate insecticides, organophosphorus insecticides, and a few other types of pesticides. The sampling locations did not represent a random distribution, but instead, most were wells open to unconfined, shallow ground water in irrigated areas. The pesticides found include the herbicides atrazine, dicamba, metribuzin, picloram, and 2,4,5-T. Also present were aldicarb sulfone and aldicarb sulfoxide, which are degradation products of the insecticide aldicarb. Except for metribuzin, pesticide concentrations were at or near the analytical reporting limits. In all instances, the concentrations of pesticides detected were below the health advisory levels that are issued by the U.S. Environmental Protection Agency
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri934197","collaboration":"Prepared in cooperation with the Washington State Department of Ecology","usgsCitation":"Ebbert, J., Cox, S., Drost, B., and Schurr, K., 1995, Distribution and sources of nitrate, and presence of fluoride and pesticides, in parts of the Pasco Basin, Washington, 1986-88: U.S. Geological Survey Water-Resources Investigations Report 93-4197, Report: vii, 173 p.; 3 Plates: 48.32 x 35.45 inches or smaller, https://doi.org/10.3133/wri934197.","productDescription":"Report: vii, 173 p.; 3 Plates: 48.32 x 35.45 inches or smaller","costCenters":[],"links":[{"id":424442,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_47890.htm","linkFileType":{"id":5,"text":"html"}},{"id":351279,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1993/4197/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":351278,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1993/4197/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":351277,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1993/4197/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":118815,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1993/4197/report-thumb.jpg"},{"id":54184,"rank":5,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1993/4197/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Washington","otherGeospatial":"Pasco Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -118.44859231635866,\n 47.54198150754928\n ],\n [\n -119.84390781849129,\n 47.54198150754928\n ],\n [\n -119.84390781849129,\n 46.0060605168527\n ],\n [\n -118.44859231635866,\n 46.0060605168527\n ],\n [\n -118.44859231635866,\n 47.54198150754928\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5fe4b07f02db6348c1","contributors":{"authors":[{"text":"Ebbert, J.C.","contributorId":57451,"corporation":false,"usgs":true,"family":"Ebbert","given":"J.C.","affiliations":[],"preferred":false,"id":193753,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cox, S.E.","contributorId":66663,"corporation":false,"usgs":true,"family":"Cox","given":"S.E.","email":"","affiliations":[],"preferred":false,"id":193754,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Drost, B. 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These four States, which comprise Segment 2 of this Atlas, are located in the Southwestern United States and extend from the rolling grasslands of the Great Plains on the east across the Rocky Mountains and Continental Divide to the desert basins of the Southwest. The 425,000-square-mile area ranges in altitude from about 14,400 feet above sea level in the Rocky Mountains of Colorado to about 100 feet near the lower Colorado River in southwestern Arizona. All the ground water in Segment 2 ultimately is derived from infiltration of precipitation, which varies considerably with the altitude and topography of the area.
The Great Plains Physiographic Province of the Central United States extends into eastern Colorado and New Mexico (fig. 1), where flat to rolling prairie (fig. 2) with scattered hills and bluffs gradually rises westward to 5,000 to 7,000 feet above sea level and abruptly gives way to the frontal ranges of the Rocky Mountains in the Southern Rocky Mountain and Basin and Range Physiographic Provinces. West of the frontal ranges in Colorado and northern New Mexico are additional and higher mountain ranges generally oriented north-south but with many spurs and extensions oriented in other directions. The many ranges of the Rocky Mountains are separated by valleys and high mountain parks (fig. 3). Colorado contains about three-fourths of the Nation's land area above 10,000 feet and has 53 mountain peaks higher than 14,000 feet. Most of these high peaks are located near the Continental Divide (fig. 1), which extends approximately north-south through central Colorado and western New Mexico. The altitude of the divide decreases in southern New Mexico to less than 4,500 feet in a few areas.
Farther westward, the mountains are less prevalent and are interspersed with broad structural basins. These basins and the broad valleys of the middle Colorado River and its tributaries form the irregular intermontane topography of the Colorado Plateaus Physiographic Province (fig. 4). Plateaus and high mesas are formed where the surface has been dissected by rugged canyons carved by the Colorado River and its tributaries (fig. 5). The largest of these canyons-the Grand Canyon-extends about 220 miles southwestward from the mouth of the Little Colorado River in Arizona and ranges from 4 to 18 miles in width and from 2,700 to 5,700 feet in depth below the rim.
Small mountain ranges and intervening broad desert valleys of the Basin and Range Physiographic Province are prevalent to the west and south of the Colorado Plateaus in western Utah, southern Arizona, and southern New Mexico (fig. 1). These mountain ranges generally protrude 3,000 to 6,000 feet above the surrounding valley floor (fig. 6) and commonly extend from 20 to 50 miles in a north or northwesterly direction.
Small parts of the Middle Rocky Mountains and Wyoming Basin Physiographic Provinces extend into northwestern Colorado and northeastern Utah (fig. 1). The topography, geology, and hydrology of the two areas are described in Chapter 1 of this Atlas.
Four of the Nation's major river systems have headwaters in the mountainous areas of Segment 2. The South Platte River of the Missouri River system drains the eastern slope of northern Colorado; the Arkansas River and its tributary, the Canadian River, drain southeastern Colorado and northeastern New Mexico; the Rio Grande and its tributary, the Pecos River, drain south-central Colorado and central New Mexico; and the Colorado River and its tributaries drain Arizona, eastern Utah, Northwestern New Mexico, and western Colorado (fig. 1). Western Utah is drained by numerous streams that terminate in local desert basins, the Great Salt Lake, or other local lakes and reservoirs. Because the Great Salt Lake lies in the Great Basin, which is the largest closed basin in North America, it has no outlet to the sea. The salinity of the lake water is about 20 percent or about 6 times the salinity of seawater.
Most of Segment 2 is sparsely populated. The average population density of counties is less than 8 persons per square mile in about 65 percent of the four-State area (fig. 7). Population densities range from less than 0.5 person per square mile in a few rural counties to more than 4 ,000 persons per square mile in populous urban areas. The 1990 population of the four States was about 10 million; almost 70 percent of this population was in Arizona and Colorado. Most land in Segment 2 is undeveloped forest grassland, or desert shrubland, much of which is used for livestock grazing. Land used for production of commercial crops primarily is in eastern Colorado and eastern New Mexico.
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Nevada"},"predicate":"IS_PART_OF","object":{"id":68687,"text":"ha730 - 2000 - Ground Water Atlas of the United States","indexId":"ha730","publicationYear":"2000","noYear":false,"title":"Ground Water Atlas of the United States"},"id":1}],"isPartOf":{"id":68687,"text":"ha730 - 2000 - Ground Water Atlas of the United States","indexId":"ha730","publicationYear":"2000","noYear":false,"title":"Ground Water Atlas of the United States"},"lastModifiedDate":"2017-05-30T15:09:11","indexId":"ha730B","displayToPublicDate":"1996-10-01T00:00:00","publicationYear":"1995","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"730","chapter":"B","title":"Ground Water Atlas of the United States: Segment 1, California, Nevada","docAbstract":"California and Nevada compose Segment 1 of the Ground Water Atlas of the United States. Segment 1 is a region of pronounced physiographic and climatic contrasts. From the Cascade Mountains and the Sierra Nevada of northern California, where precipitation is abundant, to the Great Basin in Nevada and the deserts of southern California, which have the most arid environments in the United States, few regions exhibit such a diversity of topography or environment.
Since the discovery of gold in the mid-1800's, California has experienced a population, industrial, and agricultural boom unrivaled by that of any other State. Water needs in California are very large, and the State leads the United States in agricultural and municipal water use. The demand for water exceeds the natural water supply in many agricultural and nearly all urban areas. As a result, water is impounded by reservoirs in areas of surplus and transported to areas of scarcity by an extensive network of aqueducts.
Unlike California, which has a relative abundance of water, development in Nevada has been limited by a scarcity of recoverable freshwater. The Truckee, the Carson, the Walker, the Humboldt, and the Colorado Rivers are the only perennial streams of significance in the State. The individual basin-fill aquifers, which together compose the largest known ground-water reserves, receive little annual recharge and are easily depleted. Nevada is sparsely populated, except for the Las Vegas, the Reno-Sparks, and the Carson City areas, which rely heavily on imported water for public supplies. Although important to the economy of Nevada, agriculture has not been developed to the same degree as in California due, in large part, to a scarcity of water. Some additional ground-water development might be possible in Nevada through prudent management of the basin-fill aquifers and increased utilization of ground water in the little-developed carbonate-rock aquifers that underlie the eastern one-half of the State. The potential problem of withdrawals in excess of natural recharge, however, will require careful management of ground-water withdrawals.
","largerWorkTitle":"Ground Water Atlas of the United States","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ha730B","isbn":"0607767553","usgsCitation":"Planert, M., and Williams, J.S., 1995, Ground Water Atlas of the United States: Segment 1, California, Nevada: U.S. Geological Survey Hydrologic Atlas 730, 28 p., https://doi.org/10.3133/ha730B.","productDescription":"28 p.","startPage":"B1","endPage":"B28","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":186225,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ha/730b/report-thumb.jpg"},{"id":11479,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/ha/ha730/ch_b/index.html","linkFileType":{"id":5,"text":"html"}},{"id":115250,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/ha/730b/report.pdf","text":"Report","size":"68.30 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab1e4b07f02db66de79","contributors":{"authors":[{"text":"Planert, Michael","contributorId":56659,"corporation":false,"usgs":true,"family":"Planert","given":"Michael","email":"","affiliations":[],"preferred":false,"id":277623,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Williams, John S. johnw@usgs.gov","contributorId":329,"corporation":false,"usgs":true,"family":"Williams","given":"John","email":"johnw@usgs.gov","middleInitial":"S.","affiliations":[],"preferred":true,"id":277622,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":27873,"text":"wri954194 - 1995 - Ground-water levels and directions of flow in Geauga County, Ohio, September 1994, and changes in ground-water levels, 1986-94","interactions":[],"lastModifiedDate":"2018-10-05T09:38:15","indexId":"wri954194","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1995","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":"95-4194","title":"Ground-water levels and directions of flow in Geauga County, Ohio, September 1994, and changes in ground-water levels, 1986-94","docAbstract":"This report presents the results of a study by the U.S. Geological Survey, in cooperation with the Geauga County Planning Commission and Board of County Commissioners, to determine directions of ground-water flow and to assess differences from 1986 to 1994 in groundwater levels in the glacial deposits and Pottsville Formation, Cuyahoga Group, and the Berea Sandstone. Water levels were measured in 219 wells in Geauga County, Ohio, in September 1994. Water levels measured in January and February 1986 in 88 of the 219 wells were used for comparison.
Water-level maps constructed from measurements made in September 1994 show that ground-water levels in the Pottsville Formation and the glacial deposits generally correspond to the land-surface configuration and that ground water flows from the uplands to adjacent streams and buried valleys. Ground-water flow in the Cuyahoga Group is generally downward from the Pottsville Formation to the Berea Sandstone. Directions of ground-water flow in the Berea Sandstone are toward outcrop areas at the north and east edges of Geauga County and toward subcrops beneath buried glacial valley deposits in Chardon, Chester, Munson, and Russell Townships and along the west edge of the county.
A comparison of water level measurements in 1986 and 1994 indicates that water levels declined in 70 percent of the measured wells and increased in 30 percent. The change in water levels from 1986 to 1994 ranged from an increase of 13.58 feet to a decrease of 29.25 feet. Thirty percent of all water-level changes were less than 1 foot in magnitude. In nearly 80 percent of the wells, water-level changes were within the range of plus or minus 5 feet. Among the wells for which two or more historical measurements were available, the 1994 water levels in 54 percent were outside the range of water-levels observed in previous studies (only 24 percent were greater than 1 foot outside of the previously-observed range). Water-level declines of greater than 10 feet were primarily in the Cuyahoga Group and Berea Sandstone.
