The Green Bay area, which includes parts of Brown, Outagamie, and Shawano Counties, has an area of about 525 square miles in eastern Wisconsin at the south end of Green Bay. In 1960, it had a population estimated at 124,000; Green Bay, the largest city in the area, had a population of 62,888. The Green Bay area is underlain by a basement complex of crystalline rocks of Precambrian age. Sedimentary rocks of Cambrian, Ordovician, and Silurian ages overlie the crystalline rocks. These rocks are divided, in ascending order, as follows: The Dresbach Group, Franconia Sandstone, and Trempealeau Formation of Cambrian age; the Prairie du Chien Group, St. Peter Sandstone, Platteville Formation, and Maquoketa Shale of Ordovician age; and the Niagara Dolomite of Silurian age. The Maquoketa Shale and Niagara Dolomite are present only in the eastern part of the area. Unconsolidated deposits, largely of Pleistocene age and glacial origin, overlie the older rocks in most of the area. The rocks of the Dresbach Group, Franconia Sandstone, Trempealeau Formation, Prairie du Chien Group, and St. Peter Sandstone are connected hydraulically and can be considered to form one aquifer, called the sandstone aquifer. The sandstone aquifer is the principal source of ground-water supply in the Green Bay area and is one of the most productive water-bearing units in Wisconsin. All the public water supplies in the area, except the supply for the city of Green Bay, and many of the industrial water supplies are obtained from wells tapping the sandstone aquifer. Rates of discharge of individual wells range from about 200 to 1,000 gallous per minute. The city of Green Bay also obtained its water supply from wells tapping the sandstone aquifer until August 1957, when it began using Lake Michigan as a source of water supply. Several industries also use large quantities of surface water. The Niagara Dolomite, although largely undeveloped, is potentially an important aquifer, in the eastern part of the area. Small amounts of water are obtained from dolomite of the Platteville Formation and from sand and gravel deposits of Pleistocene age. Recharge to the sandstone aquifer in the Green Bay area is derived chiefly from precipitation that infiltrates at or near the outcrop area of the aquifer in northwestern Brown County, eastern Outagamie and Shawano Counties, and southern Oconto County. The amount of recharge is estimated to be at least 30 mgd (million gallons per day). Withdrawals of water from wells tapping the sandstone aquifer in the area began when the first well was drilled in 1886. The withdrawals gradually increased to an average of about 6 mgd in 1940, about 10 mgd in 1950, and about 13 mgd in January-July of 1957, after which time the city of Green Bay discontinued pumping from wells. From August 1957 through 1960, average annual withdrawals of water remained relatively constant at about 5 mgd. Water levels in wells tapping the sandstone aquifer persistently declined until August 1957 as a result of the gradually increasing withdrawals of water. In the area of concentrated ground-water withdrawals in downtown Green Bay, the piezometric surface, which had been about 100 feet above land surface in 1886, was about 340 feet below land surface in 1957. The cessation of pumping by the city of Green Bay in August 1957 resulted in a decrease in withdrawals of ground water from about 13.1 mgd in the first half of 1957 to about 5.3 mgd in the last half and a rapid recovery in water levels. ]n the area of concentrated withdrawals, the piezometric surface had recovered about 300 feet by September 1960. Rises in water levels were recorded throughout the Green Bay area, with the amount of the rise depending on the distance from the Green Bay city wells. In September 1960, water levels appeared to be affected more by local variations in the rates of pumping than by the recovery resulting from 1957 reduction in pumping. Much additional ground water could
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1669J","collaboration":"Prepared in cooperation with the Wisconsin Geological and Natural History Survey","usgsCitation":"Knowles, D., 1964, Ground-water conditions in the Green Bay area, Wisconsin, 1950-60: U.S. Geological Survey Water Supply Paper 1669, Report: iv, 37 p.; 6 Plates: 20.00 x 33.40 inches or smaller, https://doi.org/10.3133/wsp1669J.","productDescription":"Report: iv, 37 p.; 6 Plates: 20.00 x 33.40 inches or smaller","numberOfPages":"37","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":137710,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669j/report-thumb.jpg"},{"id":27532,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27533,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27534,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27535,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27536,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27537,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27538,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669j/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","otherGeospatial":"Green Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -88.28475952148438,\n 44.21075694234126\n ],\n [\n -88.28475952148438,\n 44.71161010858431\n ],\n [\n -87.82058715820312,\n 44.71161010858431\n ],\n [\n -87.82058715820312,\n 44.21075694234126\n ],\n [\n -88.28475952148438,\n 44.21075694234126\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66d218","contributors":{"authors":[{"text":"Knowles, Doyle B.","contributorId":85566,"corporation":false,"usgs":true,"family":"Knowles","given":"Doyle B.","affiliations":[],"preferred":false,"id":144579,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2046,"text":"wsp1499G - 1964 - Water resources of the Green Bay area, Wisconsin","interactions":[],"lastModifiedDate":"2021-08-16T21:39:30.070959","indexId":"wsp1499G","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1499","chapter":"G","title":"Water resources of the Green Bay area, Wisconsin","docAbstract":"The Green Bay area comprises an area of about 525 square miles in eastern Wisconsin at the south end of Green Bay. It includes the western three-fourths of Brown County and the eastern one-ninth of Outagamie County. In 1960, the population of the area was estimated at 124,000.
\nThe most prominent topographic feature is the northwest-facing, southwestward trending Niagara escarpment. The area northwest of the escarpment drains into Green Bay via the Fox River, Suamico River, Duck Creek, and their tributaries. The area southeast of the escarpment is drained by streams that flow into Lake Michigan.
\nThe chief sources of surface water in the Green Bay area are the Fox River, Green Bay, and Lake Michigan. Smaller amounts of water are available from the East and Suamico Rivers and other streams. A sandstone aquifer is the principal source of the ground-water supply. The Niagara dolomite, although largely undeveloped, is potentially an important aquifer in the eastern part of the area. Small amounts of water are obtained also from the Platteville formation and from deposits of Pleistocene and Recent age. Water from the surfaceand ground-water sources is moderately hard to very hard.
