Contaminated ground water characterized by high concentrations of dissolved solids and dissolved sulfate, and in areas, by low pH and elevated concentrations of metals, is present near public-supply wells in the southwestern Salt Lake Valley. To provide State officials and water users with information concerning the potential movement of contaminated ground water to points of withdrawal in the area, an analysis of solute transport using computer models was done by the U.S. Geological Survey in cooperation with the Utah Department of Natural Resources, Division of Water Rights, and local municipalities and water users.
A three-dimensional solute-transport model was developed and couples with an existing ground-water flow model of Salt Lake Valley to simulate the movement of dissolved sulfate in ground water in southwestern Salt Lake Valley. Development and calibration of the transport model focused mainly on sulfate movement down-gradient from the Bingham Creek Reservoirs and the South Jordan evaporation ponds east of the mouth of Bingham Canyon. Estimates of transport parameters were adjusted during a calibration simulation representing conditions during 1965-93. After calibration, the transport model was used to simulate future sulfate movement for 1994-2043.
Because of uncertainty in estimated transport-parameter values, three projection transport simulations incorporating a range of probable parameter values were done to evaluate future sulfate movement and changes in sulfate concentrations at selected public-supply wells. These projection simulations produced a possible range of computed transport rates and patterns. In general, the projection simulations indicated movement of the sulfate plume east of the Bingham Creek reservoir toward public-supply wells northeast of the reservoirs and then eastward toward the Jordan River. Ground water with high concentrations of sulfate east of the South Jordan evaporation ponds is simulated as moving west to east under the Jordan River towards public-supply wells during the final 25 years of the simulation period. An increase in sulfate concentration from 200 mg/l in 2006 to 4,100 mg/l in 2022 was the largest simulated increase at public-supply wells northeast of the reservoirs. An increase in sulfate concentration from 150 mg/l in 2024 to 340 mg/l in 2043 was the largest simulated increase at public-supply wells in the south-central Salt Lake Valley just east of the Jordan River.
","language":"English","publisher":"Utah Department of Natural Resources, Division of Water Rights","publisherLocation":"Salt Lake City, UT","collaboration":"Prepared by the United States Geological Survey in cooperation with the Utah Department of Natural Resources Division of Water Rights","usgsCitation":"Lambert, P., 1996, Numerical simulation of solute transport in southwestern Salt Lake Valley, Utah: Technical Publication 110-D, vi, 44 p.","productDescription":"vi, 44 p.","numberOfPages":"53","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":332778,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":341630,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://waterrights.utah.gov/docImport/0588/05885651.pdf"},{"id":332776,"rank":1,"type":{"id":15,"text":"Index 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Lake\",\"state\":\"UT\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"586cc6bbe4b0f5ce109fa9a3","contributors":{"authors":[{"text":"Lambert, P. M.","contributorId":74380,"corporation":false,"usgs":true,"family":"Lambert","given":"P. M.","affiliations":[],"preferred":false,"id":657384,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70179114,"text":"70179114 - 1996 - Hydrology and simulation of ground-water flow in Juab Valley, Juab County, Utah.","interactions":[],"lastModifiedDate":"2016-12-30T10:12:24","indexId":"70179114","displayToPublicDate":"2016-11-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"seriesTitle":{"id":294,"text":"Technical Publication","active":false,"publicationSubtype":{"id":4}},"seriesNumber":"114","title":"Hydrology and simulation of ground-water flow in Juab Valley, Juab County, Utah.","docAbstract":"Plans to import water to Juab Valley, Utah, primarily for irrigation, are part of the Central Utah Project. A better understanding of the hydrology of the valley is needed to help manage the water resources and to develop conjunctive-use plans.
The saturated unconsolidated basin-fill deposits form the ground-water system in Juab Valley. Recharge is by seepage from streams, unconsumed irrigation water, and distribution systems; infiltration of precipitation; and subsurface inflow from consolidated rocks that surround the valley. Discharge is by wells, springs, seeps, evapotranspiration, and subsurface outflow to consolidated rocks. Ground-water pumpage is used to supplement surface water for irrigation in most of the valley and has altered the direction of groundwater flow from that of pre-ground-water development time in areas near and in Nephi and Levan.
Greater-than-average precipitation during 1980-87 corresponds with a rise in water levels measured in most wells in the valley and the highest water level measured in some wells. Less-than average precipitation during 1988-91 corresponds with a decline in water levels measured during 1988-93 in most wells. Geochemical analyses indicate that the sources of dissolved ions in water sampled from the southern part of the valley are the Arapien Shale, evaporite deposits that occur in the unconsolidated basin-fill deposits, and possibly residual sea water that has undergone evaporation in unconsolidated basin-fill deposits in selected areas. Water discharging from a spring at Burriston Ponds is a mixture of about 70 percent ground water from a hypothesized flow path that extends downgradient from where Salt Creek enters Juab Valley and 30 percent from a hypothesized flow path from the base of the southern Wasatch Range.
The ground-water system of Juab Valley was simulated by using the U.S. Geological Survey modular, three-dimensional, finite-difference, ground-water flow model. The numerical model was calibrated to simulate the steady-state conditions of 1949, multi-year transient-state conditions during 1949-92, and seasonal transient-state conditions during 1992-94. Calibration parameters were adjusted until model-computed water levels reasonably matched measured water levels. Parameters important to the calibration process include horizontal hydraulic conductivity, transmissivity, and the spatial distribution and amount of recharge from subsurface inflow and seepage from ephemeral streams to the east side of Juab Valley.
Chemical and stable-isotope data of water from wells completed in the Saginaw aquifer in the central Lower Peninsula of Michigan were used to prepare maps that show areal variation of δ18O; distribution of dissolved solids, dissolved chloride, dissolved iron, dissolved sulfate; and distribution of hydrochemical facies. Delta oxygen-18 values indicate the presence of modern meteoric water (δ18O approximately -10 parts per thousand) and glacial-age meteoric water, which is isotopically light (δ18O less than -15 parts per thousand). Isotopically light ground water is present in the Saginaw Bay Area in the eastern part of the study area. Dissolved-solids concentration ranges from 41 to 92,300 milligrams per liter, and dissolved-chloride concentrations range from less than 1 to 55,000 milligrams per liter. Dissolved-solids and dissolved-chloride concentrations increase toward Saginaw Bay. Dissolved-iron and dissolved-sulfate concentration ranges from 0.01 to 7.80 and 0.2 to 3,500 milligrams per liter, respectively. Most ground water from the Saginaw aquifer is classified as calcium bicarbonate, calcium sulfate, or sodium chloride.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Lansing, MI","doi":"10.3133/wri934220","usgsCitation":"Meissner, B.D., Long, D.T., and Lee, R.W., 1996, Selected geochemical characteristics of ground water from the Saginaw aquifer in the central Lower Peninsula of Michigan: U.S. Geological Survey Water-Resources Investigations Report 93-4220, iv, 19 p., https://doi.org/10.3133/wri934220.","productDescription":"iv, 19 p.","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":57525,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1993/4220/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":159068,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1993/4220/report-thumb.jpg"},{"id":407922,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_47906.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Michigan","otherGeospatial":"Saginaw aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -85.5,\n 42.1667\n ],\n [\n -83.25,\n 42.1667\n ],\n [\n -83.25,\n 44\n ],\n [\n -85.5,\n 44\n ],\n [\n -85.5,\n 42.1667\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5fa619","contributors":{"authors":[{"text":"Meissner, B. D.","contributorId":35364,"corporation":false,"usgs":true,"family":"Meissner","given":"B.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":200229,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Long, David T.","contributorId":20364,"corporation":false,"usgs":true,"family":"Long","given":"David","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":200228,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lee, Roger W.","contributorId":105273,"corporation":false,"usgs":true,"family":"Lee","given":"Roger","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":200230,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":30455,"text":"wri944242 - 1996 - Configuration of freshwater/saline-water interface and geologic controls on distribution of freshwater in a regional aquifer system, central lower peninsula of Michigan","interactions":[],"lastModifiedDate":"2017-02-06T14:45:56","indexId":"wri944242","displayToPublicDate":"2001-01-01T00:00:00","publicationYear":"1996","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":"94-4242","title":"Configuration of freshwater/saline-water interface and geologic controls on distribution of freshwater in a regional aquifer system, central lower peninsula of Michigan","docAbstract":"Electrical-resistivity logs and water-quality data were used to delineate the fresh water/saline-water interface in a 22,000-square-mile area of the central Michigan Basin, where Mississippian and younger geologic units form a regional system of aquifers and confining units.
Pleistocene glacial deposits in the central Lower Peninsula of Michigan contain freshwater, except in a 1,600-square-mile area within the Saginaw Lowlands, where these deposits typically contain saline water. Pennsylvanian and Mississippian sandstones are freshwater bearing where they subcrop below permeable Pleistocene glacial deposits. Down regional dip from subcrop areas, salinity of ground water progressively increases in Early Pennsylvanian and Mississippian sandstones, and these units contain brine in the central part of the basin. Freshwater is present in Late Pennsylvanian sandstones in the northern and southern parts of the aquifer system. Typically, saline water is present in Pennsylvanian sandstones in the eastern and western parts of the aquifer system.
Relief on the freshwater/saline-water interface is about 500 feet. Altitudes of the interface are low (300 to 400 feet above sea level) along a north-south-trending corridor through the approximate center of the area mapped. In isolated areas in the northern and western parts of the aquifer system, the altitude of the base of freshwater is less than 400 feet, but altitude is typically more than 400 feet. In the southern and northern parts of the aquifer system where Pennsylvanian rocks are thin or absent, altitudes of the base of freshwater range from 700 to 800 feet and from 500 to 700 feet above sea level, respectively.
Geologic controls on distribution of freshwater in the regional aquifer system are (1) direct hydraulic connection of sandstone aquifers and freshwater-bearing, permeable glacial deposits, (2) impedance of upward discharge of saline water from sandstones by lodgement tills, (3) impedance of recharge of freshwater to bedrock (or discharge of saline water from bedrock) by Jurassic red beds, and (4) vertical barriers to ground-water flow within and between sandstone units.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Lansing, MI","doi":"10.3133/wri944242","usgsCitation":"Westjohn, D.B., and Weaver, T.L., 1996, Configuration of freshwater/saline-water interface and geologic controls on distribution of freshwater in a regional aquifer system, central lower peninsula of Michigan: U.S. Geological Survey Water-Resources Investigations Report 94-4242, iv, 44 p., https://doi.org/10.3133/wri944242.","productDescription":"iv, 44 p.","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":119478,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1994/4242/report-thumb.jpg"},{"id":59235,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1994/4242/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Michigan","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": 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B.","contributorId":84401,"corporation":false,"usgs":true,"family":"Westjohn","given":"David","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":203281,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weaver, T. L.","contributorId":24339,"corporation":false,"usgs":true,"family":"Weaver","given":"T.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":203280,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":32078,"text":"ofr96534 - 1996 - Geologic Map of the Cascade Head Area, Northwestern Oregon Coast Range (Neskiwin, Nestucca Bay, Hebo, and Dolph 7.5 minute Quadrangles)","interactions":[],"lastModifiedDate":"2018-01-02T11:07:50","indexId":"ofr96534","displayToPublicDate":"1999-04-01T00:00:00","publicationYear":"1996","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":"96-534","title":"Geologic Map of the Cascade Head Area, Northwestern Oregon Coast Range (Neskiwin, Nestucca Bay, Hebo, and Dolph 7.5 minute Quadrangles)","docAbstract":"The geology of the Cascade Head area bridges the geology in the Tillamook Highlands to the north (Wells and others, 1994; 1995) with that of the Newport Embayment on the south (Snavely and others, 1976 a,b,c). The four 7.5-minute quadrangles (Neskowin, Nestucca Bay, Hebo, and Dolph) which comprise the Cascade Head area include significant stratigraphic, structural, and igneous data that are essential in unraveling the geology of the northern and central part of the Oregon Coast Range and of the adjacent continental shelf
Earlier studies (Snavely and Vokes, 1949) were of a broad reconnaissance nature because of limited access in this rugged, densely forested part of the Siuslaw National Forest. Also, numerous thick sills of late middle Eocene diabase and middle Miocene basalt mask the Eocene stratigraphic relationships. Previous mapping was hampered by a lack of precise biostratigraphic data. However, recent advances in biostratigraphy and radiometric age dating and geochemistry have provided the necessary tools to decipher stratigraphic and structural relationships in the Eocene sedimentary and volcanic rock sequences (W.W. Rau, personal communication, 1978 to 1988; Bukry and Snavely, 1988).