Some factors considered in the analysis of the differences in water levels in 1986 and 1994 were changes in water use, population, and the amount of available recharge. Water level differences could not be correlated to population changes between the 1980 and 1990 censuses. A decrease in the available recharge from 1986 to 1994 may be part of the cause for the decrease in water levels observed in two-thirds of the wells in and adjacent to Geauga County. Effects of withdrawal rates due to population increase on water levels, if present, are overshadowed by the effects of annual variations in precipitation.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954194","collaboration":"Prepared in cooperation with the Geauga County Planning Commission","usgsCitation":"Jagucki, M.L., and Lesney, L.L., 1995, Ground-water levels and directions of flow in Geauga County, Ohio, September 1994, and changes in ground-water levels, 1986-94: U.S. Geological Survey Water-Resources Investigations Report 95-4194, Report: iv, 28 p.; 5 Plates: 26.71 x 24.96 inches or smaller, https://doi.org/10.3133/wri954194.","productDescription":"Report: iv, 28 p.; 5 Plates: 26.71 x 24.96 inches or smaller","costCenters":[],"links":[{"id":358170,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1995/4194/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358171,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1995/4194/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358172,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1995/4194/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358173,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1995/4194/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358174,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1995/4194/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123678,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4194/report-thumb.jpg"},{"id":56697,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4194/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Ohio","county":"Geauga County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.5,\n 41.25\n ],\n [\n -81,\n 41.25\n ],\n [\n -81,\n 41.75\n ],\n [\n -81.5,\n 41.75\n ],\n [\n -81.5,\n 41.25\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa8e4b07f02db667485","contributors":{"authors":[{"text":"Jagucki, Martha L. 0000-0003-3798-8393 mjagucki@usgs.gov","orcid":"https://orcid.org/0000-0003-3798-8393","contributorId":1794,"corporation":false,"usgs":true,"family":"Jagucki","given":"Martha","email":"mjagucki@usgs.gov","middleInitial":"L.","affiliations":[{"id":513,"text":"Ohio Water Science Center","active":true,"usgs":true}],"preferred":true,"id":198824,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lesney, Lori L.","contributorId":208502,"corporation":false,"usgs":true,"family":"Lesney","given":"Lori","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":198823,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":25941,"text":"wri954216 - 1995 - Water-quality assessment of part of the Upper Mississippi River Basin, Minnesota and Wisconsin– Volatile organic compounds in surface and ground water, 1978-94","interactions":[],"lastModifiedDate":"2021-12-03T20:48:25.061877","indexId":"wri954216","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1995","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":"95-4216","title":"Water-quality assessment of part of the Upper Mississippi River Basin, Minnesota and Wisconsin– Volatile organic compounds in surface and ground water, 1978-94","docAbstract":"The U.S. Geological Survey compiled and summarized analyses of volatile organic compounds (VOC's) in surface and ground water from water-quality data bases maintained by-Federal, State, and local agencies as part of a retrospective analysis of water-quality data for the Upper Mississippi River Basin study unit of the National WaterQuality Assessment Program. The retrospective analysis focused on a study area that encompasses 19,500 mi2 of the eastern portion of the study unit. Major river basins in the study area include the part of the Upper Mississippi River drainage from Lake Pepin upstream to sampling stations on the Mississippi and Minnesota Rivers where long-term water-quality data are available and the entire drainage basin of the St. Croix River. The Twin Cities metropolitan area, with a population of 2.4 million people, is located in the south-central part of the study area. Water-quality data collected in the study area from 1978 through 1994 by the U.S. Geological Survey, the Minnesota Department of Health, the Minnesota Pollution Control Agency, the Wisconsin Department of Natural Resources, the Metropolitan Council Environmental Services, and the city of Minneapolis were included in the retrospective analysis.
\nIn this report, assessment of the presence and distribution of VOC's in surface and ground water in the study area is restricted to two groups of VOC's: target VOC's, and trihalomethane compounds (THM's). Target VOC's, the most commonly detected non-trihalomethane VOC's in surface and ground water in the study area, include 1,1- dichloroethane, 1,2-dichloroethane, 1,1,1-trichloroethane, trichloroethene, tetrachloroethene, benzene, ethylbenzene, toluene, meta+para-xylene, and ortho-xylene. Trihalomethane compounds described in this report include chloroform, bromodichloromethane, chlorodibromomethane, bromoform, and fluorodichloromethane.
\nExamination of water-quality data from widely distributed sampling networks of river sites and wells in the study area led to the following conclusions: 1) trace amounts of chlorinated VOC's were detected sporadically in waters of the Mississippi, Minnesota, St. Croix, and Vermillion Rivers; 2) benzene, ethylbenzene, toluene, and meta+paraxylene were detected sporadically in waters sampled from the chain of lakes used as the municipal supply for St. Paul, Minnesota; 3) the target VOC's were detected in less than five percent of ground-water samples at relatively low concentrations, generally near detection limits which ranged from 1 to 5 micrograms per liter; 4) VOC's were generally detected at similar frequencies, but at higher concentrations, in water samples from wells completed in sand and gravel aquifers than in water samples from wells completed in bedrock aquifers; 5) VOC's were most commonly detected in ground water in the vicinity of identifiable emission sites of VOC's, such as landfills, dumps, or major industries; 6) trichloroethene, a commonly used degreasing agent in dry cleaning, metal cleaning and cleaning septic lines, was the most frequently detected target VOC in ground water sampled from wells completed in both sand and gravel and bedrock aquifers; 7) wells producing water with detectable concentrations of the target VOC's tended to be shallower than wells producing water with no detectable concentrations of those compounds, but the differences in well depths were not statistically significant at a 95 percent confidence level; and 8) chlorination of water substantially increased the frequency of detection of trihalomethane compounds. The low frequencies of detection of the target VOC's and THM's in surface and ground water sampled from widely distributed sampling networks in the study area indicate that, although there are thousands of sites which can potentially emit these compounds to water, soil, and the atmosphere, these compounds have not had a widespread measurable effect on the quality of surface and ground water in the study area.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Mounds View, MN","doi":"10.3133/wri954216","usgsCitation":"Andrews, W., Fallon, J.D., and Kroening, S., 1995, Water-quality assessment of part of the Upper Mississippi River Basin, Minnesota and Wisconsin– Volatile organic compounds in surface and ground water, 1978-94: U.S. Geological Survey Water-Resources Investigations Report 95-4216, vii, 39 p., https://doi.org/10.3133/wri954216.","productDescription":"vii, 39 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":392466,"rank":2,"type":{"id":36,"text":"NGMDB Index 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J. 0000-0003-4780-8835","orcid":"https://orcid.org/0000-0003-4780-8835","contributorId":56261,"corporation":false,"usgs":true,"family":"Andrews","given":"W. J.","affiliations":[],"preferred":false,"id":195520,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fallon, J. D.","contributorId":57478,"corporation":false,"usgs":true,"family":"Fallon","given":"J.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":195521,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kroening, S. E.","contributorId":31793,"corporation":false,"usgs":true,"family":"Kroening","given":"S. E.","affiliations":[],"preferred":false,"id":195519,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":30222,"text":"wri954028 - 1995 - Hydrology and simulation of ground-water flow in the Aguadilla to Rio Camuy area, Puerto Rico","interactions":[],"lastModifiedDate":"2012-02-02T00:08:50","indexId":"wri954028","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1995","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":"95-4028","title":"Hydrology and simulation of ground-water flow in the Aguadilla to Rio Camuy area, Puerto Rico","docAbstract":"The aquifers of the Aguadilla to Rio Camuy area, in the northwestern part of Puerto Rico, are the least developed of those on the north coast, and relatively little information is available concerning the ground-water system. The present study, which was part of a comprehensive appraisal of the ground-water resources of the North Coast Province, attempts to interpret the hydrology of the area within the constraints of available data. The study area consists of an uplifted rolling plain that is 200 to 400 feet above sea level and a heavily forested, karst upland. The only major streams in the area are the Rfo Camuy and the Rio Guajataca. Most water used in the area is obtained from Lago de Guajataca, just south of the study area, and ground-water use is minimal (less than 5 million gallons per day). Sedimentary rocks of Tertiary age, mainly limestone and calcareous clays, comprise the aquifers of the Aguadilla to Rio Camuy area. The rocks generally dip from 4 to 7 degrees to the north, and the total sedimentary rock sequence may be as much as 6,000 feet thick near the Atlantic coast. Baseflows for the Rio Camuy are 58 cubic feet per second near Bayaney and 72 cubic feet per second near Hatillo. The ground-water discharge to the Rio Camuy between these stations is estimated to be 15 cubic feet per second, or 2.6 cubic feet per second per linear mile. The flow of the Rio Guajataca is regulated by the Guajataca Dam at Lago de Guajataca. Ground-water discharge to the Rio Guajataca between the dam and the coast is estimated to be about 17 cubic feet per.second, based on the average ground-water discharge per linear mile estimated for the Rio Camuy. Both water-table and artesian aquifers are present in the Aguadilla to Rio Camuy area; how-ever, most ground water occurs within the watertable aquifer, which was the primary focus of this study. The top of the confining unit, below the water-table aquifer, generally is within the unnamed upper member of the Cibao Formation; however, it is within the Los Puertos Formation in the eastern part of the study area. The water-table aquifer primarily is composed of rocks of the Aymam6n Limestone and the Los Puertos Formation. The estimated saturated thickness of the water-table aquifer ranges from zero at the southern limit of the aquifer to more than 600 feet south of Isabela. Hydraulic conductivity of the Aymam6n Limestone, based on specific-capacity test data for seven wells, ranges from about 1 to about 25 feet per day and averages 7.5 feet per day. Hydraulic conductivity of the Los Puertos Formation, based on specific-capacity test data for four wells, generally was less than 7 feet. per day. The average hydraulic-conductivity value for both the Aymam6n Limestone and the Los Puertos Formation, based on specific-capacity test data, is estimated to be about 6.0 feet per day. These hydraulic-conductivity values are much less than average values for the water-table aquifer reported for other parts of the North Coast Province. Transmissivity values, based on the average hydraulic-conductivity value for the aquifer derived from specific-capacity tests, range from zero to about 4,000 feet squared per day; however, these values were adjusted upward during model calibration. Ground water generally moves from the highlands in the south toward the sea to the north and west, and locally, to streams. A major groundwater divide extends from the southeastern corner of the study area to the northwest, and separates flow north and east into the study area from flow to the southwest toward the Rio Culebrinas. Nearly all recharge to the aquifer is from infiltration of rainfall into the karst uplands. Discharge from the aquifer primarily occurs as leakage to streams and to the sea, and to a lesser degree as flow to wells. A two-layer, three-dimensional, steady-state, numerical model was constructed to simulateground-water flow in the water-table aquifer between Aguadilla and the R/o Camuy area. A basic a","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nEarth Science Information Center, Open-File Reports Section [distributor],","doi":"10.3133/wri954028","usgsCitation":"Tucci, P., and Martinez, M., 1995, Hydrology and simulation of ground-water flow in the Aguadilla to Rio Camuy area, Puerto Rico: U.S. Geological Survey Water-Resources Investigations Report 95-4028, iv, 39 p. :ill. (1 col.), maps ;28 cm., https://doi.org/10.3133/wri954028.","productDescription":"iv, 39 p. :ill. (1 col.), maps ;28 cm.","costCenters":[],"links":[{"id":119400,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4028/report-thumb.jpg"},{"id":59005,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4028/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a18e4b07f02db605068","contributors":{"authors":[{"text":"Tucci, Patrick ptucci@usgs.gov","contributorId":926,"corporation":false,"usgs":true,"family":"Tucci","given":"Patrick","email":"ptucci@usgs.gov","affiliations":[],"preferred":true,"id":202885,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Martinez, M.I.","contributorId":12895,"corporation":false,"usgs":true,"family":"Martinez","given":"M.I.","email":"","affiliations":[],"preferred":false,"id":202886,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":30165,"text":"wri954069 - 1995 - Evaluating evapotranspiration for grasslands on the Arid Lands Ecology Reserve, Benton County, and Turnbull National Wildlife Refuge, Spokane County, Washington, May 1990 to September 1991","interactions":[],"lastModifiedDate":"2025-01-13T20:44:10.285504","indexId":"wri954069","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1995","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":"95-4069","title":"Evaluating evapotranspiration for grasslands on the Arid Lands Ecology Reserve, Benton County, and Turnbull National Wildlife Refuge, Spokane County, Washington, May 1990 to September 1991","docAbstract":"The report evaluates evapotranspiration at four grassland sites in eastern Washington: the Snively Basin and grass lysimeter sites on the Arid Lands Ecology Reserve, and the meadow and marsh sites on the Turnbull National Wildlife Refuge. A combination of the Bowen-ratio and Penman-Monteith methods were used to estimate evapotranspiration at the sites from May 30, 1990 to September 30, 1991. The Bowen-ratio method could be used to estimate latent-heat flux during only parts of the study period. Latent heat-flux values during these periods were used in the Penman-Monteith method to estimate canopy resistance. The daily average resistance values were used to recalculate latent-heat-flux with the Penman-Monteith method for all periods. Evapotranspiration estimates made with the two methods agreed within 3 percent over the period of study. However, for the grass lysimeter site, evapotranspiration estimates made with the Bowen-ratio method were only 41 percent of those made with weighing lysimeters. A water budget from August 20, 1990 to September 30, 1991 at the Snively Basin site estimated that 101 percent of the precipitation was returned to the atmosphere as evapotranspiration. Sixteen percent of the evapotranspiration occurred from October to February, while 76 percent occurred from March to July. April accounted for over 25 percent of the evapotranspiration for the water budget period.