\nThe Fox River, tributary to Lake Michigan at Green Bay, is a significant source of water for industrial use in the Green Bay area. The Menasha Dam, which controls release of water from the Lake Winnebago pool, is the major regulation on the Fox River, and it has considerable effect in reducing peak flows and supplementing low flows in the lower Fox River. The average discharge of the lower Fox River for the period 1898-1959, as measured at the gaging station at Rapide Croche Dam, was 2,687 mgd (million gallons per day). The longest consecutive period during which the discharge averaged less than 500 mgd was 80 days. The average discharge can be expected to fall below 700 mgd about once every 5 years for a 7-day period. In 1959, the average withdrawal of water from the Fox River was about 62 mgd. The water in the river is of the calcium magnesium bicarbonate type and is hard.
\nThe small streams in the area are utilized chiefly for stock watering; some of the water, however, is used for irrigation. The water in the small streams is more highly mineralized than the water in the Fox River and is very hard.
\nLarge quantities of water are available from Green Bay, but the disposal of industrial waste into the bay has restricted the use of the water. The major withdrawal is for condenser cooling, and, in 1959, it averaged about 415 mgd. The water from Green Bay is moderately hard but is of better chemical quality than the water from the Fox River and the small streams in the area.
\nThe only withdrawals of water from Lake Michigan for use in the Green Bay area are made by the city of Green Bay. In 1959, these withdrawals averaged 7.8 mgd.
\nThe lower Fox River is not subject to extremes of flow owing to the dampening effect of the Lake Winnebago pool and the regulation of flow at Menasha Dam. Cloudbursts over the lower Fox River valley below Menasha Dam, however, have occasionally caused extremely high water, as in 1922, when the discharge at the mouth of the Fox River was estimated to be about 50,000 mgd. Daily discharges greater than about 13,000 mgd occurred only 7 times in the period 1918-59. The 50-year flood of 15,500 mgd represents an average runoff of less than 2.6 mgd per square mile of drainage area, a relatively low runoff for a 50-year flood in Wisconsin.
\nThe sandstone aquifer is the principal source of ground water in the Green Bay area and furnishes water for public supply and industrial use. This aquifer includes rocks of Late Cambrian age, and the Prairie du Chien group and St. Peter sandstone of Ordovician age; it ranges in thickness from 550 to 640 feet. Ground water is found in openings along fractures and bedding planes and in the interstices between sand grains.
\nThe sandstone aquifer can support additional development of large supplies of ground water. Wells can be developed in most of the area that will yield 500 gpm (gallons per minute) or more, provided they are properly spaced and penetrate the entire thickness of the aquifer. It is estimated that the perennial yield of the sandstone in the Green Bay area could be at least 30 mgd if the aquifer is properly developed; only 5.4 mgd was withdrawn in 1959. The water from this sandstone aquifer is of the calcium magnesium bicarbonate type, is very hard, and, at a few places, contains objectionable amounts of iron.
\nThe Niagara dolomite, potentially a source of moderate to large quantities of water in the eastern part of the area, probably will yield 500 gpm or more to wells.
\nIn 1959, the average withdrawal of water for all uses was estimated at 495 mgd, of which 98.2 percent was from surface-water sources and 1.8 percent was from wells. About 485 mgd of water was withdrawn for industrial use, 6 mgd for public supply, and 4 mgd for rural use. The industrial use of water averaged 441 mgd for condenser cooling, 38 mgd fot processing by the paper industry, and 6 mgd for other industrial uses. The city of Green Bay used 7.8 mgd of water from Lake Michigan; other public supplies in the area used 2.6 mgd from wells. Of the withdrawals of water for rural use, about 75 percent was from wells and about 25 percent was from streams.
\nThe discharge of wastes into the lower Fox River and its tributary streams has altered the quality of the natural water. The wastes consist chiefly of treated municipal sewage and treated and untreated wastes from the paper industry, rendering plants, a sugar mill, and other industries. The industrial waste makes up about 90 percent of the oxygen-demand loading in the lower Fox River, and treated municipal sewage accounts for about 10 percent. The dissolved-oxygen concentration of water in the lower Fox River decreases rapidly in the vicinity of Green Bay during the summer when the river water is warm. If the periods when the river water is warmest, generally during July and early August, were to coincide with periods of lowest annual streamflow, generally in late August, the river would be unable to assimilate the loading of decomposable organic matter.