Many important stratigraphic and igneous relationships are displayed within the Casacde Head area:
(1) turbidite sandstone of the middle Eocene Tyee Formation, which is widespread in the central and southern part of the Oregon Coast Range (Snavely and others, 1964), was not deposited in the western part of the Cascade Head, and is of limited extent north of the map area (Wells and others, 1994);
(2) the late middle Eocene Yamhill Formation, which crops out along the west and east flank of the Oregon Coast Range, overlaps older strata and overlies an erosional unconformity on the lower Eocene Siletz River Volcanics (Snavely and others, 1990; 1991);
(3) thick sills of late middle Eocene diabase (43 Ma) are widespread in the Cascade Head area and also form much of the eastern flank of the Tillamook Highlands (Wells and others, 1994), but are rare south of the map area;
(4) Cascade Head is the northernmost eruptive center of late Eocene alkalic basalts--85 km north of the eruptive center of correlative alkalic flows of the Yachats Basalt in the Newport Embayment (Snavely and Vokes, 1949; Snavely and others, 1990; Barnes and Barnes, 1992; Davis and others, 1995);
(5) early Oligocene (33 Ma) sills and dikes of nepheline syenite and camptonite present in the Newport Embayment (Snavely and Wagner, 1961) are not found in the Cascade Head area;
(6) extensive middle Oligocene (30 Ma) granophyric gabbro sills that are widespread in the central part of the Oregon Coast Range (Snavely and Wagner, 1961; MacLeod, 1969) are not present in the Cascade Head area.
The Cascade Head area is the last segment of the Oregon Coast to receive detailed geologic mapping. Increased logging operations in the 1970's and 1980's created numerous new roadcut exposures and access to exposures in stream beds. More importantly, microfossil biostratigraphic control, available since 1970, based upon foraminifer determinations by W.W. Rau and nannofossil determinations by David Bukry provided critical information on stratigraphic succession as well as on depositional environments of the deep water (bathyal) siltstone units present in much of the Cascade Head area. These paleontologic data also permitted correlations with other sedimentary sequences mapped in the Newport Embayment and in the Tillamook Highlands as well as in western Washington.
New 7.5-minute topographic maps and aerial photographs which became available in the late 1980's provided detailed topography which can be related to the distribution of thick sills and broad landslide areas, as well as a precise geographic relationship of geologic observations in this densely forested and brush-covered terrain.
New geographic information systems (GIS) technology has produced a digitized color map of the Cascade Head area that combines the four 7.5-minute quadrangles that previously were open-filed as separate black and white 7.5-minute quadrangles (Snavely and others, 1990; 1990a; 1991; 1993).
The tectonic framework and stratigraphic architecture presented on the map of the Cascade Head area was obtained by classic geologic field methods. This information could have been obtained only through detailed observation and sampling along stream beds, road cuts, and outcrops. Remote sensing techniques were of minor help in unraveling the geology in this poorly exposed and complex terrain, a terrain that characterizes much of the Oregon and Washington Coast Ranges.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr96534","usgsCitation":"Snavely, P., Niem, A., Wong, F.L., MacLeod, N.S., Calhoun, T.K., Minasian, D.L., and Niem, W., 1996, Geologic Map of the Cascade Head Area, Northwestern Oregon Coast Range (Neskiwin, Nestucca Bay, Hebo, and Dolph 7.5 minute Quadrangles): U.S. Geological Survey Open-File Report 96-534, Report: 16 p.; 2 Plates: 44.86 x 26.85 inches and 45.27 x 28.60 inches, https://doi.org/10.3133/ofr96534.","productDescription":"Report: 16 p.; 2 Plates: 44.86 x 26.85 inches and 45.27 x 28.60 inches","costCenters":[],"links":[{"id":350270,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1996/0534/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":350271,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1996/0534/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":350269,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0534/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":167634,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0534/report-thumb.jpg"}],"scale":"24000","datum":"North American Datum of 1927","country":"United States","state":"Oregon","otherGeospatial":"Cascade Head area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124,\n 45\n ],\n [\n -123.75,\n 45\n ],\n [\n -123.75,\n 45.25\n ],\n [\n -124,\n 45.25\n ],\n [\n -124,\n 45\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a8564","contributors":{"authors":[{"text":"Snavely, Parke D. Jr.","contributorId":80328,"corporation":false,"usgs":true,"family":"Snavely","given":"Parke D.","suffix":"Jr.","affiliations":[],"preferred":false,"id":207591,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Niem, Alan","contributorId":7345,"corporation":false,"usgs":true,"family":"Niem","given":"Alan","affiliations":[],"preferred":false,"id":207587,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wong, Florence L. 0000-0002-3918-5896 fwong@usgs.gov","orcid":"https://orcid.org/0000-0002-3918-5896","contributorId":1990,"corporation":false,"usgs":true,"family":"Wong","given":"Florence","email":"fwong@usgs.gov","middleInitial":"L.","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":207586,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"MacLeod, Norman S.","contributorId":13643,"corporation":false,"usgs":true,"family":"MacLeod","given":"Norman","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":207589,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Calhoun, Tracy K.","contributorId":93114,"corporation":false,"usgs":true,"family":"Calhoun","given":"Tracy","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":207592,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Minasian, Diane L. dminasian@usgs.gov","contributorId":12906,"corporation":false,"usgs":true,"family":"Minasian","given":"Diane","email":"dminasian@usgs.gov","middleInitial":"L.","affiliations":[],"preferred":false,"id":207588,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Niem, Wendy","contributorId":67949,"corporation":false,"usgs":true,"family":"Niem","given":"Wendy","affiliations":[],"preferred":false,"id":207590,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":28783,"text":"wri964171 - 1996 - Geohydrology of the Weldon Spring ordnance works, St. Charles County, Missouri","interactions":[],"lastModifiedDate":"2019-02-25T14:40:42","indexId":"wri964171","displayToPublicDate":"1999-04-01T00:00:00","publicationYear":"1996","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":"96-4171","title":"Geohydrology of the Weldon Spring ordnance works, St. Charles County, Missouri","docAbstract":"Bedrock units at the Weldon Spring ordnance works in St. Charles County, Missouri, dip to the northeast at about 60 feet per mile, as measured by the top of the Chouteau Group. The top of the bedrock forms a generally east-west trending ridge through the Weldon Spring training area and the Weldon Spring chemical plant. This surface contains a large, broad bedrock low centered about the unnamed tributary to Dardenne Creek that contains Burgermeister spring. The low has been interpreted to be a paleodrainage that existed before deposition of glacial drift. This feature consists of smaller, more elongate paleovalleys at and west of the chemical plant where more dense drillhole data provide better definition.
The uppermost bedrock unit throughout most of the ordnance works is the BurlingtonKeokuk Limestone of Mississippian age. It is subdivided based on weathering characteristics into a lower, unweathered unit; an upper, weathered unit; and a strongly weathered subunit of the weathered unit. The unweathered unit is a light to medium gray, coarse to less commonly fine crystalline, thin to massive bedded, fossiliferous, cherty limestone. The unweathered unit can be silty or argillaceous, or can locally be dolostone or siltstone. The weathered unit is characterized by an increase in mostly horizontal fractures and partings, increased porosity, vugs, voids, breccia, and discoloration by iron oxides. A strongly weathered subunit of the weathered unit is identified in some monitoring wells where these features are particularly abundant or intense.
The overburden units are, in ascending order: residuum, basal till, glacial till, including a glacial outwash subunit, the Ferrelview Formation, loess, alluvium, and fill. Some of the thickest overburden occurs in the northern part of the training area and north of the training area and may be caused by a larger thickness of glacial drift. The paleodrainage centered about the unnamed tributary to Dardenne Creek that contains Burgermeister spring appears to have been partially filled by glacial drift, and a surface-water divide now exists southeast of the tributary.
The upper, more permeable part of the shallow aquifer consists of the residuum, basal till, glacial outwash (where there is no glacial till below it), and the weathered unit of the Burlington-Keokuk Limestone. The lower, less permeable part of the shallow aquifer consists of the unweathered unit of the Burlington-Keokuk Limestone and the Fern Glen Formation. Generally, the upper part of the shallow aquifer thins to the north, reflecting the thin to absent weathered unit north of the training area and chemical plant. A glacial drift confining unit consists of parts of the glacial till and the Ferrelview Formation. Ground water as recharge and discharge probably moves in fractures through this unit. It confines ground water where the potentiometric surface of the shallow aquifer is above its base. There are stream reaches where the streams have cut through the glacial drift confining unit to expose the underlying shallow aquifer.