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954069","collaboration":"Prepared in cooperation with State of Washington Department of Ecology","usgsCitation":"Tomlinson, S.A., 1995, Evaluating evapotranspiration for grasslands on the Arid Lands Ecology Reserve, Benton County, and Turnbull National Wildlife Refuge, Spokane County, Washington, May 1990 to September 1991: U.S. Geological Survey Water-Resources Investigations Report 95-4069, x, 72 p., https://doi.org/10.3133/wri954069.","productDescription":"x, 72 p.","costCenters":[],"links":[{"id":123534,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4069/report-thumb.jpg"},{"id":58966,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4069/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":423590,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48179.htm","text":"Arid Lands Ecology Reserve","linkFileType":{"id":5,"text":"html"}},{"id":466156,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48180.htm","text":"Turnbull National Wildlife Refuge","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Washington","county":"Benton County, Spokane County","otherGeospatial":"Arid Lands Ecology Reserve, Turnbull National Wildlife Refuge","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -119.75,\n 46.25\n ],\n [\n -119.25,\n 46.25\n ],\n [\n -119.25,\n 46.75\n ],\n [\n -119.75,\n 46.75\n ],\n [\n -119.75,\n 46.25\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118,\n 47\n ],\n [\n -117,\n 47\n ],\n [\n -117,\n 48\n ],\n [\n -118,\n 48\n ],\n [\n -118,\n 47\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5fa14e","contributors":{"authors":[{"text":"Tomlinson, Stewart A.","contributorId":76002,"corporation":false,"usgs":true,"family":"Tomlinson","given":"Stewart","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":202796,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":25625,"text":"wri944214 - 1995 - Magnitude and frequency data for historic debris flows in Grand Canyon National Park and vicinity, Arizona","interactions":[],"lastModifiedDate":"2020-12-03T13:19:27.442537","indexId":"wri944214","displayToPublicDate":"1996-09-01T00:00:00","publicationYear":"1995","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":"94-4214","title":"Magnitude and frequency data for historic debris flows in Grand Canyon National Park and vicinity, Arizona","docAbstract":"Debris flows occur in 529 tributaries of the Colorado River in Grand Canyon between Lees Ferry and Diamond Creek, Arizona (river miles 0 to 225). An episodic type of flash flood, debris flows transport poorly-sorted sediment ranging in size from clay to boulders into the Colorado River. Debris flows create and maintain debris fans and the hundreds of associated riffles and rapids that control the geomorphic framework of the Colorado River downstream from Glen Canyon Dam. Between 1984 and 1994, debris flows created 4 new rapids and enlarged 17 existing rapids and riffles. Debris flows in Grand Canyon are initiated by slope failures that occur during intense rainfall. Three of these mechanisms of slope failure are documented. Failures in weathered bedrock, particularly in the Hermit Shale and Supai Group, have initiated many historic debris flows in Grand Canyon. A second mechanism, termed the fire-hose effect, occurs when runoff pours over cliffs onto unconsolidated colluvial wedges, triggering a failure. A third initiation mechanism occurs when intense precipitation causes failures in colluvium overlying bedrock. Multiple source areas and extreme topographic relief in Grand Canyon commonly result in combinations of these three initiation mechanisms. Interpretation of 1,107 historical photographs spanning 120 years, supplemented with aerial photography made between 1935 and 1994, yielded information on the frequency of debris flows in 168 of the 529 tributaries (32 percent) of the Colorado River in Grand Canyon. Of the 168 tributaries, 96 contain evidence of debris flows that have occurred since 1872, whereas 72 tributaries have not had a debris flow during the last century. The oldest debris flow we have documented in Grand Canyon occurred 5,400 years ago in an unnamed tributary at river mile 63.3-R. Our results indicate that the frequency of debris flows ranges from one every 10 to 15 years in certain eastern tributaries, to less than one per century in other drainage basins. On average, debris flows may recur approximately every 30 to 50 years in individual tributaries, although adjacent tributaries may have considerably different histories. Peak discharges were estimated in 18 drainages for debris flows that occurred between 1939 and 1994. Typically, discharges range from about 100 to 300 cubic meters per second (m3/s). The largest debris flow in Grand Canyon during the last century, which occurred in Prospect Canyon in 1939, had a peak discharge of about 1,000 m3/s. Debris-flow deposits generally contain 15 to 30 percent sand-and-finer sediment; however, the variability of sand-and-finer sediment contained by recent debris flows is large. Reconstitution of debris-flow samples indicates a range in water content of 10 to 25 percent by weight;. Before flow regulation of the Colorado River began, debris fans aggraded by debris flows were periodically reworked by large river floods that may have been as large as 11,000 m3/s. Impoundment of the river by Glen Canyon Dam in 1963, and subsequent operation of the reservoir have reduced the magnitude of these floods. Flow releases from the dam since 1963 have only partly reworked recently-aggraded debris fans. Significant reworking of new debris-flow deposits now occurs only during river discharges higher than typical power plant releases, which currently range between 142 and 510 m3/s.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri944214","usgsCitation":"Melis, T., Webb, R.H., Griffiths, P.G., and Wise, T., 1995, Magnitude and frequency data for historic debris flows in Grand Canyon National Park and vicinity, Arizona: U.S. Geological Survey Water-Resources Investigations Report 94-4214, x, 285 p., https://doi.org/10.3133/wri944214.","productDescription":"x, 285 p.","costCenters":[{"id":49157,"text":"Rocky Mountain Regional Office","active":true,"usgs":true}],"links":[{"id":54370,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1994/4214/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124357,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1994/4214/report-thumb.jpg"}],"country":"United States","state":"Arizona","otherGeospatial":"Grand Canyon National Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -112.76092529296875,\n 35.60371874069731\n ],\n [\n -111.45904541015625,\n 35.60371874069731\n ],\n [\n -111.45904541015625,\n 36.86643755175846\n ],\n [\n -112.76092529296875,\n 36.86643755175846\n ],\n [\n -112.76092529296875,\n 35.60371874069731\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649503","contributors":{"authors":[{"text":"Melis, T.S.","contributorId":85621,"corporation":false,"usgs":true,"family":"Melis","given":"T.S.","email":"","affiliations":[],"preferred":false,"id":194461,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Webb, R. H.","contributorId":13648,"corporation":false,"usgs":true,"family":"Webb","given":"R.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":194459,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Griffiths, Peter G. 0000-0002-8663-8907 pggriffi@usgs.gov","orcid":"https://orcid.org/0000-0002-8663-8907","contributorId":187,"corporation":false,"usgs":true,"family":"Griffiths","given":"Peter","email":"pggriffi@usgs.gov","middleInitial":"G.","affiliations":[],"preferred":true,"id":194462,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wise, T.J.","contributorId":59071,"corporation":false,"usgs":true,"family":"Wise","given":"T.J.","email":"","affiliations":[],"preferred":false,"id":194460,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":29769,"text":"wri954230 - 1995 - Application of acoustic velocity meters for gaging discharge of three low-velocity tidal streams in the St. Johns River basin, northeast Florida","interactions":[],"lastModifiedDate":"2022-05-20T19:46:13.933494","indexId":"wri954230","displayToPublicDate":"1996-08-01T00:00:00","publicationYear":"1995","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":"95-4230","title":"Application of acoustic velocity meters for gaging discharge of three low-velocity tidal streams in the St. Johns River basin, northeast Florida","docAbstract":"Index-velocity data collected with acoustic velocity meters, stage data, and cross-sectional area data were used to calculate discharge at three low-velocity, tidal streamflow stations in north-east Florida. Discharge at three streamflow stations was computed as the product of the channel cross-sectional area and the mean velocity as determined from an index velocity measured in the stream using an acoustic velocity meter. The tidal streamlflow stations used in the study were: Six Mile Creek near Picolata, Fla.; Dunns Creek near Satsuma, Fla.; and the St. Johns River at Buffalo Bluff. Cross-sectional areas at the measurement sections ranged from about 3,000 square feet at Six Mile Creek to about 18,500 square feet at St. Johns River at Buffalo Bluff. Physical characteristics for all three streams were similar except for drainage area. The topography primarily is low-relief, swampy terrain; stream velocities ranged from about -2 to 2 feet per second; and the average change in stage was about 1 foot. Instantaneous discharge was measured using a portable acoustic current meter at each of the three streams to develop a relation between the mean velocity in the stream and the index velocity measured by the acoustic velocity meter. Using least-squares linear regression, a simple linear relation between mean velocity and index velocity was determined. Index velocity was the only significant linear predictor of mean velocity for Six Mile Creek and St. Johns River at Buffalo Bluff. For Dunns Creek, both index velocity and stage were used to develop a multiple-linear predictor of mean velocity. Stage-area curves for each stream were developed from bathymetric data. Instantaneous discharge was computed by multiplying results of relations developed for cross-sectional area and mean velocity. Principal sources of error in the estimated discharge are identified as: (1) instrument errors associated with measurement of stage and index velocity, (2) errors in the representation of mean daily stage and index velocity due to natural variability over time and space, and (3) errors in cross-sectional area and mean-velocity ratings based on stage and index velocity. Standard errors for instantaneous discharge for the median cross-sectional area for Six Mile Creek, Dunns Creek, and St. Johns River at Buffalo Bluff were 94,360, and 1,980 cubic feet per second, respectively. Standard errors for mean daily discharge for the median cross-sectional area for Six Mile Creek, Dunns Creek, and St. Johns River at Buffalo Bluff were 25, 65, and 455 cubic feet per second, respectively. Mean daily discharge at the three sites ranged from about -500 to 1,500 cubic feet per second at Six Mile Creek and Dunns Creek and from about -500 to 15,000 cubic feet per second on the St. Johns River at Buffalo Bluff. For periods of high discharge, the AVM index-velocity method tended to produce estimates accurate with 2 to 6 percent. For periods of moderate discharge, errors in discharge may increase to more than 50 percent. At low flows, errors as a percentage of discharge increase toward infinity.