\nIn an emergency, industrial and public supply wells could supply at least 6 mgd for a sustained period and probably as much as 10 mgd for a period of several days. Six of the wells that formerly supplied the city of Green Bay are maintained in operating condition and could furnish about the same quantity of water as the industrial and other public supply wells. Small streams in the area would be supplemental sources of water, and the water in the Fox River and Green Bay is easily accessible.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Water resources of industrial regions: A summary of the source, occurrence, availability, and use of water in the area","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1499G","usgsCitation":"Knowles, D.B., Dreher, F.C., and Whetstone, G.W., 1964, Water resources of the Green Bay area, Wisconsin: U.S. Geological Survey Water Supply Paper 1499, Report: v, 67 p.; 1 Plate: 23.50 x 31.95 inches, https://doi.org/10.3133/wsp1499G.","productDescription":"Report: v, 67 p.; 1 Plate: 23.50 x 31.95 inches","numberOfPages":"78","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":27567,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499g/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27568,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499g/report.pdf"},{"id":387952,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24443.htm"},{"id":137727,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499g/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","county":"Brown County, Oconto County, Outagamie County","city":"Green Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -88.25,\n 44.25\n ],\n [\n -88.25,\n 44.6670\n ],\n [\n -87.90,\n 44.6670\n ],\n [\n -87.90,\n 44.25\n ],\n [\n -88.25,\n 44.25\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5fe4b07f02db634ad6","contributors":{"authors":[{"text":"Knowles, Doyle Blewer","contributorId":9633,"corporation":false,"usgs":true,"family":"Knowles","given":"Doyle","email":"","middleInitial":"Blewer","affiliations":[],"preferred":false,"id":144585,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dreher, F. C.","contributorId":93878,"corporation":false,"usgs":true,"family":"Dreher","given":"F.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":144587,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Whetstone, George Walter","contributorId":30603,"corporation":false,"usgs":true,"family":"Whetstone","given":"George","email":"","middleInitial":"Walter","affiliations":[],"preferred":false,"id":144586,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2065,"text":"wsp1578 - 1964 - Geology and ground-water resources of the Bristol-Plainville-Southington area, Connecticut","interactions":[],"lastModifiedDate":"2023-01-11T19:59:47.775386","indexId":"wsp1578","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1578","title":"Geology and ground-water resources of the Bristol-Plainville-Southington area, Connecticut","docAbstract":"The Bristol-Plainville-Southington area straddles the boundary between the New England Upland and the Connecticut Valley Lowland sections of the New England physiographic province. The western parts of Bristol are Southington lie in the New England Upland section, an area of rugged topography underlain by metamorphic rocks of Palezoic age. The eastern part of the area, to the east of a prominent scarp marking the limit of the metamorphic rocks, is in the Connecticut Valley Lowland and is underlain by sedimentary rocks and interbedded basaltic lava flows of Triassic age. The lowland is characterized for the most part by broad valleys and low intervening linear hills, but in the eastern parts of Plainville and Southington, basaltic rocks form a rugged highland. The bedrock is largely mantled by glacial deposits of Wisconsin age. On hills the glacial deposits are mainly ground moraine, and in valleys mainly stratified. The metamorphic rocks comprise the Hartland Formation, Bristol Granite Gneiss of Gregory (1906), and Prospect Gneiss. These formations contain water in fractures, principally joints occurring in regular sets. The rocks generally yield supplies of 5 to 15 gpm (gallons per minute) to drilled wells averaging about 140 feet in depth. \r\n\r\nThe rocks of Triassic age in the area are the New Haven Arkose, Talcott Basalt, Shuttle Meadow Formation, Holyoke Basalt, and East Berlin Formation. The formations contain water principally in joints and other fractures and, to a lesser extent, in bedding-plane openings and pore spaces. Drilled wells penetrating these rocks generally range from 100 to 200 feet in depth and yield an average of nearly 20 gpm. The maximum yield obtained from a well in these rocks is 180 gpm. \r\n\r\nThe ground moraine of Pleistocene age is composed principally of till. The deposit averages about 24 feet in thickness, and wells penetrating it average about 16 feet in depth. The ground moraine yields small supplier of water suitable for household use when tapped by shallow large-diameter wells. The stratified glacial deposits, which are as much as 300 feet thick, comprise ice-contact and proglacial deposits and deposits of generally obscure origin termed 'undifferentiated stratified deposits.' The ice-contact and undifferentiated stratified deposits, some of which underlie proglacial deposits, are coarse grained and contain gravel beds from which supplies of as much as 1,400 gpm can be obtained. The proglacial deposits are, on the whole, finer grained than the other stratified deposits, but in places they allow development of wells producing as much as 500 gpm. However, the stratified glacial deposits throughout much of the Bristol-Plainville-Southington area are fine grained and provide only small supplies.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1578","usgsCitation":"La Sala, A., 1964, Geology and ground-water resources of the Bristol-Plainville-Southington area, Connecticut: U.S. Geological Survey Water Supply Paper 1578, Report: iv, 70 p.; 3 Plates: 31.00 × 37.03 inches or smaller, https://doi.org/10.3133/wsp1578.","productDescription":"Report: iv, 70 p.; 3 Plates: 31.00 × 37.03 inches or smaller","costCenters":[],"links":[{"id":27619,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1578/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27618,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1578/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27617,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1578/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27616,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1578/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138433,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1578/report-thumb.jpg"},{"id":397416,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24764.htm"}],"scale":"24000","country":"United States","state":"Connecticut","city":"Bristol, Plainville, Southington","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -72.998,\n 41.546\n ],\n [\n -72.817,\n 41.546\n ],\n [\n -72.817,\n 41.723\n ],\n [\n -72.998,\n 41.723\n ],\n [\n -72.998,\n 41.546\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cee4b07f02db5458ec","contributors":{"authors":[{"text":"La Sala, A. M.","contributorId":103659,"corporation":false,"usgs":true,"family":"La Sala","given":"A. M.","affiliations":[],"preferred":false,"id":144625,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2099,"text":"wsp1669AA - 1964 - Ground-water resources of the lower Mesilla Valley, Texas and New Mexico","interactions":[],"lastModifiedDate":"2016-08-19T14:33:03","indexId":"wsp1669AA","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1669","chapter":"AA","title":"Ground-water resources of the lower Mesilla Valley, Texas and New Mexico","docAbstract":"The lower Mesilla Valley extends southward from the vicinity of Anthony, Tex., to the gorge of the Rio Grande north of El Paso and westward from the Franklin Mountains to the east edge of La Mesa. The increase in the use of ground water for the public water supply of El Paso and for supplemental irrigation, when the surface-water allotments were inadequate, emphasized the need for an investigation of the ground-water resources of the lower Mesilla Valley.