A potentiometric surface map of the shallow aquifer shows a large ground-water mound in the south-central part of the training area. This mound is part of a generally east-west trending ground-water ridge through the training area and the chemical plant that defines a ground-water divide. Precipitation that percolates downward through fractures in the glacial drift confining unit recharges the shallow aquifer. Where the glacial drift confining unit is not present, precipitation can be expected to recharge the shallow aquifer more readily. There is the potential for groundwater flow in permeable overburden units where the potentiometric surface is above the top of bedrock. Generally, the residuum and locally other overburden units of the shallow aquifer potentially become more important as mediums of ground-water flow north and downgradient of the ground-water ridge. This is probably limited where clay-rich zones in the residuum confine ground water below in the bedrock. Because the thickness of the weathered unit generally decreases to the north, it generally becomes a less important medium of ground-water flow downgradient to the north. Also to the north, the potentiometric surface of the shallow aquifer is above the base of the glacial drift confining unit over a large area, indicating that the aquifer is confined. Upward ground-water gradients measured in monitoring well pairs, Burgermeister and other springs, the gaining unnamed tributary to Dardenne Creek upstream of Burgermeister spring, and Dardenne Creek indicate ground-water discharge in the northern part of the ordnance works.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964171","collaboration":"Prepared in cooperation with the U.S. Army Corps of Engineers","usgsCitation":"Mugel, D.N., 1996, Geohydrology of the Weldon Spring ordnance works, St. Charles County, Missouri: U.S. Geological Survey Water-Resources Investigations Report 96-4171, Report: iv, 47 p.; 16 Plates: 17.00 x 11.04 inches, https://doi.org/10.3133/wri964171.","productDescription":"Report: iv, 47 p.; 16 Plates: 17.00 x 11.04 inches","costCenters":[],"links":[{"id":57662,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4171/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361517,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361508,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361509,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361518,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":118798,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4171/report-thumb.jpg"},{"id":361519,"rank":14,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361510,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361520,"rank":15,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361511,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361512,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361521,"rank":16,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361522,"rank":17,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361523,"rank":18,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361513,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361514,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361515,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361516,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4171/plate-9.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Missouri","county":"St. Charles County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.94207763671875,\n 38.511639141458616\n ],\n [\n -90.5328369140625,\n 38.511639141458616\n ],\n [\n -90.5328369140625,\n 38.91133881927712\n ],\n [\n -90.94207763671875,\n 38.91133881927712\n ],\n [\n -90.94207763671875,\n 38.511639141458616\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a88b3","contributors":{"authors":[{"text":"Mugel, Douglas N. dmugel@usgs.gov","contributorId":290,"corporation":false,"usgs":true,"family":"Mugel","given":"Douglas","email":"dmugel@usgs.gov","middleInitial":"N.","affiliations":[{"id":396,"text":"Missouri Water Science Center","active":true,"usgs":true}],"preferred":true,"id":200389,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":29628,"text":"wri964187 - 1996 - Urbanization and recharge in the vicinity of East Meadow Brook, Nassau County, New York: Part 1 — Streamflow and water-table altitude, 1939-90","interactions":[],"lastModifiedDate":"2022-01-03T19:51:11.438873","indexId":"wri964187","displayToPublicDate":"1998-05-01T00:00:00","publicationYear":"1996","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":"96-4187","title":"Urbanization and recharge in the vicinity of East Meadow Brook, Nassau County, New York: Part 1 — Streamflow and water-table altitude, 1939-90","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964187","usgsCitation":"Scorca, M., 1996, Urbanization and recharge in the vicinity of East Meadow Brook, Nassau County, New York: Part 1 — Streamflow and water-table altitude, 1939-90: U.S. Geological Survey Water-Resources Investigations Report 96-4187, v, 39 p., https://doi.org/10.3133/wri964187.","productDescription":"v, 39 p.","costCenters":[],"links":[{"id":393776,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48529.htm"},{"id":58448,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4187/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":159859,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4187/report-thumb.jpg"}],"country":"United States","state":"New York","county":"Nassau County","otherGeospatial":"East Meadow Brook","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.64307403564453,\n 40.625939917833925\n ],\n [\n -73.531494140625,\n 40.625939917833925\n ],\n [\n -73.531494140625,\n 40.80081598096255\n ],\n [\n -73.64307403564453,\n 40.80081598096255\n ],\n [\n -73.64307403564453,\n 40.625939917833925\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a18e4b07f02db605251","contributors":{"authors":[{"text":"Scorca, M. P.","contributorId":21997,"corporation":false,"usgs":true,"family":"Scorca","given":"M. P.","affiliations":[],"preferred":false,"id":201844,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":31678,"text":"ofr96719 - 1996 - Preliminary bedrock geologic map of the Vermont part of the 7.5 x 15 minute Mount Ascutney and Springfield quadrangles, Windsor County, Vermont","interactions":[],"lastModifiedDate":"2022-03-28T21:13:51.191526","indexId":"ofr96719","displayToPublicDate":"1997-12-01T00:00:00","publicationYear":"1996","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":"96-719","title":"Preliminary bedrock geologic map of the Vermont part of the 7.5 x 15 minute Mount Ascutney and Springfield quadrangles, Windsor County, Vermont","docAbstract":"Bedrock in the Vermont part of the Mount Ascutney and Springfield quadrangles consists largely of, from west to east, Middle Proterozoic gneisses in the core of the Chester Dome, pre-Silurian metasedimentary, metavolcanic, and meta-igneous rocks as a cover sequence immediately above the dome, Silurian and Devonian metasedimentary and metavolcanic rocks of the Connecticut Valley sequence, and Ordovician to Silurian and Devonian metasedimentary rocks informally referred to as the New Hampshire sequence. In addition, the rocks are intruded by granitic dikes of the Devonian New Hampshire Plutonic Suite and, at Mount Ascutney, the Cretaceous White Mountain Plutonic - Volcanic Suite. The primary purpose of this report is to present preliminary results on the stratigraphic and structural relationships in the Connecticut Valley and New Hampshire sequence rocks.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr96719","usgsCitation":"Walsh, G., Armstrong, T.R., and Ratcliffe, N.M., 1996, Preliminary bedrock geologic map of the Vermont part of the 7.5 x 15 minute Mount Ascutney and Springfield quadrangles, Windsor County, Vermont: U.S. Geological Survey Open-File Report 96-719, 36 p., https://doi.org/10.3133/ofr96719.","productDescription":"36 p.","costCenters":[],"links":[{"id":121672,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_96_719.jpg"},{"id":13689,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/1996/719/","linkFileType":{"id":5,"text":"html"}},{"id":392419,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_18688.htm"}],"scale":"24000","country":"United States","state":"Vermont","county":"Windsor County","otherGeospatial":"7.5 x 15 minute Mount Ascutney and Springfield quadrangles","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -72.5,\n 43.375\n ],\n [\n -72.375,\n 43.375\n ],\n [\n -72.375,\n 43.5\n ],\n [\n -72.5,\n 43.5\n ],\n [\n -72.5,\n 43.375\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c938","contributors":{"authors":[{"text":"Walsh, G. J. 0000-0003-4264-8836","orcid":"https://orcid.org/0000-0003-4264-8836","contributorId":47409,"corporation":false,"usgs":true,"family":"Walsh","given":"G. J.","affiliations":[],"preferred":false,"id":206685,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Armstrong, T. R.","contributorId":91528,"corporation":false,"usgs":true,"family":"Armstrong","given":"T.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":206687,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ratcliffe, N. 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In 1993, the Lower Colorado River Authority implemented a water-measurement program to account for the water delivered to rice farms and to promote water conservation. During the rice-irrigation season (summer and fall) of 1995, the U.S. Geological Survey measured flows at 30 sites in the Lakeside district and 24 sites in the Gulf Coast district coincident with Lower Colorado River Authority measuring sites. In each district, the Survey made essentially simultaneous flow measurements with different types of meters twice a day once in the morning and once in the afternoon at each site on selected days for comparison with Lower Colorado River Authority measurements. One-hundred pairs of corresponding (same site, same date) Lower Colorado River Authority and U.S. Geological Survey measurements from the Lakeside district and 104 measurement pairs from the Gulf Coast district are compared statistically and graphically. For comparison, the measurement pairs are grouped by irrigation district and further subdivided by the time difference between corresponding measurements less than or equal to 1 hour or more than 1 hour. Wilcoxon signed-rank tests (to indicate whether two groups of paired observations are statistically different) on Lakeside district measurement pairs with 1 hour or less between measurements indicate that the Lower Colorado River Authority and U.S. Geological Survey measurements are not statistically different. The median absolute percent difference between the flow measurements is 5.9 percent; and 33 percent of the flow measurements differ by more than 10 percent. Similar statistical tests on Gulf Coast district measurement pairs with 1 hour or less between measurements indicate that the Lower Colorado River Authority and U.S. Geological Survey measurements are not statistically different. The median absolute percent difference between the flow measurements is 2.6 percent; and 30 percent of the flow measurements differ by more than 10 percent. The differences noted above between Lower Colorado River Authority and U.S. Geological Survey measurements with 1 hour or less between measurements and the differences between essentially simultaneous U.S. Geological Survey measurements are of similar orders of magnitude and, in some cases, very close.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Austin, TX","doi":"10.3133/wri964225","collaboration":"Prepared in cooperation with the Bureau of Reclamation, Lower Colorado River Authority, and Texas Water Development Board","usgsCitation":"Coplin, L., Liscum, F., East, J.W., and Goldstein, L., 1996, Measurement of flows for two irrigation districts in the lower Colorado River basin, Texas: U.S. Geological Survey Water-Resources Investigations Report 96-4225, iv, 38 p., https://doi.org/10.3133/wri964225.","productDescription":"iv, 38 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":118767,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4225/report-thumb.jpg"},{"id":54437,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4225/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Texas","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a28e4b07f02db611078","contributors":{"authors":[{"text":"Coplin, L.S.","contributorId":49366,"corporation":false,"usgs":true,"family":"Coplin","given":"L.S.","affiliations":[],"preferred":false,"id":194559,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Liscum, Fred","contributorId":95463,"corporation":false,"usgs":true,"family":"Liscum","given":"Fred","email":"","affiliations":[],"preferred":false,"id":194561,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"East, J. W.","contributorId":99186,"corporation":false,"usgs":true,"family":"East","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":194562,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Goldstein, L.B.","contributorId":63847,"corporation":false,"usgs":true,"family":"Goldstein","given":"L.B.","email":"","affiliations":[],"preferred":false,"id":194560,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":5163,"text":"fs21596 - 1996 - Salinity in the Colorado River in the Grand Valley, western Colorado, 1994-95","interactions":[],"lastModifiedDate":"2017-06-30T10:43:19","indexId":"fs21596","displayToPublicDate":"1997-09-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":313,"text":"Fact Sheet","code":"FS","onlineIssn":"2327-6932","printIssn":"2327-6916","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"215-96","title":"Salinity in the Colorado River in the Grand Valley, western Colorado, 1994-95","docAbstract":"Salinity, or the dissolved-solids concentration, is the measure of salts such as sodium chloride, calcium bicarbonate, and calcium sulfate that are dissolved in water. About one-half of the salinity in the Colorado River Basin is from natural sources (U.S. Department of the Interior, 1995), such as thermal springs in the Glenwood-Dotsero area, located about 90 miles upstream from Grand Junction (fig. 1). Effects of human activities, such as irrigation, reservoir evaporation, and transbasin diversions, have increased the levels of salinity in the Colorado River. High salinity can affect industrial and municipal water users by causing increased water-treatment costs, increased deterioration of plumbing and appliances, increased soap needs, and undesirable taste of drinking water. High salinity also can cause lower crop yields by reducing water and nutrient uptake by plants and can increase agricultural production costs because of higher leaching and drainage requirements. Agricultural losses might occur when salinity reaches about 700?850 milligrams per liter (U.S Department of the Interior, 1994). Figure 1. Irrigated area in the Grand Valley and locations of sampling sites for the 1994?95 salinity study of the Colorado River. The Colorado River is the major source of irrigation water to the Grand Valley (fig. 1) and also is one source of water for the Clifton Water District, which supplies domestic water to part of the eastern Grand Valley. During spring and early summer in 1994, the Colorado River in the Grand Valley had lower than average streamflow. There was concern by water users about the effect of this low streamflow on salinity in the river. In 1994, the U.S. Geological Survey (USGS), in cooperation with the Colorado River Water Conservation District, began a study to evaluate salinity in the Colorado River. This fact sheet describes results of that study. The specific objectives of the fact sheet are to (1) compare salinity in the Colorado River among different locations from Cameo to the Colorado-Utah State line, (2) assess variations in salinity for different times of the year, and (3) describe the relation between streamflow and salinity in the river.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/fs21596","usgsCitation":"Butler, D.L., and von Guerard, P.B., 1996, Salinity in the Colorado River in the Grand Valley, western Colorado, 1994-95: U.S. Geological Survey Fact Sheet 215-96, 1 sheet (4 p.) : col. ill., col. map ; 28 cm. col. ill., col. map ;, https://doi.org/10.3133/fs21596.","productDescription":"1 sheet (4 p.) : col. ill., col. map ; 28 cm. col. ill., col. map ;","costCenters":[],"links":[{"id":124927,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/fs_215_96.bmp"},{"id":582,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/fs-215-96/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Colorado","otherGeospatial":"Grand Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.42269897460938,\n 39.15349256868936\n ],\n [\n -107.72781372070312,\n 39.15349256868936\n ],\n [\n -107.72781372070312,\n 39.606746222241476\n ],\n [\n -108.42269897460938,\n 39.606746222241476\n ],\n [\n -108.42269897460938,\n 39.15349256868936\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4880e4b07f02db515edc","contributors":{"authors":[{"text":"Butler, David L.","contributorId":12843,"corporation":false,"usgs":true,"family":"Butler","given":"David","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":150527,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"von Guerard, Paul B.","contributorId":15601,"corporation":false,"usgs":true,"family":"von Guerard","given":"Paul","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":150528,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":31700,"text":"ofr96632 - 1996 - Physical characteristics of stream subbasins in the Hawk Creek-Yellow Medicine River basin, southwestern Minnesota and eastern South Dakota","interactions":[],"lastModifiedDate":"2018-04-02T10:11:15","indexId":"ofr96632","displayToPublicDate":"1997-09-01T00:00:00","publicationYear":"1996","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":"96-632","title":"Physical characteristics of stream subbasins in the Hawk Creek-Yellow Medicine River basin, southwestern Minnesota and eastern South Dakota","docAbstract":"Data that describe the physical characteristics of stream subbasins upstream from selected sites on streams in the Hawk Creek-Yellow Medicine River Basin, located in southwestern Minnesota and eastern South Dakota are presented in this report. The physical characteristics are the drainage area of the subbasin, the percentage area of the subbasin covered only by lakes, the percentage area of the subbasin covered by both lakes and wetlands, the main-channel length, and the main-channel slope. Stream sites include outlets of subbasins of at least 5 square miles, outlets of sewage treatment plants, and locations of U.S. Geological Survey low-flow, high-flow, and continuous-record gaging stations.