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954230","usgsCitation":"Sloat, J.V., and Gain, W., 1995, Application of acoustic velocity meters for gaging discharge of three low-velocity tidal streams in the St. Johns River basin, northeast Florida: U.S. Geological Survey Water-Resources Investigations Report 95-4230, iv, 26 p., https://doi.org/10.3133/wri954230.","productDescription":"iv, 26 p.","costCenters":[],"links":[{"id":123929,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_95_4230.jpg"},{"id":2485,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri954230","linkFileType":{"id":5,"text":"html"}},{"id":400876,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48314.htm"}],"country":"United States","state":"Florida","otherGeospatial":"St. Johns River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.75,\n 29.5\n ],\n [\n -81.4167,\n 29.5\n ],\n [\n -81.4167,\n 30.25\n ],\n [\n -81.75,\n 30.25\n ],\n [\n -81.75,\n 29.5\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac6e4b07f02db67aa7c","contributors":{"authors":[{"text":"Sloat, J. V.","contributorId":85997,"corporation":false,"usgs":true,"family":"Sloat","given":"J.","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":202092,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gain, W. S.","contributorId":29024,"corporation":false,"usgs":true,"family":"Gain","given":"W. S.","affiliations":[],"preferred":false,"id":202091,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":25385,"text":"wri954285 - 1995 - Agricultural pesticide applications and observed concentrations in surface waters from four drainage basins in the Central Columbia Plateau, Washington and Idaho, 1993-94","interactions":[],"lastModifiedDate":"2012-02-02T00:08:29","indexId":"wri954285","displayToPublicDate":"1996-08-01T00:00:00","publicationYear":"1995","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":"95-4285","title":"Agricultural pesticide applications and observed concentrations in surface waters from four drainage basins in the Central Columbia Plateau, Washington and Idaho, 1993-94","docAbstract":"As part of the U.S. Geological Survey's National Water-Quality Assessment Program, the use and occurrence of agricultural pesticides were investigated in four drainage basins--two dominated by irrigated agriculture and two by dryland agriculture--in the Central Columbia Plateau of eastern Washington. For this study, 85 pesticides or pesticide metabolites were selected for analysis from a list of nearly 400 compounds commonly used in the United States. Pesticide-use data included estimates of the total quantity of herbicides, insecticides, and fungicides applied to croplands in each of the four drainage basins and reported times of application for selected pesticides. Pesticide-occurrence data included concentrations of pesticides in samples collected at one surface-water site at or near the outflow of each of the four drainage basins, where surface waters were sampled one to five times a month from March 1993 through May 1994. Of the 85 pesticides or pesticide metabolites targeted for analysis, a total of 45 different compounds were detected in samples from the four sites, ranging in concentration from at or near the limit of detection (as low as 0.001 microgram per liter) to a maximum of 8.1 micrograms per liter. None of the concentrations of pesticides exceeded the U.S. Environmental Protection Agency (USEPA) drinking water standards, but concentrations of five pesticides exceeded the USEPA freshwater-chronic criteria for the protection of aquatic life. Forty-one different pesticides or pesticide metabolites were detected in surface waters sampled at the two sites representing irrigated agriculture drainage basins. The herbicides atrazine, DCPA, and EPTC were detected most frequently at the two sampling sites. Not all pesticides that were applied were detected, however. For example, disulfoton, phorate, and methyl parathion accounted for 15 percent of the insecticides applied in the two irrigated drainage basins, yet none of these pesticides were detected in samples from the two irrigated-agricultural sites. Concentrations of pesticides found in surface waters at the two sites representing irrigated agriculture did not exceed drinking water standards, but some concentrations of the insecticides carbaryl, chlorpyrifos, diazinon, and azinphos-methyl exceeded the freshwater-chronic criteria for the protection of aquatic life. Twenty-three different pesticides or pesticide metabolites were detected in samples from the two sites representing dryland agricultural drainage basins. Herbicides were the type of pesticides most heavily applied in these drainage basins, and the herbicides atrazine, triallate, and simazine were detected most frequently in samples. Some herbicides, for example triallate in the Palouse River drainage basin, were both heavily applied and frequently detected. Others, like atrazine and simazine, were not typically applied to cropland, but were frequently detected in surface-water samples. Several insecticides (Lindane, ethoprop, carbaryl, and azinphos-methyl) were detected in samples from the two sites, although they were not reported as commonly applied to croplands in the dryland agricultural drainage basins. Concentrations of pesticides found in surface waters at the two sites did not exceed drinking water guidelines, but concentrations of the insecticides diazinon and azinphos-methyl and the herbicide triallate exceeded freshwater-chronic criteria for the protection of aquatic life.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nEarth Science Information Center, Open-File Reports Section [distributor],","doi":"10.3133/wri954285","usgsCitation":"Wagner, R.J., Ebbert, J., Roberts, L., and Ryker, S., 1995, Agricultural pesticide applications and observed concentrations in surface waters from four drainage basins in the Central Columbia Plateau, Washington and Idaho, 1993-94: U.S. Geological Survey Water-Resources Investigations Report 95-4285, v, 50 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri954285.","productDescription":"v, 50 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":124013,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4285/report-thumb.jpg"},{"id":54119,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4285/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae3e4b07f02db688eea","contributors":{"authors":[{"text":"Wagner, R. J.","contributorId":37318,"corporation":false,"usgs":true,"family":"Wagner","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":193474,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ebbert, J.C.","contributorId":57451,"corporation":false,"usgs":true,"family":"Ebbert","given":"J.C.","affiliations":[],"preferred":false,"id":193475,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Roberts, L.M.","contributorId":84355,"corporation":false,"usgs":true,"family":"Roberts","given":"L.M.","email":"","affiliations":[],"preferred":false,"id":193476,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Ryker, S.J.","contributorId":16047,"corporation":false,"usgs":true,"family":"Ryker","given":"S.J.","affiliations":[],"preferred":false,"id":193473,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":28247,"text":"wri954233 - 1995 - Synthesis of nutrient and sediment data for watersheds within the Chesapeake Bay drainage basin","interactions":[],"lastModifiedDate":"2021-10-29T19:16:52.99799","indexId":"wri954233","displayToPublicDate":"1996-08-01T00:00:00","publicationYear":"1995","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":"95-4233","title":"Synthesis of nutrient and sediment data for watersheds within the Chesapeake Bay drainage basin","docAbstract":"Nutrient and sediment data collected by Federal and state agencies from 1972 through 1992 at 1,058 surface-water sites in nontidal parts of the Chesapeake Bay Basin were compiled into a large database. Adequate nutrient, sediment, and streamflow data were not available to compute annual loads for all sites because water-quality monitoring at many of the sites was either short term or noncontinuous or because stream-flow was not measured. Annual nutrient and sediment loads were calculated at a total of 127 sites. Annual loads of dissolved nitrate were calculated for 108 sites, but total nitrogen loads could be calculated for only 48 of these sites because ammonia plus organic nitrogen data were not available for many of these 108 sites. Annual loads of total phosphorus were calculated for 99 sites, and annual loads of suspended sediment were calculated for 33 sites. Loads could be calculated for only a very few sites in the Juniata River Basin (a tributary to the Susquehanna River), the York River Basin, the middle and lower reaches of the James River, and the nontidal parts of the eastern shore of the Bay.\r\n\r\n Geographic Information System (GIS) spatial data sets of land use, physiographic province, rock type, and watershed delineation were compiled for the entire Chesapeake Bay Basin (approximately 64,000 square miles). The nutrient- and sediment-yield were evaluated with respect to land use, physiographic province, rock type, and hydrologic characteristics. During years that the mean streamflow was about equal to the long-term mean streamflow, the Susquehanna River contributed about 50 percent of the freshwater, 66 percent of the total nitrogen, and 40 percent of the total phosphorus transported by tributaries to the Bay. Nutrient and sediment data were available for less than 18 percent of the predominantly agricultural areas underlain by siliciclastic rock and for less than 35 percent of the predominantly agricultural areas underlain by either carbonate rock or unconsolidated rock. Nutrient and sediment data were available for about 91 percent of the predominantly forested areas underlain by siliciclastic rock. Spatial and temporal gaps in the water-quality data and GIs data sets limited some data analysis. Correlations of annual yields or nutrients and sediment with respect to land use, physiographic province, and rock type indicated (1) basins with larger percentages of agricultural land had larger nutrient and sediment yields, (2) basins with larger percentages of forest land had smaller nutrient and sediment loads, (3) the largest total nitrogen yields were from agricultural basins underlain by carbonate rock, (4) yields or nutrients from urban basins were substantially less than yields from agricultural basins, and (5) basins with small amounts of agricultural and urban land had relatively small nutrient and sediment yields.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954233","usgsCitation":"Langland, M., Lietman, P., and Hoffman, S.A., 1995, Synthesis of nutrient and sediment data for watersheds within the Chesapeake Bay drainage basin: U.S. Geological Survey Water-Resources Investigations Report 95-4233, vi, 121 p., 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L.","affiliations":[],"preferred":false,"id":186757,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Libarkin, J.C.","contributorId":87973,"corporation":false,"usgs":true,"family":"Libarkin","given":"J.C.","email":"","affiliations":[],"preferred":false,"id":186756,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":28229,"text":"wri954024 - 1995 - Ground-water quality in agricultural areas, Anoka Sand Plain Aquifer, east-central Minnesota, 1984-90","interactions":[],"lastModifiedDate":"2019-12-08T13:07:04","indexId":"wri954024","displayToPublicDate":"1996-07-01T00:00:00","publicationYear":"1995","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":"95-4024","title":"Ground-water quality in agricultural areas, Anoka Sand Plain Aquifer, east-central Minnesota, 1984-90","docAbstract":"Ground-water quality in the Anoka Sand Plain aquifer was studied as part of the multiscale Management Systems Evaluation Area (MSEA) study by collecting water samples from shallow wells during August through November 1990. The sampling was conducted to: (1) aid in selection of the MSEA research area; (2) facilitate comparison of results at the MSEA research area to the regional scale; and (3) evaluate changes in ground-water quality in the Anoka Sand Plain aquifer since a previous study during 1984 through 1987. Samples were collected from 34 wells screened in the upper 6 meters of the surficial aquifer and located in cultivated agricultural areas. Water temperature, pH, specific conductance, and presence or absence of triazine herbicides were determined at all sites and samples from selected wells were analyzed for concentrations of dissolved oxygen, alkalinity, major cations and anions, nutrients, and selected herbicides and herbicide metabolites. The results of the study indicate that the water-quality of some shallow ground water in areas of predominantly agricultural land use has been affected by applications of nitrogen fertilizers and the herbicide atrazine.
\nConcentrations of nitrite plus nitrate nitrogen (nitrate-N) in 19 samples ranged from less than the detection limit of 0.1 to 21 milligrams per liter (mg/L) with a median of 10 mg/L. Concentrations of nitrate-N were not significantly correlated with depth below the water table or dissolved oxygen but were significantly correlated with concentrations of chloride. Concentrations of nitrate-N during 1990 were generally similar to concentrations measured during 1984 through 1987. Changes in concentrations of nitrate-N during 1984 through 1990 were likely related to variations in recharge or other site-specific factors.
\nImmunoassay analyses were used as screening tools to detect the presence of triazine herbicides. All samples in which triazine herbicides were detected by immunoassay, and selected samples in which triazine herbicides were not detected by immunoassay, were analyzed for selected herbicides and herbicide metabolites by gas chromatography/mass spectroscopy (GC/MS). There was an excellent correspondence between concentrations of triazine herbicides indicated by immunoassay and concentrations of atrazine measured by GC/MS, indicating that the immunoassay method was a valuable qualitative to semi-quantitative tool for evaluating the presence and approximate concentration of atrazine.
\nThe combined results of immunoassay and GC/MS analyses indicate that atrazine was detected in 11 of the 34 wells with a median concentration less than the immunoassay detection limit of 0.1 micrograms per liter (μg/L). Atrazine was detected in 11 of the 17 samples analyzed by GC/MS at concentrations ranging from the detection limit of 0.05 to 0.81 μg/L with a median of 0.09 μg/L. Atrazine metabolite de-ethylatrazine (DEA) was the most frequently detected herbicide or herbicide metabolite and generally was present at the greatest concentrations. There were detections of DEA in 13 of the 17 samples analyzed at concentrations ranging from the detection limit of 0.05 to 1.12 μg/L with a median of 0.15 μg/L. Concentrations of DEA were significantly correlated with concentrations of calcium, magnesium, and specific conductance. The atrazine metabolite de-isopropylatrazine and the herbicide metolachlor both were detected in 1 of the 17 wells. The frequency of detection and the concentrations of atrazine in shallow ground water during 1990 were very similar to results of sampling conducted in 1984.