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States, 1962","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1669AA","usgsCitation":"Leggat, E., Lowry, M., and Hood, J.W., 1964, Ground-water resources of the lower Mesilla Valley, Texas and New Mexico: U.S. Geological Survey Water Supply Paper 1669, Report: iv, 49 p.; 8 Plates, https://doi.org/10.3133/wsp1669AA.","productDescription":"Report: iv, 49 p.; 8 Plates","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":27666,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27667,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27668,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27669,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27672,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27673,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669aa/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27665,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27671,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138191,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669aa/report-thumb.jpg"},{"id":27670,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db696a4d","contributors":{"authors":[{"text":"Leggat, E. R.","contributorId":28222,"corporation":false,"usgs":true,"family":"Leggat","given":"E. R.","affiliations":[],"preferred":false,"id":144671,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lowry, M.E.","contributorId":55807,"corporation":false,"usgs":true,"family":"Lowry","given":"M.E.","email":"","affiliations":[],"preferred":false,"id":144672,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hood, J. W.","contributorId":87908,"corporation":false,"usgs":true,"family":"Hood","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":144673,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2114,"text":"wsp1619X - 1964 - Geology and ground-water resources of Rock County, Wisconsin","interactions":[],"lastModifiedDate":"2015-10-02T14:37:26","indexId":"wsp1619X","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1619","chapter":"X","title":"Geology and ground-water resources of Rock County, Wisconsin","docAbstract":"Rock County is in south-central Wisconsin adjacent to the Illinois State line. The county has an area of about 723 square miles and had a population of about 113,000 in 1957 ; it is one of the leading agricultural and industrial counties in the State. The total annual precipitation averages about 32 inches, and the mean annual temperature is about 48 ? F. Land-surface altitudes are generally between 800 and 00 feet, but range from 731 feet, where the Rock River flows into Illinois, to above 1,080 feet, at several places in the northwestern part of the county. The northern part of Rock County consists of the hills and kettles of a terminal moraine which slopes southward to a flat, undissected outwash plain. The southeastern part of the county is an area of gentle slopes, whereas the southwestern part consists of steep-sided valleys and ridges. Rock County is within the drainage basin of the Rock River, which flows southward through the center of the county. The western and southwestern parts of ,the county are drained by the Sugar River und Coon Creek, both of which flow into the Pecatonica River in Illinois and thence into the Rock River. The southeastern part of the county is drained by Turtle Creek, which also flows into Illinois before joining the Rock River. Nearly all the lakes and ponds are in the northern one-third of the county, the area of most recent glaciation. The aquifers in Rock County are of sedimentary origin and include deeply buried sandstones, shales, and dolomites of the Upper Cambrian series. This series overlies crystalline rocks of Precambrian age and supplies water to all the cities and villages in the county. The St. Peter sandstone of Ordovician age underlies all Rock County except where the formation has been removed by erosion in the Rock and Sugar River valleys, and perhaps in Coon Creek valley. The St. Peter sandstone is the principal source of water for domestic, stock, and small industrial wells in the western half of the county. This sandstone also yields some water to uncased wells that tap the deeper rocks of the Upper Cambrian series. East of the Rock River the Platteville, Decorah, and Galena formations undifferentiated, or Platteville-Galena unit, is the principal source of water for domestic and stock wells. Unconsolidated deposits of glacial origin cover most of Rock County and supply water to many small wells. In the outwash deposits along the Rock River, wells of extremely high capacity have been developed for industrial and municipal use. The most significant feature of the bedrock surface in Rock County is the ancestral Rock River valley, which has been filled with glacial outwash to a depth of at least 396 feet below the present land surface. East of the buried valley the bedrock has a fiat, relatively undissected surface. West of the valley the bedrock surface is rugged and greatly dissected. Ground water in Rock County occurs under both water-table and artesian conditions; however, because of the interconnection and close relation of all ground water in the county, the entire system is considered to be a single groundwater body whose surface may be represented by one piezometric map. Recharge occurs locally, throughout the county. Nearly all recharge is derived directly from precipitation that percolates downward to become a part of the groundwater body. Natural movement of water in the consolidated water-bearing units is generally toward the buried Rock and Sugar River valleys. Movement of water in the sandstones of Cambrian age was calculated to be about 44 million gallons a day toward the Rock River. Discharge from wells in Rock County in 1957 was about 23 million gallons a day. Nearly 90 percent of this water was drawn from the area along the Rock River. Drilled wells, most of which were drilled by the cable-tool method, range in diameter from 3 to 26 inches, and in depth from 46 to 1,225 feet. Driven wells in alluvium and glacial drift are usually 1? to 2? in
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Carolina\",\"nation\":\"USA \"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4dba","contributors":{"authors":[{"text":"Goddard, Grover Cleveland","contributorId":104031,"corporation":false,"usgs":true,"family":"Goddard","given":"Grover","email":"","middleInitial":"Cleveland","affiliations":[],"preferred":false,"id":143969,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2173,"text":"wsp1944 - 1964 - Quality of surface waters of the United States, 1962, Parts 7 and 8, Lower Mississippi River basin and western Gulf of Mexico basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:23","indexId":"wsp1944","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1944","title":"Quality of surface waters of the United States, 1962, Parts 7 and 8, Lower Mississippi River basin and western Gulf of Mexico basins","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1944","usgsCitation":"Love, S.K., 1964, Quality of surface waters of the United States, 1962, Parts 7 and 8, Lower Mississippi River basin and western Gulf of Mexico basins: U.S. Geological Survey Water Supply Paper 1944, xii, 645 p. :ill. ;25 cm., https://doi.org/10.3133/wsp1944.","productDescription":"xii, 645 p. :ill. ;25 cm.","costCenters":[],"links":[{"id":138311,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1944/report-thumb.jpg"},{"id":27784,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1944/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a8be4b07f02db651abe","contributors":{"authors":[{"text":"Love, S. K.","contributorId":27419,"corporation":false,"usgs":true,"family":"Love","given":"S.