","language":"English","publisher":"United States","publisherLocation":"Denver, CO","doi":"10.3133/ofr96632","collaboration":"Prepared in cooperation with Minnesota Department of Transportation","usgsCitation":"Sanocki, C.A., 1996, Physical characteristics of stream subbasins in the Hawk Creek-Yellow Medicine River basin, southwestern Minnesota and eastern South Dakota: U.S. Geological Survey Open-File Report 96-632, Document: 21 p.; Plate: 44 x 36 inches, https://doi.org/10.3133/ofr96632.","productDescription":"Document: 21 p.; Plate: 44 x 36 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science 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-95.877685546875, 44.999767019181306 ], [ -95.88317871093749, 45.01238950389271 ], [ -95.88523864746094, 45.01821432797107 ], [ -95.87699890136719, 45.02355322956419 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685bab","contributors":{"authors":[{"text":"Sanocki, Christopher A.","contributorId":100432,"corporation":false,"usgs":true,"family":"Sanocki","given":"Christopher","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":206776,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":22054,"text":"ofr96732 - 1996 - Preliminary report on the distribution of modern fauna and flora at selected sites in north-central and north-eastern Florida Bay","interactions":[],"lastModifiedDate":"2020-03-27T06:58:12","indexId":"ofr96732","displayToPublicDate":"1997-08-01T00:00:00","publicationYear":"1996","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":"96-732","title":"Preliminary report on the distribution of modern fauna and flora at selected sites in north-central and north-eastern Florida Bay","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr96732","issn":"0094-9140","usgsCitation":"Brewster-Wingard, G., Ishman, S., Edwards, L.E., and Willard, D., 1996, Preliminary report on the distribution of modern fauna and flora at selected sites in north-central and north-eastern Florida Bay: U.S. Geological Survey Open-File Report 96-732, 34 p. , https://doi.org/10.3133/ofr96732.","productDescription":"34 p. ","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"links":[{"id":153089,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":1223,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pdf/of/ofr96732.html","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Florida","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.5390625,\n 30.939924331023445\n ],\n [\n -87.51708984375,\n 30.334953881988564\n ],\n [\n -85.8251953125,\n 29.99300228455108\n ],\n [\n -84.17724609375,\n 29.075375179558346\n ],\n [\n -83.1884765625,\n 28.34306490482549\n ],\n [\n -82.4853515625,\n 26.05678288577881\n ],\n [\n -80.57373046875,\n 24.627044746156027\n ],\n [\n -79.7607421875,\n 26.41155054662258\n ],\n [\n -80.04638671875,\n 27.89734922968426\n ],\n [\n -80.9912109375,\n 30.031055426540206\n ],\n [\n -81.40869140625,\n 30.713503990354965\n ],\n [\n -81.82617187499999,\n 30.80791068136646\n ],\n [\n -84.814453125,\n 30.789036751261136\n ],\n [\n -84.990234375,\n 31.109388560814963\n ],\n [\n -87.5390625,\n 30.939924331023445\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66c98d","contributors":{"authors":[{"text":"Brewster-Wingard, G. L.","contributorId":102508,"corporation":false,"usgs":true,"family":"Brewster-Wingard","given":"G. L.","affiliations":[],"preferred":false,"id":186879,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ishman, S. E.","contributorId":20346,"corporation":false,"usgs":true,"family":"Ishman","given":"S. E.","affiliations":[],"preferred":false,"id":186877,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Edwards, Lucy E. 0000-0003-4075-3317 leedward@usgs.gov","orcid":"https://orcid.org/0000-0003-4075-3317","contributorId":2647,"corporation":false,"usgs":true,"family":"Edwards","given":"Lucy","email":"leedward@usgs.gov","middleInitial":"E.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"preferred":true,"id":186876,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Willard, Debra A. 0000-0003-4878-0942","orcid":"https://orcid.org/0000-0003-4878-0942","contributorId":85982,"corporation":false,"usgs":true,"family":"Willard","given":"Debra A.","affiliations":[],"preferred":false,"id":186878,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":32945,"text":"pp1410E - 1996 - Hydrology of the southeastern Coastal Plain aquifer system in South Carolina and parts of Georgia and North Carolina","interactions":[],"lastModifiedDate":"2017-01-11T10:27:03","indexId":"pp1410E","displayToPublicDate":"1997-08-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1410","chapter":"E","title":"Hydrology of the southeastern Coastal Plain aquifer system in South Carolina and parts of Georgia and North Carolina","docAbstract":"The wedge of sediments present beneath the Coastal Plain of South Carolina and adjacent parts of Georgia and North Carolina consists of sand, silt, clay, and limestone. These strata have been subdivided into six regional aquifers: the surficial aquifer, the Floridan aquifer system, the Tertiary sand aquifer, the Black Creek aquifer, the Middendorf aquifer, and the Cape Fear aquifer. Intervening confining units separate the aquifers, except for the Floridan aquifer system and the Tertiary sand aquifer, which together function as a single hydrologic unit.
\nThe quality of ground water from the Coastal Plain aquifers of South Carolina generally is acceptable for most uses in most areas. The water in most aquifers under most of the Coastal Plain contains low concentrations of dissolved solids (less than 500 milligrams per liter) and no dominant constituents in the recharge areas. Downgradient, the water is a calcium bicarbonate or sodium bicarbonate type throughout most of the Coastal Plain. Sodium-chloride-type water is present still farther downgradient, near the coast.
\nA quasi-three-dimensional, finite-difference digital ground-water flow model was constructed to simulate flow in the Coastal Plain aquifers prior to development. The model also was used to evaluate the hydraulic responses to pumping that have occurred up to November 1982. The model consisted of five layers and a 48 by 63 node grid with a uniform square grid cell of 4 miles on a side.
\nThe Coastal Plain aquifers are recharged primarily by precipitation in their outcrop areas. Discharge is primarily as base flow to upper Coastal Plain rivers, to overlying aquifers by leakage through confining units, and to wells.
\nTotal simulated flow in the deep ground-water system was 967 cubic feet per second at the end of the transient simulation (1982). Recharge to the deep flow system simulated by the model was 793 cubic feet per second in the study area in 1982. Simulated aquifer discharge to large rivers was 660 cubic feet per second. Discharge to smaller rivers was not simulated because of the scale of the model.
\nChanges resulting from ground-water pumping were significant as of 1982. The simulated water budget indicates that in 1982, 249 cubic feet per second were discharged from the aquifer system by wells. This pumping was balanced by the following changes from predevelopment conditions: 110 cubic feet per second derived from storage, 67 cubic feet per second decrease in aquifer-to-river discharge, 44 cubic feet per second increase in net inflow from source-sinks, and a net increase in inflow of 28 cubic feet per second across boundaries. Head declines in the Black Creek and Middendorf aquifers have occurred throughout much of the eastern part of the Coastal Plain of South Carolina as a result of pumping in the Myrtle Beach and Florence areas. Simulation indicates that the dominant sources of water for upper Coastal Plain pumping centers such as the city of Florence are decrease in flow to rivers in the upper Coastal Plain and water derived from storage. The dominant sources of water for pumping centers in the Myrtle Beach area are water derived from storage, leakage from overlying aquifers, and net increases in inflow across boundaries.