\nConcentrations of atrazine and DEA generally were greater near the water table and decreased or were not detected in deeper wells. All of the samples in which atrazine and DEA were detected also had increased (greater than 3 mg/L) nitrate-N concentrations. However, not all samples with increased concentrations of nitrate-N had detections of atrazine or DEA. This likely indicates either that there were sources of nitrate-N other than cultivated fields on which both atrazine and nitrogen were applied or that nitrate-N reached ground water more readily than atrazine or DEA.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Mounds View, MN","doi":"10.3133/wri954024","collaboration":"Prepared in cooperation with the University of Minnesota Department of Soil Science and the U.S. Department of Agriculture, Agricultural Research Service","usgsCitation":"Landon, M., and Delin, G., 1995, Ground-water quality in agricultural areas, Anoka Sand Plain Aquifer, east-central Minnesota, 1984-90: U.S. Geological Survey Water-Resources Investigations Report 95-4024, iv, 25 p., https://doi.org/10.3133/wri954024.","productDescription":"iv, 25 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true},{"id":589,"text":"Toxic Substances Hydrology 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N.","contributorId":12834,"corporation":false,"usgs":true,"family":"Delin","given":"G. N.","affiliations":[],"preferred":false,"id":199429,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":25575,"text":"wri954139 - 1995 - Hydrogeology and water quality at the management systems evaluation area near Piketon, Ohio","interactions":[],"lastModifiedDate":"2023-01-09T22:03:28.347265","indexId":"wri954139","displayToPublicDate":"1996-07-01T00:00:00","publicationYear":"1995","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":"95-4139","title":"Hydrogeology and water quality at the management systems evaluation area near Piketon, Ohio","docAbstract":"This report presents the results of a study by the U.S. Geological Survey, The Ohio State University, and the U.S. Department of Agriculture to describe the hydrology, water quality, and geochemical factors controlling water quality at the Ohio Management Systems Evaluation Area (MSEA). The Ohio MSEA is located on a 650-acre farm in the Scioto River Valley in Pike County, south-central Ohio. The farm is underlain by an incised bedrock valley filled with about 70 feet of sand and gravel outwash deposits that are covered by a veneer of silty clay alluvium and silty loam and sandy loam soils. Outwash sediment are composed predominantly of dolomite, quartz, and calcite, and have a median organic carbon concentration of 0.39 weight percent. Horizontal hydraulic conductivity of the sediment based on results of multiple-well aquifer tests ranges from 400 to 560 feet per day. Ground-water flow is from east to west-southwest at an average velocity of 1.5 to 2.5 feet per day. Ground water and surface water at the site are highly interconnected. Big Beaver Creek recharges the outwash aquifer along the eastern edge of the study area, and ground water discharges to the Scioto River at the western edge of the study area. High-stage events on the Scioto River cause frequent flow reversals in the aquifer that allow streamwater to travel a maximum observed distance of 190 feet inland. A zone of oxidizing waters (characterized by high dissolved oxygen concentration and Eh) is found in shallow ground water for several hundred feet adjacent to Big Beaver Creek and the Scioto River. This zone of oxidizing ground water is caused by the periodic inflow of surface waters to the aquifer. A ground-water budget for the study area indicates that the aquifer received 17.7 inches of recharge during water year 1992; of this amount, 72 percent originated as infiltrating precipitation, 28 percent as infiltration of surface water from Big Beaver Creek, and 0.2 percent as leakage from bedrock. Areal variation in water quality is caused by areal differences in the relative importance of these three recharge sources. The effects of bedrock leakage are evident only in the northeast corner of the study area. Here, deep outwash waters are transitional in composition between the calcium magnesium bicarbonate waters found elsewhere in the outwash aquifer and the calcium sodium chloride waters of the bedrock aquifer. Mixing calculations indicate that these deep outwash waters are composed of as much as 26 percent bedrock water. In the southern part of the MSEA, ground water is diluted by surface water from Big Beaver Creek as it recharges the aquifer through a sand and gravel streambed. At the northeast corner of the MSEA, however, Big Beaver Creek flows across a shale streambed through which no infiltration occurs. Redox reactions in the outwash aquifer control variations in aquifer chemistry with depth. From the water table to about 40 feet below land surface, oxidizing conditions are characterized by the presence of dissolved oxygen and nitrates in ground water, Eh greater than 200 millivolts, ferrihydrite coatings on sediment grains, and the absence of dissolved iron and manganese. From about 40 feet below land surface to the base of the aquifer, reducing conditions are characterized by dissolved oxygen concentrations less than 2 mg/L, Eh less than 200 millivolts, and the presence of dissolved iron and manganese. Denitrification in the reducing zone naturally remediates anthropogenic nitrate contamination of the aquifer while oxidizing pyrite in the aquifer sediment.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri954139","usgsCitation":"Jagucki, M.L., Finton, C.D., Springer, A.E., and Bair, E., 1995, Hydrogeology and water quality at the management systems evaluation area near Piketon, Ohio: U.S. Geological Survey Water-Resources Investigations Report 95-4139, vii, 117 p., https://doi.org/10.3133/wri954139.","productDescription":"vii, 117 p.","costCenters":[{"id":513,"text":"Ohio Water Science Center","active":true,"usgs":true},{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":411594,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48239.htm","linkFileType":{"id":5,"text":"html"}},{"id":124878,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4139/report-thumb.jpg"},{"id":54294,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4139/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Ohio","city":"Piketon","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -83.02476524225692,\n 39.05708700203755\n ],\n [\n -83.06035253063361,\n 39.05708700203755\n ],\n [\n -83.06035253063361,\n 39.01848388151214\n ],\n [\n -83.02476524225692,\n 39.01848388151214\n ],\n [\n -83.02476524225692,\n 39.05708700203755\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ae4b07f02db6251e5","contributors":{"authors":[{"text":"Jagucki, Martha L. 0000-0003-3798-8393 mjagucki@usgs.gov","orcid":"https://orcid.org/0000-0003-3798-8393","contributorId":1794,"corporation":false,"usgs":true,"family":"Jagucki","given":"Martha","email":"mjagucki@usgs.gov","middleInitial":"L.","affiliations":[{"id":513,"text":"Ohio Water Science Center","active":true,"usgs":true}],"preferred":true,"id":777020,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Finton, Christopher D.","contributorId":97145,"corporation":false,"usgs":true,"family":"Finton","given":"Christopher","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":194257,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Springer, Abraham E.","contributorId":76278,"corporation":false,"usgs":true,"family":"Springer","given":"Abraham","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":194256,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bair, E. Scott","contributorId":73231,"corporation":false,"usgs":true,"family":"Bair","given":"E. Scott","affiliations":[],"preferred":false,"id":194255,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":25832,"text":"wri954163 - 1995 - Water-quality assessment of the Kentucky River Basin, Kentucky: Results of investigations of surface-water quality, 1987-90","interactions":[],"lastModifiedDate":"2021-12-27T21:37:05.905512","indexId":"wri954163","displayToPublicDate":"1996-06-01T00:00:00","publicationYear":"1995","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":"95-4163","title":"Water-quality assessment of the Kentucky River Basin, Kentucky: Results of investigations of surface-water quality, 1987-90","docAbstract":"The U.S. Geological Survey investigated the water quality of the Kentucky River Basin in Kentucky as part of the National Water-Quality Assessment program. Data collected during 1987-90 were used to describe the spatial and temporal variability of water-quality constituents including metals and trace elements, nutrients, sediments, pesticides, dissolved oxygen, and fecal-coliform bacteria. Oil-production activities were the source of barium, bromide, chloride, magnesium, and sodium in several watersheds. High concentrations of aluminum, iron, and zinc were related to surface mining in the Eastern Coal Field Region. High concentrations of lead and zinc occurred in streambed sediments in urban areas, whereas concentrations of arsenic, strontium, and uranium were associated with natural geologic sources. Concentrations of phosphorus were significantly correlated with urban and agricultural land use. The high phosphorus content of Bluegrass Region soils was an important source of phosphorus in streams. At many sites in urban areas, most of the stream nitrogen load was attributable to wastewater-treatment-plant effluent. Average suspended-sediment concentrations were positively correlated with discharge. There was a downward trend in suspended-sediment concentrations downstream in the Kentucky River main stem during the study. The most frequently detected herbicides in water samples were atrazine, 2,4-D, alachlor, metolachlor, and dicamba. Diazinon, malathion, and parathion were the most frequently detected organophosphate insecticides in water samples. Detectable concentrations of aldrin, chlordane, DDT, DDE, dieldrin, endrin, endosulfan, heptachlor, and lindane were found in streambed-sediment samples. Dissolved-oxygen concentrations were sometimes below the minimum concentration needed to sustain aquatic life. At some sites, high concentrations of fecal-indicator bacteria were found and water samples did not meet sanitary water-quality criteria.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954163","usgsCitation":"Haag, K.H., Garcia, R., Jarrett, G., and Porter, S.D., 1995, Water-quality assessment of the Kentucky River Basin, Kentucky: Results of investigations of surface-water quality, 1987-90: U.S. Geological Survey Water-Resources Investigations Report 95-4163, viii, 70 p., https://doi.org/10.3133/wri954163.","productDescription":"viii, 70 p.","costCenters":[],"links":[{"id":393476,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48258.htm"},{"id":54580,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4163/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123681,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4163/report-thumb.jpg"}],"country":"United States","state":"Kentucky","otherGeospatial":"Kentucky River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -85.1667,\n 36.9\n ],\n [\n -82.6667,\n 36.9\n ],\n [\n -82.6667,\n 38.733\n ],\n [\n -85.1667,\n 38.733\n ],\n [\n -85.1667,\n 36.9\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac7e4b07f02db67adf2","contributors":{"authors":[{"text":"Haag, K. H.","contributorId":67925,"corporation":false,"usgs":true,"family":"Haag","given":"K.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":195260,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Garcia, Rene","contributorId":106089,"corporation":false,"usgs":true,"family":"Garcia","given":"Rene","email":"","affiliations":[],"preferred":false,"id":195262,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Jarrett, G. L.","contributorId":83963,"corporation":false,"usgs":true,"family":"Jarrett","given":"G. L.","affiliations":[],"preferred":false,"id":195261,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Porter, S. D.","contributorId":8882,"corporation":false,"usgs":true,"family":"Porter","given":"S.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":195259,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":27608,"text":"wri954098 - 1995 - Water-quality characteristics of selected public recreational lakes and ponds in Connecticut","interactions":[],"lastModifiedDate":"2012-02-02T00:08:42","indexId":"wri954098","displayToPublicDate":"1996-06-01T00:00:00","publicationYear":"1995","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":"95-4098","title":"Water-quality characteristics of selected public recreational lakes and ponds in Connecticut","docAbstract":"Reconnaissance limnological and lakebed-sediment surveys were conducted in Connecticut during 1989-91 by the U.S. Geological Survey, in cooperation with the Connecticut Department of Environmental Protec- tion, to evaluate water-quality characteristics of selected public recreational lakes and ponds in the State. Limnological surveys were conducted on 49 lakes and ponds selected from a list of 105 publicly owned waterbodies that qualified for water- quality assessments under Section 314 of the Federal Clean Water Act. Lakebed-sediment surveys were conducted in 9 river impoundments and 1 riverine lake below industrial areas and 2 headwater lakes in relatively pristine areas. The limnological surveys consisted of two sampling events--during spring turnover and during the summer stratifi- cation. Each sampling event included depth profiles of water temperature, specific conductance, hydrogen-ion activity, and dissolved oxygen concen- trations; measurements of Secchi disc transparency; and the collection of samples for the analyses of alkalinity, chlorophyll, phosphorus, and nitrogen concentrations. Areal extent and population density of the dominant aquatic macrophytes were qualita- tively noted during the summer sampling event. These water-quality data were used to determine the trophic classification and acidification status of the 49 lakes. The trophic classification yielded the following results: 2 oligotrophic, 8 early mesotrophic, 13 mesotrophic, 5 late mesotrophic, 10 eutrophic, and 11 highly eutrophic lakes. In terms of acidification status, 7 lakes were classified as acid threatened and 42 as not threatened. A Wilcoxon two-tailed signed rank test was used to compare data for 13 lakes and ponds from the present survey with data from the 1973-75 or 1978-79 surveys conducted by the Connecticut Agricultural Experiment Station and Connecticut Department of Environmental Protection. The test showed no significant difference at the 90 percent confidence level for spring nitrogen and summer chlorophyll-a concen- trations, a significant increase at the 90 percent confidence level in summer phosphorus concentra- tions, and a significant decrease at the 95 percent confidence level in summer transparency. For the lakebed-sediment surveys, composite-grab samples were collected from the deepest part of each lake. Samples were analyzed for arsenic, cyanide, organic and inorganic carbon, selected metals, and methylene-extractable, synthetic organic compounds classified by the U.S. Environmental Protection Agency as semi-volatile priority pollutants. Hanover Pond, Eagleville Lake, and West Thompson Lake had three of the four highest concentrations of cadmium, chromium, copper, lead, nickel, zinc, and cyanide. The four lakes with the highest concentrations of arsenic (Aspinook Pond, Fitchville Pond, Mashapaug Pond, and West Thompson Lake) are located in the eastern part of Connecticut. The three samples with the highest mercury concentrations were from Lake Lillinonah and Lake Zoar. There appears to be a positive correlation between the concentrations of cadmium, chromium, copper, lead, nickel, zinc, and cyanide. Only 15 of the 54 synthetic organic compounds analyzed for were detected in 9 of the 12 lakes sampled. Of these 15 compounds, 14 are polycyclic aromatic hydrocarbons and the 15th is a phthalate ester. Hanover Pond had the most compounds detected (9), and phenanthrene was the compound detected in the most lakes (8).","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nEarth Science Information Center, Open-File Reports Section [distributor],","doi":"10.3133/wri954098","usgsCitation":"Healy, D.F., and Kulp, K., 1995, Water-quality characteristics of selected public recreational lakes and ponds in Connecticut: U.S. Geological Survey Water-Resources Investigations Report 95-4098, ix, 277 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri954098.","productDescription":"ix, 277 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":159026,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4098/report-thumb.jpg"},{"id":56474,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4098/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a09e4b07f02db5fafec","contributors":{"authors":[{"text":"Healy, D. F.","contributorId":97120,"corporation":false,"usgs":true,"family":"Healy","given":"D.