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":144768,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1154,"text":"wsp1779S - 1964 - Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada","interactions":[],"lastModifiedDate":"2012-02-02T00:05:12","indexId":"wsp1779S","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1779","chapter":"S","title":"Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada","docAbstract":"Practically all the ground water of economic importance in the Truckee Meadows area, an alluviated intermontane basin in western Nevada is in the valley fill, which consists of unconsolidated and partially consolidated sedimentary deposits. The Mesozoic and Cenozoic consolidated rocks of the mountains bordering the valley contain some water in fractures and other openings, but they have virtually no interstitial permeability. The permeability of the valley fill is extremely variable. The Truckee Formation, which is the oldest deposit of the valley fill, yields very little water to wells. Permeable lenses of sand and gravel in the valley fill that are younger than the Truckee Formation yield moderate to large amounts of water to wells. \r\n\r\nThe estimated average annual recharge to and discharge from the groundwater reservoir is 35,000 acre-feet. About 25,000 acre-feet of the recharge is from the infiltration of irrigation water diverted from the Truckee River. Most of the discharge is by evapotranspiration and by seepage to ditches and streams. \r\n\r\nSome water in the area is unsuitable for many uses because of its poor chemical quality. Water in the Steamboat Springs area is hot and has high concentrations of chloride and dissolved solids. Both water draining areas of bleached rock and ground water downgradient from areas of leached rock have high concentrations of sulfate and dissolved solids. Surface water of low dissolved-solids content mixes with and dilutes some highly mineralized ground water. \r\n\r\nIncreased pumping in discharge areas will help to alleviate waterlogged conditions and will decrease ground-water losses by evapotranspiration. Increased pumping near the Truckee River may induce recharge from the river to the ground-water system.","language":"ENGLISH","publisher":"U.S. Government Printing Office,","doi":"10.3133/wsp1779S","usgsCitation":"Cohen, P.M., and Loeltz, O.J., 1964, Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada: U.S. Geological Survey Water Supply Paper 1779, v, 63 p. :ill., maps ;23 cm., https://doi.org/10.3133/wsp1779S.","productDescription":"v, 63 p. :ill., maps ;23 cm.","costCenters":[],"links":[{"id":137311,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1779s/report-thumb.jpg"},{"id":25954,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779s/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25955,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779s/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25956,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779s/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25957,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1779s/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ae4b07f02db6250cd","contributors":{"authors":[{"text":"Cohen, Philip M.","contributorId":67860,"corporation":false,"usgs":true,"family":"Cohen","given":"Philip","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":143269,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Loeltz, Omar J.","contributorId":86312,"corporation":false,"usgs":true,"family":"Loeltz","given":"Omar","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":143270,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1156,"text":"wsp1754 - 1964 - Preliminary results of hydrogeologic investigations in the valley of the Humboldt River near Winnemucca, Nevada","interactions":[],"lastModifiedDate":"2021-11-17T19:59:07.216414","indexId":"wsp1754","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1754","title":"Preliminary results of hydrogeologic investigations in the valley of the Humboldt River near Winnemucca, Nevada","docAbstract":"Most of the ground water of economic importance and nearly all the ground water closely associated with the flow o# the Humboldt River in the. 40-mile reach near Winnemucca, Nev., are in unconsolidated sedimentary deposits. These deposits range in age from Pliocene to Recent and range in character from coarse poorly sorted fanglomerate to lacustrine strata of clay, silt, sand, and gravel. The most permeable deposit consists of sand and gravel of Lake Lahontan age--the so-called medial gravel unit--which is underlain and overlain by fairly impermeable silt and clay also of Lake Lahontan age. \r\n\r\nThe ultimate source of nearly all the water in the study area is precpitation within the drainage basin of the Humboldt River. Much of this water reaches the study, area as flow or underflow of the Humboldt River and as underflow from other valleys tributary to the study area. Little if any flow from the tributary streams in the study area usually reaches the Humboldt River. Most of the tributary streamflow within the study area evaporates or is transpired by vegetation, but a part percolates downward through unconsolidated deposits of the alluvial fans flanking the mountains and move downgradient as ground-water underflow toward the Humboldt River. \r\n\r\nAreas that contribute significant amounts of ground-water underflow to. the valley of the Humboldt River within the study area are (1) the valley of the Humboldt River upstream from the study area, (2) the Pole Creek-Rock Creek area, (3) Paradise Valley, and (4) Grass Valley and the northwestern slope of the Sonoma Range. The total average underflow from these areas in the period 1949-61 was about 14,000-19,000 acre-feet per year. Much of this underflow discharged into the Humboldt River within the study area and constituted a large part of the base flow of the river. \r\n\r\nStreamflow in the Humboldt River increases substantially in the early spring, principally because of runoff to the river in the reaches upstream from the study area. The resulting increase of the stage of the river causes the river to lose large amounts of water by infiltration to the ground-water reservoir in the study area. In addition, there is much recharge to the ground-water reservoir in the spring and early summer as a result of seepage losses from irrigation ditches and the downward percolation of some of the excess water applied for irrigation. The average net increase of ground water in storage in the deposits beneath and adjacent to the flood plain of the Humboldt River during the spring and early summer is about 10,000 acre-feet.