\nTransmissivity values used in the flow simulation range from less than 1,000 feet squared per day near the updip limit of most aquifers to about 30,000 feet squared per day in the Middendorf aquifer in the Savannah River Plant area. Vertical hydraulic conductivity values used in simulation of confining units range from about 6x10-7 feet per day for the confining unit between the Middendorf and Black Creek aquifers in coastal areas to 3x10-2 feet per day for most of the confining units near their updip limits. Storage coefficients used in transient simulations were 0.15 where unconfined conditions exist and 0.0005 where confined conditions exist.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Denver, CO","doi":"10.3133/pp1410E","usgsCitation":"Aucott, W.R., 1996, Hydrology of the southeastern Coastal Plain aquifer system in South Carolina and parts of Georgia and North Carolina: U.S. Geological Survey Professional Paper 1410, vii, 83 p., https://doi.org/10.3133/pp1410E.","productDescription":"vii, 83 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":60848,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1410e/report.pdf","text":"Report","size":"22.81 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":121869,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1410e/report-thumb.jpg"}],"country":"United States","state":"Georgia, North Carolina, South Carolina","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -79.87060546875,\n 34.94899072578227\n ],\n [\n -80.8154296875,\n 34.34343606848294\n ],\n [\n -81.353759765625,\n 33.706062655101206\n ],\n [\n -82.265625,\n 33.293803558346596\n ],\n [\n -81.134033203125,\n 31.194007509998823\n ],\n [\n -79.47509765625,\n 32.26855544621479\n ],\n [\n -78.167724609375,\n 33.348884792201694\n ],\n [\n -77.838134765625,\n 33.8339199536547\n ],\n [\n -78.49731445312499,\n 34.97600151317591\n ],\n [\n -79.12353515625,\n 35.60371874069731\n ],\n [\n -79.87060546875,\n 34.94899072578227\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fc79f","contributors":{"authors":[{"text":"Aucott, Walter R.","contributorId":90275,"corporation":false,"usgs":true,"family":"Aucott","given":"Walter","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":209493,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":23778,"text":"ofr96735 - 1996 - Coalbed methane potential in the Appalachian states of Pennsylvania, West Virginia, Maryland, Ohio, Virginia, Kentucky, and Tennessee; an overview","interactions":[],"lastModifiedDate":"2012-02-02T00:08:18","indexId":"ofr96735","displayToPublicDate":"1997-08-01T00:00:00","publicationYear":"1996","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":"96-735","title":"Coalbed methane potential in the Appalachian states of Pennsylvania, West Virginia, Maryland, Ohio, Virginia, Kentucky, and Tennessee; an overview","docAbstract":"This report focuses on the coalbed methane (CBM) potential of the central Appalachian basin (Virginia, eastern Kentucky, southern West Virginia, and Tennessee) and the northern Appalachian basin (Pennsylvania, northern West Virginia, Maryland, and Ohio). As of April 1996, there were about 800 wells producing CBM in the central and northern Appalachian basin. For the Appalchian basin as a whole (including the Cahaba coal field, Alabama, and excluding the Black Warrior Basin, Alabama), the total CBM production for 1992, 1993, 1994, and 1995, is here estimated at 7.77, 21.51, 29.99, and 32 billion cubic feet (Bcf), respectively. These production data compare with 91.38, 104.70, 110.70, and 112.11 Bcf, respectively, for the same years for the Black Warrior Basin, which is the second largest CBM producing basin in the United States. For 1992-1995, 92-95% of central and northern Appalachian CBM production came from southwestern Virginia, which has by far the largest CBM production the Appalachian states, exclusive of Alabama. For 1994, the average daily production of CBM wells in Virginia was 119.6 Mcf/day, which is about two to four times the average daily production rates for many of the CBM wells in the northern Appalachian basin.\r\n\r\nFor 1992-1995, there is a clear increase in the percentage of CBM being produced in the central and northern Appalachian basin as compared with the Black Warrior Basin. In 1992, this percentage was 8% of the combined central and northern Appalachian and Black Warrior Basin CBM production as compared with 22% in 1995. These trends imply that the Appalachian states, except for Alabama and Virginia, are in their infancy with respect to CBM production.\r\n\r\nTotal in place CBM resources in the central and northern Appalachian basin have been variously estimated at 66-76 trillion cubic feet (Tcf), of which an estimated 14.55 Tcf (3.07 Tcf for central Appalachian basin and 11.48 Tcf for northern Appalachian basin) is technically recoverable according to Ricei s (1995) report. This compares with 20 Tcf in place and 2.30 Tcf as technically recoverable CBM for the Black Warrior Basin. These estimates should be considered preliminary because of unknown CBM potential in Ohio, Maryland, Tennessee, and eastern Kentucky. The largest potential for CBM development in the central Appalachian basin is in the Pocahontas coal beds, which have total gas values as much as 700 cf/ton, and in the New River coal beds. In the northern Appalachian basin, the greatest CBM potential is in the Middle Pennsylvanian Allegheny coal beds, which have total gas values as much as 252 cf/ton. Rice (1995) estimated a mean estimated ultimate recovery per well of 521 MMcfg for the central Appalachian basin and means of 121 and 216 MMcfg for the anticlinal and synclinal areas, respectively, of the northern Applachian basin.\r\n\r\nThere is potential for CBM development in the Valley coal fields and Richmond basin of Virginia, the bituminous region of southeastern Kentucky, eastern Ohio, northern Tennessee, and the Georges Creek coal field of western Maryland and adjacent parts of Pennsylvania. Moreover, the Anthracite region of eastern Pennsylvania, which has the second highest known total gas content for a single coal bed (687 cf/ton) in the central and northern Appalachian basin, should be considered to have a fair to good potential for CBM development where structure, bed continuity, and permeability are favorable.\r\n\r\nCBM is mainly an undeveloped unconventional fossil-fuel resource in the central and northern Appalachian basin states, except in Virginia, and will probably contribute an increasing part of total Appalachian gas production into the next century as development in Pennsylvania, West Virginia, Ohio, and other Appalachian states continue. The central and northern Appalachian basins are frontier or emerging regions for CBM exploration and development, which will probably extend well into the next century. On the basis of CBM production ","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr96735","issn":"0094-9140","usgsCitation":"Lyons, P., 1996, Coalbed methane potential in the Appalachian states of Pennsylvania, West Virginia, Maryland, Ohio, Virginia, Kentucky, and Tennessee; an overview: U.S. Geological Survey Open-File Report 96-735, 66 p. :ill.; 28 cm., https://doi.org/10.3133/ofr96735.","productDescription":"66 p. :ill.; 28 cm.","costCenters":[],"links":[{"id":157392,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0735/report-thumb.jpg"},{"id":9124,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/1996/of96-735/","linkFileType":{"id":5,"text":"html"}},{"id":53008,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0735/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6aec1b","contributors":{"authors":[{"text":"Lyons, Paul C.","contributorId":79894,"corporation":false,"usgs":true,"family":"Lyons","given":"Paul C.","affiliations":[],"preferred":false,"id":190709,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":25434,"text":"wri964138 - 1996 - Detailed study of selenium and other constituents in water, bottom sediment, soil, alfalfa, and biota associated with irrigation drainage in the Uncompahgre Project area and in the Grand Valley, west-central Colorado, 1991-93","interactions":[],"lastModifiedDate":"2025-01-08T14:26:25.607745","indexId":"wri964138","displayToPublicDate":"1997-07-01T00:00:00","publicationYear":"1996","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":"96-4138","title":"Detailed study of selenium and other constituents in water, bottom sediment, soil, alfalfa, and biota associated with irrigation drainage in the Uncompahgre Project area and in the Grand Valley, west-central Colorado, 1991-93","docAbstract":"In 1985, the U.S. Department of the Interior began a program to study the effects of irrigation drainage in the Western United States. These studies were done to determine whether irrigation drainage was causing problems related to human health, water quality, and fish and wildlife resources. Results of a study in 1991-93 of irrigation drainage associated with the Uncompahgre Project area, located in the lower Gunnison River Basin, and of the Grand Valley, located along the Colorado River, are described in this report. The focus of the report is on the sources, distribution, movement, and fate of selenium in the hydrologic and biological systems and the effects on biota. Generally, other trace- constituent concentrations in water and biota were not elevated or were not at levels of concern.
Soils in the Uncompahgre Project area that primarily were derived from Mancos Shale contained the highest concentrations of total and watrer-extractable selenium. Only 5 of 128 alfalfa samples had selenium concentrations that exceeded a recommended dietary limit for livestock. Selenium data for soil and alfalfa indicate that irrigation might be mobilizing and redistributing selenium in the Uncompahgre Project area.
Distribution of dissolved selenium in ground water is affected by the aqueous geochemical environment of the shallow ground- water system. Selenium concentrations were as high as 1,300 micrograms per liter in water from shallow wells. The highest concentrations of dissolved selenium were in water from wells completed in alluvium overlying the Mancos Shale of Cretaceous age; selenium concentrations were lower in water from wells completed in Mancos Shale residuum. Selenium in the study area could be mobilized by oxidation of reduced selenium, desorption from aquifer sediments, ion exchange, and dissolution. Infiltration of irrigation water and, perhaps nitrate, provide oxidizing conditions for mobilization of selenium from alluvium and shale residuum and for transport to streams and irrigation drains that are tributary to the Gunnison, Uncompahgre, and Colorado Rivers.
Selenium concentrations in about 64 percent of water samples collected from the lower Gunnison River and about 50 percent of samples from the Colorado River near the Colorado-Utah State line exceeded the U.S. Environmental Protection Agency criterion of 5 micrograms per liter for protection of aquatic life. Almost all selenium concentrations in samples collected during the nonirrigation season from Mancos Shale areas exceeded the aquatic-life criterion. The maximum selenium concentrations in surface-water samples were 600 micrograms per liter in the Uncompahgre Project area and 380 micrograms per liter in the Grand Valley.
Irrigation drainage from the Uncompahgre Project and the Grand Valley might account for as much as 75 percent of the selenium load in the Colorado River near the Colorado-Utah State line. The primary source areas of selenium were the eastern side of the Uncompahgre Project and the western one-half of the Grand Valley, where there is extensive irrigation on soils derived from Mancos Shale. The largest mean selenium loads from tributary drainages were 14.0 pounds per day from Loutsenhizer Arroyo in the Uncompahgre Project and 12.8 pounds per day from Reed Wash in the Grand Valley. Positive correlations between selenium loads and dissolved-solids loads could indicate that salinity-control projects designed to decrease dissolved-solids loads also could decrease selenium loads from the irrigated areas. Selenium concentrations in irrigation drainage in the Grand Valley were much higher than concentrations predicted by simple evaporative concentration of irrigation source water. Selenium probably is removed from pond water by chemical and biological processes and incorporated into bottom sediment. The maximum selenium concentration in bottom sediment was 47 micrograms per gram from a pond on the eastern side of the Uncompahgre Project.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964138","usgsCitation":"Butler, D.L., Wright, W.G., Stewart, K.C., Osmundson, B.C., Krueger, R.P., and Crabtree, D., 1996, Detailed study of selenium and other constituents in water, bottom sediment, soil, alfalfa, and biota associated with irrigation drainage in the Uncompahgre Project area and in the Grand Valley, west-central Colorado, 1991-93: U.S. Geological Survey Water-Resources Investigations Report 96-4138, ix, 136 p., https://doi.org/10.3133/wri964138.","productDescription":"ix, 136 p.","costCenters":[],"links":[{"id":123072,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4138/report-thumb.jpg"},{"id":54166,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4138/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":465849,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48486.htm","text":"Grand Valley area","linkFileType":{"id":5,"text":"html"}},{"id":465850,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48487.htm","text":"Uncompahgre area","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48b1e4b07f02db530813","contributors":{"authors":[{"text":"Butler, D. L.","contributorId":36967,"corporation":false,"usgs":true,"family":"Butler","given":"D.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":193676,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wright, W. G.","contributorId":19582,"corporation":false,"usgs":true,"family":"Wright","given":"W.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":193675,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Stewart, K. C.","contributorId":46519,"corporation":false,"usgs":true,"family":"Stewart","given":"K.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":193677,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Osmundson, B. C.","contributorId":15655,"corporation":false,"usgs":true,"family":"Osmundson","given":"B.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":193674,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Krueger, R. P.","contributorId":8890,"corporation":false,"usgs":true,"family":"Krueger","given":"R.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":193672,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Crabtree, D.W.","contributorId":10070,"corporation":false,"usgs":true,"family":"Crabtree","given":"D.W.","email":"","affiliations":[],"preferred":false,"id":193673,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":29337,"text":"wri964038C - 1996 - Benthic invertebrates of benchmark streams in agricultural areas of eastern Wisconsin — Western Lake Michigan drainages","interactions":[],"lastModifiedDate":"2022-01-21T21:01:57.760672","indexId":"wri964038C","displayToPublicDate":"1997-07-01T00:00:00","publicationYear":"1996","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":"96-4038","chapter":"C","title":"Benthic invertebrates of benchmark streams in agricultural areas of eastern Wisconsin — Western Lake Michigan drainages","docAbstract":"This study describes the benthic invertebrate communities of 20 benchmark streams in agricultural areas of eastern Wisconsin. Streams with minimal adverse effects from human activity were selected from four agricultural areas with differing surficial deposits and bedrock types (relatively homogeneous units, or RHU's). Most aquatic invertebrate orders were well represented in the 20 benchmark stream samples; 217 species and 151 genera within 56 families were identified. Diptera was the best represented order (96 species), followed by Trichoptera (42 species) and Ephemeroptera (26 species). Diptera were the most abundant organisms in terms of numbers of individuals in the sample (28 percent of the total) followed by Trichoptera (25 percent) and Ephemeroptera (13 percent). Nine species of freshwater mussels were found, but only in 5 of the 20 benchmark streams.