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":198405,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kulp, K.P.","contributorId":49791,"corporation":false,"usgs":true,"family":"Kulp","given":"K.P.","email":"","affiliations":[],"preferred":false,"id":198404,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":25523,"text":"wri944237 - 1995 - Geohydrology and water quality of the Durham Center Area, Durham, Connecticut","interactions":[],"lastModifiedDate":"2019-10-15T06:53:59","indexId":"wri944237","displayToPublicDate":"1996-06-01T00:00:00","publicationYear":"1995","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":"94-4237","title":"Geohydrology and water quality of the Durham Center Area, Durham, Connecticut","docAbstract":"Contaminated ground water is widespread and persistent beneath the Durham Center area in the town of Durham, Conn. Most of the contaminants are organic halides, usually trichloroethene, 1,1,1-trichloroethane, and tetrachloroethene. Less extensive chemical contamination of surface water, soil, and glacial sediments also has been detected. Two manufacturing companies, located at the northern and southern ends of this largely residential area, are believed to be the principal sources of the organic compounds detected in ground water. The contamination of water in the bedrock, the primary source of drinking water throughout the area, is the major environmental concern. Maximum concentrations of trichloroethene in three bed- rock wells range from 4,500 to about 5,500 mg/L (micrograms per liter). Concentrations of trichloroethene greater than 5 mg/L, the maximum contaminant level established for drinking water by the U.S Environmental Protection Agency, have regularly been detected in water samples from many other bedrock wells for at least 9 years. The geohydrology of the area is highly complex. Compact lodgment till that is up to 30 feet thick and probably fractured, overlies the bedrock. The bedrock is lithologically heterogeneous, and con- sists mostly of red fluvial sandstone, siltstone, and conglomerate; it is locally interbedded with black lacustrine shales and gray sandstones. Lithology and stratigraphy interpreted from borehole-geophysical logs at Durham Center are consistent with the Portland Formation subfacies described in earlier geologic studies. Beds strike nearly north-south and dip gently eastward. At least one high-angle normal fault transects the bedrock; it strikes northeast and dips northwest. Acoustic televiewer logs, measurements at out-crops, and azimuthal, square-array, resistivity data indicate a dominance of northeast-striking fractures that dip steeply northwest and southeast. Less prevalent strike directions are north to east-north-east. The till and sedimentary bedrock are dual-porosity, dual-permeability media. The hydraulic conductivity of the bulk mass of till is believed to be on the order of tenths of a foot per day to about 2.5 feet per day, with a total porosity of about 25 percent and an estimated average fracture porosity of less than 1 percent. The reported transmissivities of the bedrock range from less than 1 to about 17,000 feet squared per day and storativity is generally about 10-4, but the accuracy of these values is uncertain. The intergranular porosity of the sandstone units is estimated to average 5 percent, and estimates of fracture porosity from square-array, resistivity soundings at two sites were 1.1 and 2.7 percent. The bedrock has characteristics of both a single aquifer and a multi-unit, artesian or leaky aquifer system. A local ground-water-flow system that includes the upper part of the bedrock is unconfined. A large- scale flow system in deeper parts of the bedrock has transported organic compounds across topographic drainage divides. Borehole-geophysical logs and head measurements indicate that the natural ground- water-flow system in the bedrock has been altered by drilled wells that connect fractures and by with- drawals from wells. A conceptual model of the movement and fate of organic contaminants suggests that (1) nonaqueous phase organic halides are retained near their source; (2) flow is primarily through fractures in the till and through fractures and bedding-plane openings in the sedimentary rocks; (3) retardation of contaminants occurs primarily by diffusion from fractures into the aquifer matrix; and (4) transport directions of dissolved organic halides are controlled by a combination of natural hydraulic gradients, hydraulic gradients produced by the cyclical pumping of wells, and by the strike directions of bedrock faults, fractures, and bedding planes.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri944237","usgsCitation":"Melvin, R., Stone, J.R., Craft, P.A., Lane, J., and Davies, B., 1995, Geohydrology and water quality of the Durham Center Area, Durham, Connecticut: U.S. Geological Survey Water-Resources Investigations Report 94-4237, v, 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III","contributorId":72413,"corporation":false,"usgs":true,"family":"Davies","given":"B.S.","suffix":"III","email":"","affiliations":[],"preferred":false,"id":194036,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":27410,"text":"wri944110 - 1995 - Water levels in the Calumet aquifer and their relation to surface-water levels in northern Lake County, Indiana, 1985-92","interactions":[],"lastModifiedDate":"2016-05-24T10:55:16","indexId":"wri944110","displayToPublicDate":"1996-06-01T00:00:00","publicationYear":"1995","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":"94-4110","title":"Water levels in the Calumet aquifer and their relation to surface-water levels in northern Lake County, Indiana, 1985-92","docAbstract":"The U.S. Geological Survey made 2,328 water-level measurements at a total of 96 ground-water and surface-water sites in northern Lake County, Indiana, from August 1985 through September 1992. This report lists and summarizes the significance of the measurements. Northern Lake County is on the southern shore of Lake Michigan and includes the cities of East Chicago, Gary, Hammond, and Whiting. The study area is underlain by the unconfined Calumet aquifer and receives about 36 inches of precipitation per year.
\nThe U.S. Geological Survey investigated ground-water levels and flow in the Calumet aquifer and the effect of Lake Michigan levels on ground-water and surface-water levels throughout the study area. Summary statistics of the water-level data were computed for each site.
\nGround-water levels annually reach a maximum in June or July and a minimum in September or October. Measured groundwater fluctuations in the Calumet aquifer during the study period ranged from 0.40 to 5.01 feet, and the mean ground-water fluctuation was about 2.3 feet The largest surface-water fluctuations were affected by record setting Lake Michigan levels. Midmonth daily averages for the data-collection period show that Lake Michigan fluctuated 4.14 feet Water-level fluctuations on the Grand Calumet River were from 1.06 to 2.45 feet.
\nAnalysis of water-level data indicates that the 1988 drought did not substantially affect water levels in the Calumet aquifer, but the deficit in precipitation reversed vertical flow gradients in ground water at three paired deep and shallow wells. High water levels in Lake Michigan during 1985-87 created long-term backwater effects on the Grand Calumet River as far as 11.0 miles upstream from Lake Michigan.
\nAnalysis of water-level data from the data-collection network indicates that the water table normally slopes toward streams, ditches, sewers, the Indiana Harbor Canal, and Lake Michigan. The slope of the water table toward the Grand Calumet River is greatest in the winter and can decrease to being almost horizontal in the summer. Wells near streams respond quickly to nearby surface-water-level changes. Water-table maps indicate that sewers and dewatering systems are lowering ground-water levels in large areas. Ditches, the Grand Calumet River, and the Indiana Harbor Canal connect the Lake Michigan water level to large parts of the study area. The surface-water stage in the Indiana Harbor Canal, which functions as a ditch, can equal Lake Michigan's stage up to 3.75 miles inland from the lakeshore. Human activity, the stage of Lake Michigan, and the storage capacity of the Calumet aquifer combine to reduce vertical changes in the water table in the study area.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Indianapolis, IN","doi":"10.3133/wri944110","collaboration":"Indiana Department of Environmental Management","usgsCitation":"Greeman, T.K., 1995, Water levels in the Calumet aquifer and their relation to surface-water levels in northern Lake County, Indiana, 1985-92: U.S. Geological Survey Water-Resources Investigations Report 94-4110, v, 61 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri944110.","productDescription":"v, 61 p. :ill., maps ;28 cm.","startPage":"1","endPage":"61","numberOfPages":"67","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":158683,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1994/4110/report-thumb.jpg"},{"id":56269,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1994/4110/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Indiana","county":"Lake","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-87.2223,41.6248],[-87.2222,41.6152],[-87.2221,41.6039],[-87.2218,41.5698],[-87.22,41.4632],[-87.2198,41.3747],[-87.2196,41.3601],[-87.22,41.3388],[-87.2198,41.3188],[-87.2197,41.3043],[-87.2189,41.2893],[-87.2187,41.2744],[-87.2193,41.2671],[-87.219,41.2426],[-87.2184,41.2417],[-87.2263,41.2353],[-87.2762,41.2187],[-87.2859,41.2154],[-87.3241,41.1862],[-87.3313,41.1829],[-87.3405,41.1824],[-87.3448,41.1824],[-87.38,41.1726],[-87.394,41.1625],[-87.4,41.1625],[-87.4055,41.1625],[-87.4147,41.1619],[-87.4411,41.1731],[-87.4466,41.174],[-87.4484,41.1744],[-87.4587,41.1702],[-87.4801,41.1701],[-87.5263,41.1661],[-87.5261,41.267],[-87.5265,41.2983],[-87.527,41.4086],[-87.5265,41.4712],[-87.5255,41.5516],[-87.5239,41.6941],[-87.524,41.7135],[-87.5234,41.7131],[-87.5134,41.7054],[-87.5158,41.7027],[-87.5133,41.7004],[-87.4997,41.6914],[-87.4922,41.6865],[-87.4848,41.6843],[-87.4829,41.6811],[-87.4768,41.6789],[-87.4712,41.6753],[-87.4613,41.6718],[-87.4503,41.6741],[-87.4397,41.6647],[-87.436,41.6656],[-87.4355,41.6729],[-87.4245,41.6802],[-87.4177,41.6753],[-87.4396,41.6565],[-87.4228,41.6439],[-87.4167,41.6439],[-87.4099,41.644],[-87.4087,41.644],[-87.4044,41.6413],[-87.392,41.6382],[-87.3748,41.6329],[-87.3711,41.6315],[-87.3538,41.6285],[-87.3384,41.6259],[-87.3274,41.6259],[-87.3218,41.6219],[-87.315,41.6201],[-87.3101,41.6201],[-87.3058,41.6202],[-87.3003,41.6202],[-87.296,41.6198],[-87.2831,41.6203],[-87.2702,41.6208],[-87.2223,41.6248]]]},\"properties\":{\"name\":\"Lake\",\"state\":\"IN\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5f9d21","contributors":{"authors":[{"text":"Greeman, Theodore K.","contributorId":30655,"corporation":false,"usgs":true,"family":"Greeman","given":"Theodore","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":198064,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":26008,"text":"wri924192 - 1995 - Geohydrology and water quality of stratified-drift aquifers in the middle Merrimack River basin, south-central New Hampshire","interactions":[],"lastModifiedDate":"2012-02-02T00:08:24","indexId":"wri924192","displayToPublicDate":"1996-06-01T00:00:00","publicationYear":"1995","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":"92-4192","title":"Geohydrology and water quality of stratified-drift aquifers in the middle Merrimack River basin, south-central New Hampshire","docAbstract":"The U.S. Geological Survey, in cooperation with the State of New Hampshire, Department of Environmental Services, Water Resources Division has assessed the geohydrology and water quality of stratified-drift aquifers in the middle Merrimack River basin in south-central New Hampshire. The middle Merrimack River basin drains 469 square miles; 98 square miles is underlain by stratified-drift aquifers. Saturated thickness of stratified drift within the study area is generally less than 40 feet but locally greater than 100 feet. Transmissivity of stratified-drift aquifers is generally less than 2,000 feet squared per day but locally exceeds 6, 000 feet squared per day. At present (1990), ground-water withdrawals from stratified drift for public supply are about 0.4 million gallons per day within the basin. Many of the stratified-drift aquifers within the study area are not developed to their fullest potential. The geohydrology of stratified-drift aquifers was investigated by focusing on basic aquifer properties, including aquifer boundaries; recharge, discharge, and direction of ground-water flow; saturated thickness and storage; and transmissivity. Surficial geologic mapping assisted in the determination of aquifer boundaries. Data from 757 wells and test borings were used to produce maps of water-table altitude, saturated thickness, and transmissivity of stratified drift. More than 10 miles of seismic-refraction profiling and 14 miles of seismic-reflection profiling were also used to construct the water table and saturated-thickness maps. Stratified-drift aquifers in the southern, western, and central parts of the study area are typically small and discontinuous, whereas aquifers in the eastern part along the Merrimack River valley are continuous. The Merrimack River valley aquifers formed in glacial Lakes Merrimack and Hooksett. Many other smaller discontinuous aquifers formed in small temporary ponds during deglaciation. A stratified-drift aquifer in Goffstown was analyzed for aquifer yield by use of a two-dimensional, finite-difference ground-water-flow model. Yield of the Goffstown aquifer was estimated to be 2.5 million gallons per day. Sensitivity analysis showed that the estimate of aquifer yield was most sensitive to changes in hydraulic conductivity. The amount of water induced into the aquifer from the Piscataquog River was most affected by changes in estimates of streambed conductance. Results of analysis of water samples from 10 test wells indicate that, with some exceptions, water in the stratified-drift aquifers generally meets U.S. Environmental Protection Agency primary and secondary drinking-water regulations. Water from two wells had elevated sodium concentrations, waterfront two wells had elevated concentrations of dissolved iron, and waterfront seven wells had elevated concentrations of manganese. Known areas of contamination were avoided during water-quality sampling.