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1754","usgsCitation":"Cohen, P.M., 1964, Preliminary results of hydrogeologic investigations in the valley of the Humboldt River near Winnemucca, Nevada: U.S. Geological Survey Water Supply Paper 1754, Report: v, 59 p.; 4 Plates: 40.00 × 27.85 inches or smaller, https://doi.org/10.3133/wsp1754.","productDescription":"Report: v, 59 p.; 4 Plates: 40.00 × 27.85 inches or smaller","costCenters":[],"links":[{"id":25962,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1754/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25960,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1754/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25963,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1754/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25959,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1754/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25961,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1754/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":391813,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24929.htm"},{"id":137313,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1754/report-thumb.jpg"}],"country":"United States","state":"Nevada","city":"Winnemucca","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118,\n 40.843\n ],\n [\n -117.278,\n 40.843\n ],\n [\n -117.278,\n 41.134\n ],\n [\n -118,\n 41.134\n ],\n [\n -118,\n 40.843\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4af5e4b07f02db6922a0","contributors":{"authors":[{"text":"Cohen, Philip M.","contributorId":67860,"corporation":false,"usgs":true,"family":"Cohen","given":"Philip","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":143274,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2186,"text":"wsp1747 - 1964 - Geology and hydrology of the West Milton area, Saratoga County, New York","interactions":[],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1747","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1747","title":"Geology and hydrology of the West Milton area, Saratoga County, New York","docAbstract":"This report describes the geology, ground-water conditions, streamflow characteristics, and quality of water in the West Milton area, Saratoga County, N.Y. The West Milton area is in the east-central part of New York in the hilly region that forms a transition zone between the Adirondack Mountains and the Hudson-Mohawk valley lowland. Bedrock underlying the area consists of crystalline rocks of Precambrian age and sandstone, dolomite, limestone, and shale formations of Cambrian and Ordovician age. The formations have been moderately folded and have been displaced as much as several hundred feet' along at least three northeast-trending normal faults. The bedrock is overlain in nearly all parts of the area by a layer of unconsolidated deposits which ranges in thickness from a few feet to more than 200 feet. The unconsolidated deposits are of Pleistocene age and consist of unstratified materials (till) laid down by glacial ice at stratified sediments deposited by glacial meltwaters. The topography of the bedrock surface differs greatly from the topography of the land surface. Although not evident in the present topography, at least two channels, cut in bedrock by preglacial streams, pass through the area. \r\n\r\nGround-water supplies adequate to satisfy domestic requirements can be obtained from wells in any part of the area. Large ground-water supplies may be taken from coarse-grained stratified deposits comprising two aquifers in the valley of Kayaderosseras Creek. The Atomic Energy Commission has pumped as much as 1 mgd from a horizontal well drawing from the uppermost aquifer which is composed of flood-plain deposits. Part of the water yielded by this well during extended periods of pumping is induced flow from the creek. Three nearby vertical wells drilled by the Commission comprise a separate well field capable of yielding at least 2 mgd and possibly as much as 3 mgd from the deeper stratified deposits underlying the valley. A pumping test showed that at near the center of this well field the coefficient of transmissibility is about 125,000 gpd per ft and the coefficient of storage is about 0.0003. The water obtained from the sand and gravel has a hardness of about 125 ppm and contains about 150 ppm of dissolved solids. \r\n\r\nMost of the Government reservation is drained by Glowegee Creek, one of the larger tributaries of Kayaderosseras Creek. The average streamflow of Kayaderosseras Creek at West Milton is 141 cfs or about 1.5 cfs per sq. mi. The monthly mean discharge has ranged from a low of 21.7 cfs in September 1958 to a high of 866 cfs in March 1936, and the annual mean discharge has ranged from 94.5 cfs in 1941 to 198 cfs in 1952. The mean annual flood is 1,740 cfs and the 50-year flood is 5,300 cfs. \r\n\r\nStreamflow data have been collected on Glowegee Creek since 1948 at a station 0.5 mile south of West Milton. The average streamflow of Glowegee Creek at this station is 41 cfs or about 1.5 cfs per sq mi. The mean annual flood is 740 cfs and the 50-year flood is 2,250 cfs. \r\n\r\nThe quality of the water in both Kayaderosseras Creek and Glowegee Creek is satisfactory for public supply and most industrial purposes. The mineral content of both streams is low--the dissolved-solids content averaging about 93 ppm in Kayaderosseras Creek and about 131 ppm in Glowegee Creek. The average hardness of water in Kayaderosseras Creek and Glowegee Creek is 68 ppm and 102 ppm, respectively. During periods of low flow, suspended sediment discharge in both streams is less than 10 tons per day, but during periods of high flow, the sediment discharge has been as great as 163 tons per day in Glowegee Creek and 437 tons per day in Kayaderosseras Creek.","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1747","usgsCitation":"Mack, F., Pauszek, F.H., and Crippen, J.R., 1964, Geology and hydrology of the West Milton area, Saratoga County, New York: U.S. Geological Survey Water Supply Paper 1747, viii, 110 p. :illus., maps, diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1747.","productDescription":"viii, 110 p. :illus., maps, diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":137741,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1747/report-thumb.jpg"},{"id":27816,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27817,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27818,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27819,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27820,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27821,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1747/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27815,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b4691","contributors":{"authors":[{"text":"Mack, Frederick K.","contributorId":95858,"corporation":false,"usgs":true,"family":"Mack","given":"Frederick K.","affiliations":[],"preferred":false,"id":144794,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pauszek, F. H.","contributorId":61399,"corporation":false,"usgs":true,"family":"Pauszek","given":"F.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144793,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Crippen, John R.","contributorId":13208,"corporation":false,"usgs":true,"family":"Crippen","given":"John","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":144792,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2203,"text":"wsp1764 - 1964 - Ground-water geology of the Dickson, Lawrenceburg, and Waverly areas in the western Highland Rim, Tennessee","interactions":[],"lastModifiedDate":"2024-01-31T20:36:24.280058","indexId":"wsp1764","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1764","title":"Ground-water geology of the Dickson, Lawrenceburg, and Waverly areas in the western Highland Rim, Tennessee","docAbstract":"Ground-water supplies in the Dickson, Lawrenceburg, and Waverly areas are obtained from wells and springs in limestone and chert formations of Missisippian age. In the Dickson area most of the wells and springs are in Warsaw Limestone. In the Lawrenceburg and Waverly areas, ground-water supplies are obtained from Fort Payne Chert and from residuum. In all three areas a few wells obtain small amounts of water from gravel stringers in the residuum. \r\n\r\nYields of well range from a few to 300 gpm (gallons per minute). Wells having the largest yields obtain water from residual material (colluvium) in the valley of Trace Creek in the Waverly area. Fewer than 10 percent of all wells inventoried yield more than 25 gpm. Springs are common in all the areas studied and yield as much as 1,000 gpm. \r\n\r\nThe quality of water from wells and springs iv the areas studied generally is good. The water is of the calcium bicarbonate type, and most of it is moderately hard to hard. The constituents in water from springs and from wells are about the same, although water from springs tends to be softer and slightly lower in dissolved-solids content. \r\n\r\nSprings constitute the largest potential source of water in the three areas. Twenty-one of the large springs discharge approximately 12 million gallons per day, or about 8,000 gpm. Another potential source of water is residuum underlying the valley of Trace Creek in the Waverly area. Wells yielding as much as 500 gpm probably could be developed in this aquifer.