\nCommunity measures were calculated for the following: total number of individuals; number of species; number of families; Margalef's diversity index; percent dominant family; percent Ephemeroptera-Plecoptera-Trichoptera (EPT); ratio of EPT to Chironomidae; percent shredders; ratio of scrapers to collectors-gatherers-filterers; Hilsenhoff's Biotic Index; Hilsenhoff's family level biotic index; and mean tolerance value. The S AS statistical software package was used for calculations of variance and correlations, normality checks, and principal components analysis of these measures and to find relations between benthic-invertebrate data and environmental-setting, habitat, and water-quality data.
\nCoefficients of variation within the RHU's were as great or greater than those for all 20 streams for most measures and RHU's. The specific taxa assemblages present at the sites did not show distinct differences between RHU's or similarities within the RHU's. The covariance and the Kruskal-Wallis tests showed that the benthic invertebrate measures were not related to RHU. These results all indicate that the combined effect of the RHU variables (bedrock geology, texture of surficial deposits, and land use/land cover) were not elemental in describing invertebrate communities in the study-area streams.
\nA principal components analysis (PCA) was done on the 20 benchmark streams which used the invertebrate population measures as variables. A three-dimensional ordination plot of these components revealed that 18 of the 20 streams could be divided into three groups relative to stream size, available habitat, and water quality. The three classifications of streams include large, warmer streams with slight pollution; deep, mixed-water streams with minimal pollution; and small, cold, pristine headwater streams. The two streams not defined by the three PCA groupings were not suitable to represent benchmark conditions. One site lacked suitable quality habitat or sufficient nutrients to support a healthy population of invertebrates, causing low measures of diversity. The other site appeared to be affected by sedimentation and low flows.
\nThe classification groupings did not show any significant relations to percentage agricultural land use. Percentage of agricultural land use varied greatly within each group and the means for each group were similar. All streams in this study had some level of protection from agricultural practices in their basins. Although the intensity of agriculture is known to be a factor causing deterioration of invertebrate populations in past studies, the finding in this study indicated that the level of protection the stream received and other factors such as environmental setting and habitat could be more important to benthic invertebrates than the percentage of agriculture in the basin.
\nInformation gathered from these benchmark streams can be used as a regional reference for comparison with other streams in agricultural areas, based on communities of aquatic biota, habitat, and water quality.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964038C","usgsCitation":"Rheaume, S.J., Lenz, B.N., and Scudder, B.C., 1996, Benthic invertebrates of benchmark streams in agricultural areas of eastern Wisconsin — Western Lake Michigan drainages: U.S. Geological Survey Water-Resources Investigations Report 96-4038, vi, 39 p., https://doi.org/10.3133/wri964038C.","productDescription":"vi, 39 p.","numberOfPages":"46","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":394722,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48405.htm"},{"id":58180,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4038c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":119051,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4038c/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","otherGeospatial":"Lake Michigan","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -89.483642578125,\n 43.1090040242731\n ],\n [\n -89.483642578125,\n 45.46783598133375\n ],\n [\n -86.737060546875,\n 45.46783598133375\n ],\n [\n -86.737060546875,\n 43.1090040242731\n ],\n [\n -89.483642578125,\n 43.1090040242731\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a53e4b07f02db62b4bb","contributors":{"authors":[{"text":"Rheaume, S. J.","contributorId":70804,"corporation":false,"usgs":true,"family":"Rheaume","given":"S.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":201366,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lenz, B. N.","contributorId":106164,"corporation":false,"usgs":true,"family":"Lenz","given":"B.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":201368,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Scudder, B. C.","contributorId":71588,"corporation":false,"usgs":true,"family":"Scudder","given":"B.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":201367,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":26669,"text":"wri954278 - 1996 - Influences of environmental settings on aquatic ecosystems in the Apalachicola-Chattahoochee-Flint River basin","interactions":[],"lastModifiedDate":"2023-01-11T21:49:05.716986","indexId":"wri954278","displayToPublicDate":"1997-07-01T00:00:00","publicationYear":"1996","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":"95-4278","title":"Influences of environmental settings on aquatic ecosystems in the Apalachicola-Chattahoochee-Flint River basin","docAbstract":"The watershed boundary of the Apalachicola-Chattahoochee-Flint (ACF) River basin defines an aquatic ecosystem whose water quality is the result of complex interactions of natural and human influences on land and water resources. Topics relating to the basin's environmental setting-its physical, biological, and cultural characteristics-are summarized to provide an understanding of factors that influence water quality and the health of aquatic ecosystems.
The ACF River basin lies partly in southwestern Georgia, southeastern Alabama, and northwestern Florida and covers 19,800 square miles in the Blue Ridge, the Piedmont, and the Coastal Plain Provinces. The basin includes the drainages of the Chattahoochee River and the Flint River, which meet to form the Apalachicola River. The Apalachicola River flows into the Gulf of Mexico at Apalachicola Bay. Basin hydrology and water quality are influenced by 16 mainstem reservoirs, 13 of which are on the Chattahoochee River. Ground water in the basin is contained in six aquifers-the surficial aquifer system, the Floridan aquifer system, the Claiborne aquifer, the Clayton aquifer, the Providence aquifer, and the crystalline-rock aquifer.
Physiography, climate, and hydrology of the ACF River basin provide natural conditions that support a rich and abundant diversity of plants and animals. Although most of the ACF River basin has been altered by human activities, the basin's environment is noteworthy for its remaining biological diversity and the role it plays in sustaining biological productivity in Apalachicola Bay. The Bay produces 90 percent of Florida's and 13 percent of the Nation's oyster harvest; and functions as a nursery for penaeid shrimp, blue crabs, and a variety of fin fish. The diversity of the basin's aquatic fauna is noteworthy because the basin is home to (1) the largest number of fish species among Gulf Coast drainages east of the Mississippi River, (2) the largest assemblage of freshwater fish in Florida, (3) the largest number of mollusc species among western Florida drainages, and (4) the highest species density of amphibians and reptiles on the continent north of Mexico.
Population of the ACF River basin in 1990 was estimated at 2.6 million. Nearly 90 percent of the total population lived in Georgia, and nearly 60 percent lived in the Metropolitan Atlanta area. The 1990 basin population is projected to increase by 15 percent to 3.0 million by the year 2000, and by 30 percent to 3.4 million by 2010. The largest increases in populations are projected for the Metropolitan Atlanta area.
In 1972-76, approximately 59 percent of the basin was covered by forest, 29 percent was agricultural, 5 percent was wetland, 4 percent was urban, and 3 percent was water or barren land. Most of the original land cover of the basin has been transformed by human activity. Timber is the basin's largest cash crop and most forests consist of second-growth stands or large acreages of planted pine. The dominant agricultural land use in the Piedmont Province is pasture and confined feeding for dairy, livestock, and poultry production. Row-crop agriculture, orchards, and silviculture are most common in the Coastal Plain Province. The top five crops in order from most to least acres harvested in 1990 were peanuts, corn, soybeans, wheat, and cotton.
The water in the basin is used for public and industrial supply, irrigation, power generation, navigation, and recreation. Although most public-supply withdrawals in the Blue Ridge and Piedmont Provinces are from surface-water sources, with the exception of counties near or immediately below the Fall Line, all publicly supplied water in the Coastal Plain is withdrawn from ground-water sources. Ground water supplied 18 percent of the basin's population served by public supply. Total water withdrawn in the ACF River basin in 1990 was 2,098 million gallons per day (Mgal/d), of which Georgia withdrew 82 percent and Florida and Alabama each withdrew 9 percent. Power generation is the single largest water use. Sixteen of the basin's 22 power generating plants are located along the mainstem of the Chattahoochee River. The U.S. Army Corps of Engineers maintains a navigation channel from the mouth of the Apalachicola River to Columbus, Ga., on the Chattahoochee River and to Bainbridge, Ga., on the Flint River.
Water quality in the basin is influenced by the operation of 137 municipal wastewater-treatment facilities. In 1990, 354 Mgal/d of municipal wastewater was discharged within the ACF River basin. Eighty-eight percent of the wastewater was discharged into the Chattahoochee River basin, 10.6 percent into the Flint River basin, and 1.4 percent into the Apalachicola River basin.