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nU.S. Geological Survey, Earth Science Information Center, Open-File Reports Section [distributor],","doi":"10.3133/wri924192","usgsCitation":"Ayotte, J., and Toppin, K.W., 1995, Geohydrology and water quality of stratified-drift aquifers in the middle Merrimack River basin, south-central New Hampshire: U.S. Geological Survey Water-Resources Investigations Report 92-4192, 1 v. (various pagings) :ill., maps (some col.) ;28 cm.; PGS - 149 p., 4 over-size sheets, scale 1:24,000, https://doi.org/10.3133/wri924192.","productDescription":"1 v. (various pagings) :ill., maps (some col.) ;28 cm.; PGS - 149 p., 4 over-size sheets, scale 1:24,000","costCenters":[],"links":[{"id":2007,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri924192/","linkFileType":{"id":5,"text":"html"}},{"id":123655,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_92_4192.jpg"},{"id":54767,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1992/4192/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":54768,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1992/4192/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":54769,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1992/4192/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":54770,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1992/4192/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":54771,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1992/4192/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":54772,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1992/4192/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":54773,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1992/4192/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":54774,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1992/4192/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a8b8c","contributors":{"authors":[{"text":"Ayotte, Joseph D. jayotte@usgs.gov","contributorId":1802,"corporation":false,"usgs":true,"family":"Ayotte","given":"Joseph D.","email":"jayotte@usgs.gov","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":false,"id":195634,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Toppin, Kenneth W. ktoppin@usgs.gov","contributorId":3753,"corporation":false,"usgs":true,"family":"Toppin","given":"Kenneth","email":"ktoppin@usgs.gov","middleInitial":"W.","affiliations":[],"preferred":true,"id":195635,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":25945,"text":"wri954180 - 1995 - Evaluation of ground-water resources From available data, 1992, East Molokai Volcano, Hawaii","interactions":[],"lastModifiedDate":"2023-01-13T21:44:17.179935","indexId":"wri954180","displayToPublicDate":"1996-06-01T00:00:00","publicationYear":"1995","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":"95-4180","title":"Evaluation of ground-water resources From available data, 1992, East Molokai Volcano, Hawaii","docAbstract":"Available ground-water data for East Molokai Volcano consist of well-construction information and records of ground-water pumpage, water levels, and chloride concentrations. Ground-water pumpage records are available for ten wells. Seventeen long-term (10 years or more) records of water-level and/or chloride concentration are available for eleven wells; however, only seven of these records are for observation wells. None of the available data show significant long-term changes in water level or chloride concentration; however, short-term changes due to variations in the quantity of water pumped, and rainfall are evident.\r\n\r\nEvaluation of the historical distribution and rates of ground-water pumpage, and variations in water levels and chloride concentrations is constrained by the scanty distribution of spatial and temporal data. Data show a range in water levels from greater than 850 feet above mean sea level in wells located in the windward valley of Waikolu to about 10 feet in wells located east of Kualapuu to 1 to 5 feet in the wells located along the south shore of East Molokai Volcano. An accurate contour map of water levels and chloride concentrations at the surface of the basal-water body cannot be constructed for any time period. Because water-level and chloride data are not collected at regular time intervals, many long-term records are incomplete. Information on the variation in chloride concentration with depth through the freshwater part of the basal-water body and into the zone of transition between freshwater and saltwater does not exist.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954180","usgsCitation":"Anthony, S., 1995, Evaluation of ground-water resources From available data, 1992, East Molokai Volcano, Hawaii: U.S. Geological Survey Water-Resources Investigations Report 95-4180, iii, 32 p., https://doi.org/10.3133/wri954180.","productDescription":"iii, 32 p.","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":411926,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48271.htm","linkFileType":{"id":5,"text":"html"}},{"id":54699,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4180/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123846,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4180/report-thumb.jpg"}],"country":"United States","state":"Hawaii","otherGeospatial":"East Molokai Volcano","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -156.7968576402636,\n 21.17324374217698\n ],\n [\n -156.98726313422551,\n 21.17324374217698\n ],\n [\n -156.98726313422551,\n 21.059916232762532\n ],\n [\n -156.7968576402636,\n 21.059916232762532\n ],\n [\n -156.7968576402636,\n 21.17324374217698\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cbe4b07f02db543b21","contributors":{"authors":[{"text":"Anthony, Stephen S. santhony@usgs.gov","contributorId":2507,"corporation":false,"usgs":true,"family":"Anthony","given":"Stephen S.","email":"santhony@usgs.gov","affiliations":[],"preferred":true,"id":195525,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28047,"text":"wri954055 - 1995 - Methods to estimate annual mean spring discharge to the Snake River between Milner Dam and King Hill, Idaho","interactions":[],"lastModifiedDate":"2013-11-22T13:14:41","indexId":"wri954055","displayToPublicDate":"1996-06-01T00:00:00","publicationYear":"1995","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":"95-4055","title":"Methods to estimate annual mean spring discharge to the Snake River between Milner Dam and King Hill, Idaho","docAbstract":"Many individual springs and groups of springs discharge water from volcanic rocks that form the north canyon wall of the Snake River between Milner Dam and King Hill. Previous estimates of annual mean discharge from these springs have been used to understand the hydrology of the eastern part of the Snake River Plain. Four methods that were used in previous studies or developed to estimate annual mean discharge since 1902 were (1) water-budget analysis of the Snake River; (2) correlation of water-budget estimates with discharge from 10 index springs; (3) determination of the combined discharge from individual springs or groups of springs by using annual discharge measurements of 8 springs, gaging-station records of 4 springs and 3 sites on the Malad River, and regression equations developed from 5 of the measured springs; and (4) a single regression equation that correlates gaging-station records of 2 springs with historical water-budget estimates. Comparisons made among the four methods of estimating annual mean spring discharges from 1951 to 1959 and 1963 to 1980 indicated that differences were about equivalent to a measurement error of 2 to 3 percent. The method that best demonstrates the response of annual mean spring discharge to changes in ground-water recharge and discharge is method 3, which combines the measurements and regression estimates of discharge from individual springs.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954055","usgsCitation":"Kjelstrom, L., 1995, Methods to estimate annual mean spring discharge to the Snake River between Milner Dam and King Hill, Idaho: U.S. Geological Survey Water-Resources Investigations Report 95-4055, iv, 9 p., https://doi.org/10.3133/wri954055.","productDescription":"iv, 9 p.","numberOfPages":"13","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":123596,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4055/report-thumb.jpg"},{"id":56885,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4055/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho","otherGeospatial":"Snake River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -115.25,42.0 ], [ -115.25,43.0 ], [ -114.0,43.0 ], [ -114.0,42.0 ], [ -115.25,42.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a55e4b07f02db62d060","contributors":{"authors":[{"text":"Kjelstrom, L.C.","contributorId":89104,"corporation":false,"usgs":true,"family":"Kjelstrom","given":"L.C.","email":"","affiliations":[],"preferred":false,"id":199124,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":22782,"text":"ofr95441 - 1995 - Similar agricultural areas, different ground-water quality, Red River of the North Basin, 1993-95","interactions":[],"lastModifiedDate":"2018-03-12T10:18:40","indexId":"ofr95441","displayToPublicDate":"1996-06-01T00:00:00","publicationYear":"1995","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":"95-441","title":"Similar agricultural areas, different ground-water quality, Red River of the North Basin, 1993-95","docAbstract":"The U.S. Geological Survey has studied the ground-water quality within two areas of the Red River of the North Basin in southeastern North Dakota and west-central Minnesota. Although both areas are underlain by sandy surficial aquifers over which intensive irrigated agriculture dominates the land use, their ground-water quality differs. Ground water from the eastern study area has significantly higher concentrations of nitrate and agricultural herbicides than does ground water from the western area. Major differences in rainfall and minor differences in soils, depth to ground water, and agricultural practices between these two areas can account for the differences measured in ground-water quality. These same factors may indicate changes in ground-water quality from agricultural land uses in other surficial aquifers in the Red River of the North Basin.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Mounds View, MN","doi":"10.3133/ofr95441","issn":"0094-9140","usgsCitation":"Cowdery, T., 1995, Similar agricultural areas, different ground-water quality, Red River of the North Basin, 1993-95: U.S. Geological Survey Open-File Report 95-441, 4 p., https://doi.org/10.3133/ofr95441.","productDescription":"4 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true},{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":155833,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1995/0441/report-thumb.jpg"},{"id":52211,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1995/0441/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United 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T.K.","contributorId":92658,"corporation":false,"usgs":true,"family":"Cowdery","given":"T.K.","affiliations":[],"preferred":false,"id":188868,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28467,"text":"wri954049 - 1995 - Hydrogeology and water quality of the Mississippi River alluvium near Muscatine, Iowa, June 1992 through June 1994","interactions":[],"lastModifiedDate":"2018-07-25T16:45:56","indexId":"wri954049","displayToPublicDate":"1996-05-01T00:00:00","publicationYear":"1995","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":"95-4049","title":"Hydrogeology and water quality of the Mississippi River alluvium near Muscatine, Iowa, June 1992 through June 1994","docAbstract":"A study of the Mississippi River alluvium near Muscatine, Iowa, was conducted to evaluate ground-water flow and water quality using data collected from June 1992 through June 1994. The study area included approximately 80 square miles in parts of Muscatine and Louisa Counties in Iowa and Rock Island and Mercer Counties in Illinois.
\nA steady-state, ground-water flow model was constructed using February 1993 hydrologic conditions. Model results indicate that drawdown in the lower alluvium caused by the pumping centers in Iowa extends beneath the Muscatine Slough in the northwest part of the study area and beneath the Mississippi River in the central and northern parts of the area. The primary sources of ground water in the alluvium are recharge from precipitation, leakage from the Mississippi River, and infiltration of upland runoff. The bedrock is not a major contributor of ground water to the alluvium.
\nThe areal distribution of selected water-quality properties and constituents in ground water results from several factors. Localized large chloride and nitrite-plus-nitrate nitrogen concentrations could be indicative of contamination from human activity. Specific conductance and calcium, magnesium, and sulfate concentrations are larger in ground water near the boundary between the river valley and upland area and could result from infiltration of upland runoff or lithologic differences in the alluvium. Large iron or manganese concentrations occur in the ground water near the Mississippi River and Muscatine Slough that result from microbial processes and the presence of dissolved organic carbon.