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1764","usgsCitation":"Marcher, M.V., Bingham, R.H., and Lounsbury, R., 1964, Ground-water geology of the Dickson, Lawrenceburg, and Waverly areas in the western Highland Rim, Tennessee: U.S. Geological Survey Water Supply Paper 1764, Report: iv, 50 p.; 7 Plates: 19.68 × 38.83 inches or smaller, https://doi.org/10.3133/wsp1764.","productDescription":"Report: iv, 50 p.; 7 Plates: 19.68 × 38.83 inches or smaller","costCenters":[],"links":[{"id":27871,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397419,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24942.htm","text":"Lawrenceburg area"},{"id":27866,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27867,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27868,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138156,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1764/report-thumb.jpg"},{"id":27865,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27869,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27870,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27872,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1764/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397418,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24941.htm","text":"Dickson area"},{"id":397420,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24943.htm","text":"Waverly area"}],"scale":"31680","country":"United States","state":"Tennessee","city":"Dickson, Lawrenceburg, Waverly","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.5,\n 36\n ],\n [\n -87.25,\n 36\n ],\n [\n -87.25,\n 36.125\n ],\n [\n -87.5,\n 36.125\n ],\n [\n -87.5,\n 36\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.375,\n 35.125\n ],\n [\n -87.25,\n 35.125\n ],\n [\n -87.25,\n 35.375\n ],\n [\n -87.375,\n 35.375\n ],\n [\n -87.375,\n 35.125\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.875,\n 36\n ],\n [\n -87.75,\n 36\n ],\n [\n -87.75,\n 36.125\n ],\n [\n -87.875,\n 36.125\n ],\n [\n -87.875,\n 36\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d966","contributors":{"authors":[{"text":"Marcher, Melvin V.","contributorId":11590,"corporation":false,"usgs":true,"family":"Marcher","given":"Melvin","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":144819,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bingham, Roy H.","contributorId":56632,"corporation":false,"usgs":true,"family":"Bingham","given":"Roy","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144820,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lounsbury, Richard Edwin","contributorId":102054,"corporation":false,"usgs":true,"family":"Lounsbury","given":"Richard Edwin","affiliations":[],"preferred":false,"id":144821,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2236,"text":"wsp1779X - 1964 - Quality of Delaware River water at Trenton, New Jersey","interactions":[],"lastModifiedDate":"2017-07-07T09:14:45","indexId":"wsp1779X","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1779","chapter":"X","title":"Quality of Delaware River water at Trenton, New Jersey","docAbstract":"Water in the Delaware River at Trenton, NJ, is a mixture of several types--water from the mountainous headwater region, water from the coal-mining regions, and water from the limestone valleys. The quantities of these types of water, in relation to the total quantity of water at Trenton, vary with changes in season and reservoir releases. \r\n\r\n The chemical quality of the water during the 17-year period 1945-61 was excellent, and the water was suitable for most uses after little or no treatment. The average concentration of dissolved solids was 86 ppm (parts per million), and 90 percent of the time it ranged from 57 to 126 ppm. Usually the pH of the water was close to 7.0 (considered to be a neutral point-neither acid nor alkaline). The hardness was less than 86 ppm 95 percent of the time. The general composition of the dissolved-solids content, in terms of equivalents, is 28 percent calcium, 14 percent magnesium, 8 percent sodium plus potassium, 43 percent bicarbonate plus sulfate, 5 percent chloride, and 2 percent nitrate. Concentrations of minerals in the river water are lowest during March, April and May (median concentration of dissolved solids 66 PPM) and are highest during August and September (median, 107 PPM). \r\n\r\n Each year an average of 880,000 tons of dissolved solids and 932,000 tons of suspended solids are carried past Trenton by the Delaware River. The greatest monthly loads of dissolved solids are in March and April, and the smallest are from July to October. Suspended-solids loads are greater when the streamflow is high but small the rest of the time. Concentration of suspended solids exceeds 100 PPM only 5 percent of the time.\r\n\r\n The headwaters in the Delaware River basin are the source of water of excellent quality. Much of this water is stored in reservoirs, and when released during August and September, it improves the quality of the water at Trenton. These releases to augment low flow have the effect of narrowing the range of concentrations of dissolved constituents. In 1952 and 1962, 6 and 19 percent, respectively, of the drainage area above Trenton was regulated by reservoirs. After proposed construction, 60 percent will be regulated by 1975. Thus, it may be that the high concentrations of dissolved constituents observed in the 1945-61 period will not occur again. \r\n\r\n It is possible that the water quality observed during the period 1945-61 (dissolved solids 57-126 PPM 90 percent of the time, pH close to 7.0, hardness less than 86 PPM 95 percent of the time) is representative of what can be expected in the future, for a variety of hydrologic conditions were experienced in the 17-year period.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1779X","usgsCitation":"McCarthy, L.T., and Keighton, W.B., 1964, Quality of Delaware River water at Trenton, New Jersey: U.S. Geological Survey Water Supply Paper 1779, iv, 51 p. :graphs, fold. map (in pocket) ;24 cm., https://doi.org/10.3133/wsp1779X.","productDescription":"iv, 51 p. :graphs, fold. map (in pocket) ;24 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":137764,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1779x/report-thumb.jpg"},{"id":27995,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779x/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27996,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1779x/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a8fe4b07f02db65515d","contributors":{"authors":[{"text":"McCarthy, Leo T. Jr.","contributorId":27029,"corporation":false,"usgs":true,"family":"McCarthy","given":"Leo","suffix":"Jr.