Two-thirds of the 938 stream miles in the Georgia portion of the ACF River basin having water quality that does not meet or only partially meets the designated-use criteria in the Chattahoochee River basin. The Chattahoochee River is the most heavily-used water resource both in the ACF River basin and in Georgia. Urban runoff or unknown nonpoint sources are cited as the causes of water-quality regulations in 72 percent of violations. The remaining causes primarily are combined sewer overflows in the Atlanta area, and discharges from municipal or industrial treatment facilities with inadequate treatment capabilities or operational deficiencies.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954278","usgsCitation":"Couch, C.A., Hopkins, E.H., and Hardy, P.S., 1996, Influences of environmental settings on aquatic ecosystems in the Apalachicola-Chattahoochee-Flint River basin: U.S. Geological Survey Water-Resources Investigations Report 95-4278, v, 58 p., https://doi.org/10.3133/wri954278.","productDescription":"v, 58 p.","costCenters":[],"links":[{"id":411748,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48352.htm","linkFileType":{"id":5,"text":"html"}},{"id":55537,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4278/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":13458,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wrir95-4278/","linkFileType":{"id":5,"text":"html"}},{"id":119083,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4278/report-thumb.jpg"}],"country":"United States","state":"Alabama, Florida, Georgia","otherGeospatial":"Apalachicola-Chattahoochee-Flint River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -85.45,\n 34.8333\n ],\n [\n -85.45,\n 29.6267\n ],\n [\n -83.5167,\n 29.6267\n ],\n [\n -83.5167,\n 34.8333\n ],\n [\n -85.45,\n 34.8333\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f1e4b07f02db5ee565","contributors":{"authors":[{"text":"Couch, C. A.","contributorId":36972,"corporation":false,"usgs":true,"family":"Couch","given":"C.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":196802,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hopkins, E. H.","contributorId":18411,"corporation":false,"usgs":true,"family":"Hopkins","given":"E.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":196801,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hardy, P. 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Weathering and erosion have modified the original domed surfaces of the volcanoes, leaving a landscape of deep valleys and steep interfluvial ridges in the interior highlands. The Koolau Range in eastern Oahu and the Waianae Range in western Oahu are the eroded remnants of the Koolau and Waianae Volcanoes.\r\n\r\nThe origin, mode of emplacement, texture, and composition of the rocks of Oahu affect their ability to store and transmit water. The volcanic rocks are divided into four groups: (1) lava flows, (2) dikes, (3) pyroclastic deposits, and (4) saprolite and weathered basalt. Stratified sequences of thin-bedded lava flows form the most productive aquifers in Hawaii. Dikes are near-vertical sheets of massive intrusive rock that typically contain only fracture permeability. Pyroclastic deposits include ash, cinder, and spatter; they are essentially granular, with porosity and permeability similar to those of granular sediments. Weathering of basaltic rocks in the humid, subtropical climate of Oahu alters igneous minerals to clays and oxides, reducing the permeability of the parent rock. Saprolite is weathered material that has retained textural features of the parent rock.\r\n\r\nEstimates of hydraulic conductivity along the plane of dike-free lava flows tend to fall within about one order of magnitude, from about 500 to about 5,000 feet per day. Estimates of specific yield range from about 1 to 20 percent; most of the values lie within a narrow range of about 5 to 10 percent.\r\n\r\nThe occurrence of ground water on Oahu is determined by the type and character of the rocks and by the presence of geohydrologic barriers. The primary modes of freshwater occurrence on Oahu are as a basal lens of fresh ground water floating on saltwater, as dike-impounded ground water, and as perched ground water. Saltwater occurs at depth throughout much of the island.\r\n\r\nA regional aquifer system composed of the Waianae aquifer in the Waianae Volcanics and the Koolau aquifer in the Koolau Basalt is subdivided into well-defined areas by geohydrologic barriers. The aquifers are separated by the Waianae confining unit formed by weathering along the Waianae-Koolau unconformity. In some coastal areas, a caprock of sedimentary deposits overlies and confines the aquifers.\r\n\r\nThe island of Oahu has been divided into seven major ground-water areas delineated by deep-seated structural geohydrologic barriers; these areas are further subdivided by shallower internal barriers to ground-water flow. The Koolau rift zone along the eastern (windward) side of the island and the Waianae rift zone to the west (Waianae area) constitute two of the major ground-water areas. North-central Oahu is divided into three smaller ground-water areas, Mokuleia, Waialua, and Kawailoa. The Schofield ground-water area encompasses much of the Schofield Plateau of central Oahu. Southern Oahu is divided into six areas, Ewa, Pearl Harbor, Moanalua, Kalihi, Beretania, and Kaimuki. Southeastern Oahu is divided into the Waialae and Wailupe-Hawaii Kai areas. Along the northeast coast of windward Oahu is the Kahuku ground-water area.\r\n\r\nThe aquifers of Oahu contain shallow freshwater and deeper saltwater flow systems. There are five fresh ground-water flow systems: meteoric freshwater flow diverges from ground-water divides that lie somewhere within the Waianae and Koolau rift zones, forming an interior flow system in central Oahu (which is divided into the northern and southern Oahu flow systems) and exterior flow systems in western (Waianae area) Oahu, eastern (windward) Oahu, and southeastern Oahu.\r\n\r\nDevelopment of the ground-water resources on Oahu began when the first well was drilled near Honouliuli in the summer of 1879. By 1890, 86 wells had been drilled on the island. From about 1891 to about 1910, development increased rapidly with the drilling of a","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1412A","usgsCitation":"Nichols, W., Shade, P.J., and Hunt, C.D., 1996, Summary of the Oahu, Hawaii, regional aquifer-system analysis: U.S. Geological Survey Professional Paper 1412, viii, 71 p. *MISSING PAGES*, https://doi.org/10.3133/pp1412A.","productDescription":"viii, 71 p. *MISSING PAGES*","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":117833,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1412a/report-thumb.jpg"},{"id":94746,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1412a/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":486410,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4868.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Hawaii","otherGeospatial":"Oahu","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -158.3019853212155,\n 21.587546117430605\n ],\n [\n -158.12029304901154,\n 21.278411927892975\n ],\n [\n -157.95027578225046,\n 21.273733453894693\n ],\n [\n -157.70437098011104,\n 21.23768539325078\n ],\n [\n -157.61899750281034,\n 21.284611779277185\n ],\n [\n -157.7182350490743,\n 21.48980076150177\n ],\n [\n -157.97800392017717,\n 21.727240606356965\n ],\n [\n -158.3019853212155,\n 21.587546117430605\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b00e4b07f02db6981c1","contributors":{"authors":[{"text":"Nichols, William D.","contributorId":98296,"corporation":false,"usgs":true,"family":"Nichols","given":"William D.","affiliations":[],"preferred":false,"id":152342,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Shade, Patricia J.","contributorId":30618,"corporation":false,"usgs":true,"family":"Shade","given":"Patricia","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":152341,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hunt, Charles D. Jr. cdhunt@usgs.gov","contributorId":1730,"corporation":false,"usgs":true,"family":"Hunt","given":"Charles","suffix":"Jr.","email":"cdhunt@usgs.gov","middleInitial":"D.","affiliations":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"preferred":false,"id":152340,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":21710,"text":"ofr9696 - 1996 - Data base for a national mineral-resource assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the conterminous United States","interactions":[{"subject":{"id":21710,"text":"ofr9696 - 1996 - Data base for a national mineral-resource assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the conterminous United States","indexId":"ofr9696","publicationYear":"1996","noYear":false,"displayTitle":"Data Base for a National Mineral-Resource Assessment of Undiscovered Deposits of Gold, Silver, Copper, Lead, and Zinc in the Conterminous United States","title":"Data base for a national mineral-resource assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the conterminous United States"},"predicate":"SUPERSEDED_BY","object":{"id":39996,"text":"ofr2002198 - 2002 - Assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the United States: A Portable Document (PDF) recompilation of USGS Open-File Report 96-96 and Circular 1178","indexId":"ofr2002198","publicationYear":"2002","noYear":false,"title":"Assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the United States: A Portable Document (PDF) recompilation of USGS Open-File Report 96-96 and Circular 1178"},"id":1}],"supersededBy":{"id":39996,"text":"ofr2002198 - 2002 - Assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the United States: A Portable Document (PDF) recompilation of USGS Open-File Report 96-96 and Circular 1178","indexId":"ofr2002198","publicationYear":"2002","noYear":false,"title":"Assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the United States: A Portable Document (PDF) recompilation of USGS Open-File Report 96-96 and Circular 1178"},"lastModifiedDate":"2025-12-10T14:27:20.230631","indexId":"ofr9696","displayToPublicDate":"1997-06-01T00:00:00","publicationYear":"1996","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":"96-96","displayTitle":"Data Base for a National Mineral-Resource Assessment of Undiscovered Deposits of Gold, Silver, Copper, Lead, and Zinc in the Conterminous United States","title":"Data base for a national mineral-resource assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the conterminous United States","docAbstract":"For this assessment, the conterminous United States was divided into 12 regions Adirondack Mountains, Central and Southern Rocky Mountains, Colorado Plateau, East Central, Great Basin, Great Plains, Lake Superior, Northern Appalachians, Northern Rocky Mountains, Pacific Coast, Southern Appalachians, and Southern Basin and Range. The assessment, which was conducted by regional assessment teams of scientists from the USGS, was based on the concepts of permissive tracts and deposit models. Permissive tracts are discrete areas of the United States for which estimates of numbers of undiscovered deposits of a particular deposit type were made. A permissive tract is defined by its geographic boundaries such that the probability of deposits of the type delineated occurring outside the boundary is neglible. Deposit models, which are based on a compilation of worldwide literature and on observation, are sets of data in a convenient form that describe a group of deposits which have similar characteristics and that contain information on the common geologic attributes of the deposits and the environments in which they are found. Within each region, the assessment teams delineated permissive tracts for those deposit models that were judged to be appropriate and, when the amount of information warranted, estimated the number of undiscovered deposits. A total of 46 deposit models were used to assess 236 separate permissive tracts. Estimates of undiscovered deposits were limited to a depth of 1 km beneath the surface of the Earth. \r\n\r\nThe estimates of the number of undiscovered deposits of gold, silver, copper, lead, and zinc were expressed in the form of a probability distribution. Commonly, the number of undiscovered deposits was estimated at the 90th, 50th, and 10th percentiles. A Monte Carlo simulation computer program was used to combine the probability distribution of the number of undiscovered deposits with the grade and tonnage data sets associated with each deposit model to obtain the probability distribution for undiscovered metal.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr9696","issn":"0566-8174","usgsCitation":"Ludington, S.D., Cox, D.P., and McCammon, R., 1996, Data base for a national mineral-resource assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the conterminous United States (Superseded by OFR 2002-198): U.S. Geological Survey Open-File Report 96-96, HTML Document; CD-ROM, https://doi.org/10.3133/ofr9696.","productDescription":"HTML Document; CD-ROM","costCenters":[{"id":595,"text":"U.S. Geological 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2002-198","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c9c9","contributors":{"authors":[{"text":"Ludington, S. D.","contributorId":80682,"corporation":false,"usgs":true,"family":"Ludington","given":"S.","middleInitial":"D.","affiliations":[],"preferred":false,"id":185360,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cox, D. P.","contributorId":82689,"corporation":false,"usgs":true,"family":"Cox","given":"D.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":185361,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McCammon, R.B.","contributorId":17218,"corporation":false,"usgs":true,"family":"McCammon","given":"R.B.","email":"","affiliations":[],"preferred":false,"id":185359,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":30532,"text":"wri964122 - 1996 - Use of dye tracing in water-resources investigations in Wyoming, 1967-94","interactions":[],"lastModifiedDate":"2012-02-02T00:09:12","indexId":"wri964122","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-4122","title":"Use of dye tracing in water-resources investigations in Wyoming, 1967-94","docAbstract":"During 1967-94, the U.S. Geological Survey made numerous applications of dye tracing for water-resources investigations in Wyoming. Many of the dye tests were done in cooperation with other agencies. Results of all applications, including some previously unpublished, are described. A chronology of past applications in Wyoming and a discussion of potential future applications are included. Time-of-travel and dispersion measurements were made in a 113-mile reach of the Wind/Bighorn River below Boysen Dam; a 117-mile reach of the Green River upstream from Fontenelle Reservoir and a 70-mile reach downstream; parts of four tributaries to the Green (East Fork River, 39 miles; Big Sandy River, 112 miles; Horse Creek, 14 miles; and Blacks Fork, 14 miles); a 75-mile reach of the Little Snake River along the Wyoming-Colorado State line; and a 95-mile reach of the North Platte River downstream from Casper. Reaeration measurements were made during one of the time-of-travel measurements in the North Platte River. Sixty-eight dye-dilution measurements of stream discharge were made at 22 different sites. These included 17 measurements for verifying the stage-discharge relations for streamflow-gaging stations on North and South Brush Creeks near Saratoga, and total of 29 discharge measurements at 12 new stations at remote sites on steep, rough mountain streams crossing limestone outcrops in northeastern Wyoming. The largest discharge measured by dye tracing was 2,300 cubic feet per second. In karst terrane, four losing streams-North Fork Powder River, North Fork Crazy Woman Creek, Little Tongue River, and Smith Creek-were dye-tested. In the Middle Popo Agie River, a sinking stream in Sinks Canyon State Park, a dye test verified the connection of the sink (Sinks of Lander Cave) to the rise, where flow in the stream resumes.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/wri964122","usgsCitation":"Wilson, J.F., and Rankl, J., 1996, Use of dye tracing in water-resources investigations in Wyoming, 1967-94: U.S. Geological Survey Water-Resources Investigations Report 96-4122, vi, 64 p. :ill, maps ;28 cm., https://doi.org/10.3133/wri964122.","productDescription":"vi, 64 p. :ill, maps ;28 cm.","costCenters":[],"links":[{"id":161208,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4122/report-thumb.jpg"},{"id":59309,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4122/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e487ee4b07f02db514c07","contributors":{"authors":[{"text":"Wilson, J. F. Jr.","contributorId":99541,"corporation":false,"usgs":true,"family":"Wilson","given":"J.","suffix":"Jr.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":203413,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rankl, J.G.","contributorId":107733,"corporation":false,"usgs":true,"family":"Rankl","given":"J.G.","affiliations":[],"preferred":false,"id":203414,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":26901,"text":"wri964218 - 1996 - Hydraulic conductivity of the streambed, east branch Grand Calumet River, northern Lake County, Indiana","interactions":[],"lastModifiedDate":"2016-05-16T07:57:41","indexId":"wri964218","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-4218","title":"Hydraulic conductivity of the streambed, east branch Grand Calumet River, northern Lake County, Indiana","docAbstract":"Horizontal and vertical hydraulic conductivity of the Streambed were estimated from results of hydraulic tests along four transects across the east branch Grand Calumet River in northern Lake County, Indiana. Tests were done in two types of temporary wells installed in the Streambed 2-inch-diameter wells that had a 1- or 2-foot length of wire-wrapped screen and 3-inch-diameter wells that were open at the ends. When possible, the hydraulic tests included monitoring both falling- and rising-water levels. A total of 47 tests for horizontal hydraulic conductivity and 20 tests for vertical hydraulic conductivity were done.