\nTemporal variations of concentrations for selected water-quality constituents in groundwater samples attest to the dynamic nature of the ground-water system as it responds to natural and human-induced changes in water quality. Leakage from the Mississippi River affects ground-water quality in the alluvium adjacent to the river. Temporal variations in water quality of the Mississippi River can be caused by seasonally, amount of discharge, or upstream human activities.
\nThe quality of ground water induced from discrete zones of the alluvium by the pumping centers in Iowa has implications for the entire ground-water resource. The ground-water flow model calculated that 10 percent of the water that enters the zone of active pumping on the Iowa side of the Mississippi River originates from the zone west and north of Muscatine Slough, and that 5.2 percent originates from the zone on the Illinois side of the Mississippi River east of the center of the river channel.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Iowa City, IA","doi":"10.3133/wri954049","collaboration":"Prepared in cooperation with Muscatine Power and Water, Muscatine, Iowa","usgsCitation":"Lucey, K., Kuzniar, R., and Caldwell, J., 1995, Hydrogeology and water quality of the Mississippi River alluvium near Muscatine, Iowa, June 1992 through June 1994: U.S. Geological Survey Water-Resources Investigations Report 95-4049, Report: vi, 74 p.; 1 plate: 30.39 x 40.43 inches, https://doi.org/10.3133/wri954049.","productDescription":"Report: vi, 74 p.; 1 plate: 30.39 x 40.43 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"links":[{"id":57269,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4049/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123670,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4049/report-thumb.jpg"},{"id":355976,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1995/4049/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Illinois, Iowa","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -91.19270324707031,\n 41.22876543240588\n ],\n [\n -91.19270324707031,\n 41.44118219439961\n ],\n [\n -90.99014282226562,\n 41.44118219439961\n ],\n [\n -90.99014282226562,\n 41.22876543240588\n ],\n [\n -91.19270324707031,\n 41.22876543240588\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685325","contributors":{"authors":[{"text":"Lucey, K.J.","contributorId":70002,"corporation":false,"usgs":true,"family":"Lucey","given":"K.J.","email":"","affiliations":[],"preferred":false,"id":199852,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kuzniar, R.L.","contributorId":44558,"corporation":false,"usgs":true,"family":"Kuzniar","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":199851,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Caldwell, J.P.","contributorId":83496,"corporation":false,"usgs":true,"family":"Caldwell","given":"J.P.","email":"","affiliations":[],"preferred":false,"id":199853,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":21717,"text":"ofr95650 - 1995 - Data report for onshore-offshore wide-angle seismic recordings in the Bering-Chukchi Sea, Western Alaska and eastern Siberia","interactions":[],"lastModifiedDate":"2017-08-02T12:32:57","indexId":"ofr95650","displayToPublicDate":"1996-05-01T00:00:00","publicationYear":"1995","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":"95-650","title":"Data report for onshore-offshore wide-angle seismic recordings in the Bering-Chukchi Sea, Western Alaska and eastern Siberia","docAbstract":"This report presents fourteen deep-crustal wide-angle seismic reflection and refraction profiles recorded onland in western Alaska and eastern Siberia from marine air gun sources in the Bering-Chukchi Seas. During a 20-day period in August, 1994, the R/V Ewing acquired two long (a total of 3754 km) deep-crustal seismic-reflection profiles on the continental shelf of the Bering and Chukchi Seas, in a collaborative project between Stanford University and the United States Geological Survey (USGS). The Ewing's 137.7 liter (8355 cu. in.) air gun array was the source for both the multichannel reflection and the wide-angle seismic data. The Ewing, operated by the Lamont-Doherty Earth Observatory, steamed northward from Nunivak Island to Barrow, and returned, firing the air gun array at intervals of either 50 m or 75 m. About 37,700 air gun shots were fired along the northward directed Lines 1 and 2, and more than 40,000 air gun shots were fired along the southward directed Line 3. The USGS and the University of Alaska, Fairbanks (UAF), deployed an array of twelve 3-component REFTEK and PDAS recorders in western Alaska and eastern Siberia which continuously recorded the air gun signals fired during the northward bound Lines 1 and 2. Seven of these recorders also continuously recorded the southward bound Line 3. These wide-angle seismic data were acquired to: (1) image reflectors in the upper to lower crust, (2) determine crustal and upper mantle refraction velocities, and (3) provide important constraints on the geometry of the Moho along the seismic lines. In this report, we describe the land recording of wide-angle data conducted by the USGS and the UAF, describe in detail how the wide-angle REFTEK and PDAS data were reduced to common receiver gather seismic sections, and illustrate the wide-angle seismic data obtained by the REFTEKs and PDAS's. Air gun signals were observed to ranges in excess of 400 km, and crustal and upper /mantle refractions indicate substantial variation in the crustal thickness along the transect.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr95650","issn":"0566-8174","usgsCitation":"Brocher, T.M., Allen, R.M., Stone, D.B., Wolf, L.W., and Galloway, B.K., 1995, Data report for onshore-offshore wide-angle seismic recordings in the Bering-Chukchi Sea, Western Alaska and eastern Siberia: U.S. Geological Survey Open-File Report 95-650, 57 p., https://doi.org/10.3133/ofr95650.","productDescription":"57 p.","costCenters":[],"links":[{"id":154559,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1995/0650/report-thumb.jpg"},{"id":51244,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1995/0650/report.pdf","text":"Report","size":"13.89.MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -175,\n 64\n ],\n [\n -158,\n 64\n ],\n [\n -158,\n 72\n ],\n [\n -175,\n 72\n ],\n [\n -175,\n 64\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac5e4b07f02db679d9a","contributors":{"authors":[{"text":"Brocher, Thomas M. 0000-0002-9740-839X brocher@usgs.gov","orcid":"https://orcid.org/0000-0002-9740-839X","contributorId":262,"corporation":false,"usgs":true,"family":"Brocher","given":"Thomas","email":"brocher@usgs.gov","middleInitial":"M.","affiliations":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"preferred":true,"id":185395,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Allen, Richard M.","contributorId":139575,"corporation":false,"usgs":false,"family":"Allen","given":"Richard","email":"","middleInitial":"M.","affiliations":[{"id":6609,"text":"UC Berkeley","active":true,"usgs":false}],"preferred":false,"id":185393,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Stone, David B.","contributorId":193572,"corporation":false,"usgs":false,"family":"Stone","given":"David","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":185392,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wolf, Lorraine W.","contributorId":72817,"corporation":false,"usgs":false,"family":"Wolf","given":"Lorraine","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":185396,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Galloway, Brian K.","contributorId":63418,"corporation":false,"usgs":false,"family":"Galloway","given":"Brian","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":185394,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":25533,"text":"wri954027 - 1995 - Geohydrology, water quality, and conceptual model of the hydrologic system Saco Landfill area, Saco, Maine","interactions":[],"lastModifiedDate":"2021-01-27T19:55:47.173605","indexId":"wri954027","displayToPublicDate":"1996-05-01T00:00:00","publicationYear":"1995","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":"95-4027","title":"Geohydrology, water quality, and conceptual model of the hydrologic system Saco Landfill area, Saco, Maine","docAbstract":"A geohydrologic study of the Saco Municipal Landfill in Saco, Maine, was done during 1993-94 to provide a preliminary interpretation of the geology and hydrology needed to guide additional studies at the landfill as part of the Superfund Program. The Saco Landfill, which was active from the early 1960's until 1986, includes three disposal areas on a 90-acre parcel. Sandy Brook, a small perennial stream, flows from north to south through the land-fill between the disposal areas. Discharge of leachate from the disposal areas to aquifers and streams has been documented since 1974. The landfill was declared a Superfund site in 1990 by the U.S. Environmental Protection Agency. Multiple lines of evidence are used in this study to indicate areas of ground-water contamination and sources of water flow in Sandy Brook. The geohydrologic system on the east side of Sandy Brook consists of an upper water-table aquifer and a lower aquifer, separated by a thick sequence of glaciomarine silt and clay. Depths to bedrock range from 60 to more than 200 ft (feet), on the basis of data from seismic-refraction studies and drilling. The upper aquifer, which is generally less than 15 ft thick, consists of fine-to medium-grained sand deposited in a shallow postglacial marine environment. The lower aquifer, which was deposited as a series of glaciomarine fans, contains two sediment types: Well-sorted sand and gravel and unsorted sediments called diamict sediments. East of Sandy Brook, the thickness of the lower aquifer ranges from 25 to 100 ft, based on drilling at the landfill. The glaciomarine silts and clays (known as the presumpscot Formation) range from 50 to more than 100 ft thick. West of Sandy Brook, the glaciomarine silt and clay is largely absent, and fractured bedrock is very close to land surface under one of the disposal areas in the northwestern part of the property. The lower aquifer is unconfined in the southwestern side of the study area; bedrock slopes towards the south, and the aquifer thickens to 100 ft at the southwestern end of the study area. Preliminary estimates of mean annual streamflow in Sandy Brook, based on a partial year of continuous record, indicate that runoff increases from approximately 2.1 ft3/s (cubic feet per second) upstream from the landfill to 2.7 ft3/s downstream from the landfill, although the drainage area down-stream is only 11 percent greater than the drainage area upstream. A water-budget estimate based on available streamflow and climatic data indicates that Sandy Brook below the landfill gains about 80 million gallons per year from sources outside the drainage-basin boundary. Possible sources include the lower aquifer north or west of the landfill area and the fractured bedrock northwest of Sandy Brook. Specific conductance of water in Sandy Brook increases downstream from the landfill. In September 1993, specific conductance was 184 liS/cm (microsiemens per centimeter at 25 degrees Celsius) upstream from the landfill and 496 uS/cm downstream from the landfill. Continuous monitoring of specific conductance in Sandy Brook shows that the downstream increase is less during periods of stormflow because of dilution. Electromagnetic terrain-conductivity surveys, results of ground-water chemical analyses, and changes in streamwater quality have been used to identify areas of likely ground-water contamination. The specific conductance of ground water exceeds 2,000 uS/cm in some areas near the landfills. This compares to specific conductances of less than 200 uS/cm in water from most shallow wells that are considered to represent background water quality. Ground water in the upper aquifer east of Sandy Brook and in the lower aquifer west of Sandy Brook has been affected by leachate flowing from the landfill areas. The extent of contamination in bedrock, if any, is unknown. Water levels measured in 16 wells were used to help determine the direction of ground-water flow. The electromagnetic terrain-conduct surveys and stream specific-conductance data support the interpretation that water in the upper aquifer flows radially away from the two disposal areas east of Sandy Brook towards Sandy Brook and other small surface-water bodies in the area. West of Sandy Brook, ground water under the third disposal area moves in the lower aquifer northeast and southeast towards Sandy Brook, where it discharges to the stream.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri954027","usgsCitation":"Nielsen, M., Stone, J.R., Hansen, B.P., and Nielsen, J., 1995, Geohydrology, water quality, and conceptual model of the hydrologic system Saco Landfill area, Saco, Maine: U.S. Geological Survey Water-Resources Investigations Report 95-4027, v, 94 p., https://doi.org/10.3133/wri954027.","productDescription":"v, 94 p.","costCenters":[],"links":[{"id":382724,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4027/report.pdf"},{"id":157697,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4027/report-thumb.jpg"}],"country":"United States","state":"Maine","city":"Saco","otherGeospatial":"Saco Landfill area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -70.46356201171875,\n 43.496518702067206\n ],\n [\n -70.41996002197266,\n 43.496518702067206\n ],\n [\n -70.41996002197266,\n 43.50872101129684\n ],\n [\n -70.46356201171875,\n 43.50872101129684\n ],\n [\n -70.46356201171875,\n 43.496518702067206\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a877c","contributors":{"authors":[{"text":"Nielsen, M.G.","contributorId":103635,"corporation":false,"usgs":true,"family":"Nielsen","given":"M.G.","email":"","affiliations":[],"preferred":false,"id":194077,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stone, J. R.","contributorId":87964,"corporation":false,"usgs":true,"family":"Stone","given":"J.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":194076,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hansen, B. P.","contributorId":45332,"corporation":false,"usgs":true,"family":"Hansen","given":"B.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":194074,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Nielsen, J.P.","contributorId":76355,"corporation":false,"usgs":true,"family":"Nielsen","given":"J.P.","email":"","affiliations":[],"preferred":false,"id":194075,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ]}