\nData collected during the tests were analyzed by use of methods developed by earlier investigators. Horizontal hydraulic conductivity of the streambed was varied and ranged from 1.Ox1O-2 to 1.2x1O+3 feet per day. Compared to the previously reported range of horizontal hydraulic conductivity for the Calumet aquifer, 6.5X10-1 to 3.6x1O+2 feet per day, results of 24 hydraulic tests in the streambed of the east branch Grand Calumet River were within the reported range, 18 were less than the lowest reported value, and 5 were greater than the highest reported value.
\nVertical hydraulic conductivity of the streambed was less varied than horizontal hydraulic conductivity and ranged from 3.Ox1O-1 to 7.3x1O+1 feet per day. The ratio between horizontal and vertical hydraulic conductivity calculated for each transect ranged from 1:0.09 to 1:8.5.
\nThe hydraulic conductivity of the streambed generally was dependant on the type of sediments in the part of the streambed that was tested. Although most of the streambed contained soft, fine-grained sediments, parts of the streambed also contained fill materials including coal, cinders, and concrete and asphalt rubble. The highest values of horizontal hydraulic conductivity generally were calculated from data collected at locations where the streambed contained fill materials, particularly concrete and asphalt rubble. Horizontal hydraulic conductivities determined for 11 hydraulic tests in predominantly fill materials ranged from 1.2x1O+1 to 1.2x1O+3 feet per day and averaged 5.6x1O+2 feet per day. The lowest values of horizontal hydraulic conductivity were calculated from data collected at locations where the streambed contained fine-grained sediments. Horizontal hydraulic conductivities determined for 36 hydraulic tests in predominantly fine-grained sediments ranged from 1.Ox1O-2 to 2.4x1O+2 feet per day and averaged 1.5x1O+1 feet per day.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964218","collaboration":"Indiana Department of Environmental Management","usgsCitation":"Duwelius, R., 1996, Hydraulic conductivity of the streambed, east branch Grand Calumet River, northern Lake County, Indiana: U.S. Geological Survey Water-Resources Investigations Report 96-4218, v, 37 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri964218.","productDescription":"v, 37 p. :ill., maps ;28 cm.","startPage":"1","endPage":"37","numberOfPages":"41","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":125111,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4218/report-thumb.jpg"},{"id":55782,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4218/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Indiana","county":"Lake","otherGeospatial":"Grand Calumet River","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":"4f4e48cfe4b07f02db54629e","contributors":{"authors":[{"text":"Duwelius, R.F.","contributorId":28250,"corporation":false,"usgs":true,"family":"Duwelius","given":"R.F.","affiliations":[],"preferred":false,"id":197217,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":26144,"text":"wri964209 - 1996 - Hydrogeology and water quality of the shallow aquifer system at the Explosive Experimental Area, Naval Surface Warfare Center, Dahlgren site, Dahlgren, Virginia","interactions":[],"lastModifiedDate":"2023-04-13T19:58:23.68834","indexId":"wri964209","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-4209","title":"Hydrogeology and water quality of the shallow aquifer system at the Explosive Experimental Area, Naval Surface Warfare Center, Dahlgren site, Dahlgren, Virginia","docAbstract":"In October 1993, the U.S. Geological Survey began a study to characterize the hydrogeology of the shallow aquifer system at the Explosive Experimental Area, Naval Surface Warfare Center, Dahlgren Site, Dahlgren, Virginia, which is located on the Potomac River in the Coastal Plain Physiographic Province. The study provides a description of the hydrogeologic units, directions of ground-water flow, and back-ground water quality in the study area to a depth of about 100 feet. Lithologic, geophysical, and hydrologic data were collected from 28 wells drilled for this study, from 3 existing wells, and from outcrops.
The shallow aquifer system at the Explosive Experimental Area consists of two fining-upward sequences of Pleistocene fluvial-estuarine deposits that overlie Paleocene-Eocene marine deposits of the Nanjemoy-Marlboro confining unit. The surficial hydrogeologic unit is the Columbia aquifer. Horizontal linear flow of water in this aquifer generally responds to the surface topography, discharging to tidal creeks, marshes, and the Potomac River, and rates of flow in this aquifer range from 0.003 to 0.70 foot per day.
The Columbia aquifer unconformably overlies the upper confining unit 12-an organic-rich clay that is 0 to 55 feet thick. The upper confining unit conformably overlies the upper confined aquifer, a 0- to 35-feet thick unit that consists of interbedded fine-grained to medium-grained sands and clay. The upper confined aquifer probably receives most of its recharge from the adjacent and underlying Nanjemoy-Marlboro confining unit. Water in the upper confined aquifer generally flows eastward, northward, and northeastward at about 0.03 foot per day toward the Potomac River and Machodoc Creek.
The Nanjemoy-Marlboro confining unit consists of glauconitic, fossiliferous silty fine-grained sands of the Nanjemoy Formation. Where the upper confined system is absent, the Nanjemoy-Marlboro confining unit is directly overlain by the Columbia aquifer. In some parts of the Explosive Experimental Area, horizontal hydraulic conductivities of the Nanjemoy-Marlboro confining unit and the Columbia aquifer are similar (from 10-4 to 10-2 foot per day), and these units effectively combine to form a thick (greater than 50 feet) aquifer.
The background water quality of the shallow aquifer system is characteristic of ground waters in the Virginia Coastal Plain Physiographic Province. Water in the Columbia aquifer is a mixed ionic type, has a median pH of 5.9, and a median total dissolved solids of 106 milligrams per liter. Water in the upper confined aquifer and Nanjemoy-Marlboro confining unit is a sodium- calcium-bicarbonate type, and generally has higher pH, dissolved solids, and alkalinity than water in the Columbia aquifer. Water in the upper confined aquifer and some parts of the Columbia aquifer is anoxic, and it has high concentrations of dissolved iron, manganese, and sulfide.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964209","usgsCitation":"Bell, C.F., 1996, Hydrogeology and water quality of the shallow aquifer system at the Explosive Experimental Area, Naval Surface Warfare Center, Dahlgren site, Dahlgren, Virginia: U.S. Geological Survey Water-Resources Investigations Report 96-4209, v, 37 p., https://doi.org/10.3133/wri964209.","productDescription":"v, 37 p.","costCenters":[],"links":[{"id":54940,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4209/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122911,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4209/report-thumb.jpg"},{"id":415729,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48543.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Virginia","city":"Dahlgren","otherGeospatial":"Explosive Experimental Area, Naval Surface Warfare Center","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -77.0597,\n 38.3167\n ],\n [\n -77.0597,\n 38.279\n ],\n [\n -77.0167,\n 38.279\n ],\n [\n -77.0167,\n 38.3167\n ],\n [\n -77.0597,\n 38.3167\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ae4b07f02db625174","contributors":{"authors":[{"text":"Bell, C. F.","contributorId":14449,"corporation":false,"usgs":true,"family":"Bell","given":"C.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":195893,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":24371,"text":"ofr96468 - 1996 - Hydrologic data for wetland sites at Millington, Shelby County, and Huntingdon, Carroll County, Tennessee, May 1994 through September 1995","interactions":[],"lastModifiedDate":"2012-02-02T00:08:11","indexId":"ofr96468","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-468","title":"Hydrologic data for wetland sites at Millington, Shelby County, and Huntingdon, Carroll County, Tennessee, May 1994 through September 1995","docAbstract":"Hydrologic data at two wetland sites near Millington and Huntingdon in West Tennessee were collected to assist efforts by the Tennessee Department of Transportation to determine hydrologic conditions at the sites prior to wetland restoration. The Millington site is located along the Big Creek Drainage Canal east of State Route 240. Water levels were monitored in thirteen 8-inch-diameter wells from July 1994 through September 1995. Water-level recorders provided continuous measurement of water level during periods of wetland inundation and depth to water table during periods of noninundation. A crest-stage indicator and a continuous-stage recorder were installed to monitor surface-water fluctuation. Precipitation data were recorded to determine timing and duration of rainfall events. Land surface at the wells was inundated from 0 to 48 percent of the study period. Additionally, water levels at the wells were within 1.5 feet of the land surface from 0 to 56 percent of the study period. The Huntingdon study site is located along the Crooked Creek Drainage Canal at State Route 22. Ground-water levels were monitored in two wells (wells W-1 and W-2) with continuous water- level recorders from May 1994 through September 1995. Water levels did not rise above land surface at either well during the study. Water levels at wells W-1 and W-2 were within 1.5 feet of the land surface 46 and 50 percent of the study period, respectively. Surface-water stage was monitored at a pond on the mitigation site.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/ofr96468","issn":"0094-9140","usgsCitation":"Robinson, J.A., and Diehl, T., 1996, Hydrologic data for wetland sites at Millington, Shelby County, and Huntingdon, Carroll County, Tennessee, May 1994 through September 1995: U.S. Geological Survey Open-File Report 96-468, iv, 31 p. :ill, maps ;28 cm., https://doi.org/10.3133/ofr96468.","productDescription":"iv, 31 p. :ill, maps ;28 cm.","costCenters":[],"links":[{"id":1721,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/ofr96468","linkFileType":{"id":5,"text":"html"}},{"id":156258,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a1ce4b07f02db607c31","contributors":{"authors":[{"text":"Robinson, J. A.","contributorId":57417,"corporation":false,"usgs":true,"family":"Robinson","given":"J.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":191797,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Diehl, T.H.","contributorId":89170,"corporation":false,"usgs":true,"family":"Diehl","given":"T.H.","email":"","affiliations":[],"preferred":false,"id":191798,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}