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":144867,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Keighton, Walter B.","contributorId":81877,"corporation":false,"usgs":true,"family":"Keighton","given":"Walter","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":144868,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2237,"text":"wsp1613D - 1964 - Relation of salt-water encroachment to the major aquifer zones, Savannah area, Georgia and South Carolina","interactions":[],"lastModifiedDate":"2019-12-30T10:01:08","indexId":"wsp1613D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1613","chapter":"D","title":"Relation of salt-water encroachment to the major aquifer zones, Savannah area, Georgia and South Carolina","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1613D","usgsCitation":"McCollum, M., and Counts, H.B., 1964, Relation of salt-water encroachment to the major aquifer zones, Savannah area, Georgia and South Carolina: U.S. Geological Survey Water Supply Paper 1613, Report: iv, 26 p.; 4 Plates: 9.50 x 14.00 inches or smaller, https://doi.org/10.3133/wsp1613D.","productDescription":"Report: iv, 26 p.; 4 Plates: 9.50 x 14.00 inches or smaller","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":109995,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24805.htm","linkFileType":{"id":5,"text":"html"},"description":"24805"},{"id":137778,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1613d/report-thumb.jpg"},{"id":27999,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1613d/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28000,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1613d/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28001,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1613d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27997,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1613d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27998,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1613d/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Georgia, South Carolina","city":"Savannah","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.40869140625,\n 31.81689688674699\n ],\n [\n -80.67260742187499,\n 31.81689688674699\n ],\n [\n -80.67260742187499,\n 32.26855544621476\n ],\n [\n -81.40869140625,\n 32.26855544621476\n ],\n [\n -81.40869140625,\n 31.81689688674699\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67c286","contributors":{"authors":[{"text":"McCollum, M.J.","contributorId":40576,"corporation":false,"usgs":true,"family":"McCollum","given":"M.J.","email":"","affiliations":[],"preferred":false,"id":144870,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Counts, H. B.","contributorId":11201,"corporation":false,"usgs":true,"family":"Counts","given":"H.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":144869,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2253,"text":"wsp1777 - 1964 - Geology and ground-water resources of Washington County, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1777","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1777","title":"Geology and ground-water resources of Washington County, Colorado","docAbstract":"Washington County, in northeastern Colorado, has an area of 2,520 square miles. The eastern two-thirds of the county, part of the High Plains physiographic section, is relatively flat and has been moderately altered by the deposition of loess and dune sand, and by stream erosion. The western one-third is a part of the South Platte River basin and has been deeply dissected by tributary streams. The soils and climate of the county are generally suited for agriculture, which is the principal industry. \r\n\r\nThe rocks that crop out in the county influence the availability of ground water. The Pierre Shale, of Late Cretaceous age, underlies the entire area and ranges in thickness from 2,000 to 4,500 feet. This dense shale is a barrier to the downward movement of water and yields little or no water to wells. The Chadron Formation, of Oligocene age, overlies the Pierre Shale in the northern and central parts of the area. The thickness of the formation ranges from a few feet to about 300 feet. Small to moderate quantities of water are available from the scattered sand lenses and from the highly fractured zones of the siltstone. The Ogallala Formation, of Pliocene age, overlies the Chadron Formation and in Washington County forms the High Plains section of the Great Plains province. The thickness of the Ogallala Formation ranges from 0 to about 400 feet, and the yield from wells ranges from a few gallons per hour to about 1,500 gpm. Peorian loess, of Pleistocene age, and dune sand, of Pleistocene to Recent age, mantle a large pan of the county and range in thickness from a few inches to about 120 feet Although the loess and dune sand yield little water to wells, they absorb much of the precipitation and conduct the water to underlying formations. Alluvium, of Pleistocene and Recent age, occupies most of the major stream valleys in thicknesses of a few feet to about 250 feet. The yield of wells tapping the alluvium ranges from a few gallons per minute to about 3,000 gpm, according to the thickness of saturated material. \r\n\r\nDevelopment of ground water for irrigation has been generally restricted to the South Platte, Arikaree, and Beaver valleys. There were 134 irrigation wells, 3 industrial wells, and 10 municipal wells in the county in 1959. The annual ground-water pumpage from Washington County is estimated to be 18,000 acre-ft; about 10,000 acre-ft is from the High Plains ground-water province. Although some ground water enters the county as underflow, most of the recharge to ground-water reservoirs is from precipitation on the land surface. Recharge to the Ogallala Formation in the county is assumed to be approximately equal to the natural discharge from the county by underflow because ground-water withdrawals are from storage, and no other significant amount of natural discharge is apparent. Undertow in the Ogallala was calculated to be 83,000 acre-ft per year and the rate of recharge from precipitation to be about 0.95 inch per year. Neither recharge nor discharge was calculated for that part of the county in the South Platte River basin. \r\n\r\nAll ground water in Washington County has a high proportion of carbonate and is classed as hard to very hard. The sodium-adsorption-ratio for all samples analyzed was below the limit recommended for irrigation water. All the water from the Ogallala Formation and most of the water from the Chadron Formation is suitable for domestic use. Some water from the alluvial deposits overlying the Pierre Shale was exceptionally high in calcium, magnesium, and sodium sulfates. \r\n\r\nGround water has been heavily developed for irrigation in the South Platte valley and in some parts of the Beaver and Arikaree valleys. Some additional areas, however, could be developed in the latter two valleys. Large quantities of ground water in the Ogallala Formation are available for future development. The quantity of water in storage in the High Plains ground-water province in Washington County is about 6.5 million acre-f","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1777","usgsCitation":"McGovern, H.E., 1964, Geology and ground-water resources of Washington County, Colorado: U.S. Geological Survey Water Supply Paper 1777, iv, 46 p. :illus., maps (4 fold. 1 col., in pocket) ;24 cm., https://doi.org/10.3133/wsp1777.","productDescription":"iv, 46 p. :illus., maps (4 fold. 1 col., in pocket) ;24 cm.","costCenters":[],"links":[{"id":110015,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24953.htm","linkFileType":{"id":5,"text":"html"},"description":"24953"},{"id":137835,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1777/report-thumb.jpg"},{"id":28024,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28025,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28026,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28027,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28028,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1777/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db68580b","contributors":{"authors":[{"text":"McGovern, Harold E.","contributorId":9634,"corporation":false,"usgs":true,"family":"McGovern","given":"Harold","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":144901,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1669,"text":"wsp1779F - 1964 - Hydrologic studies of small watersheds, Honey Creek basin, Collin and Grayson Counties, Texas, 1953-1959","interactions":[],"lastModifiedDate":"2016-08-23T14:27:54","indexId":"wsp1779F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1779","chapter":"F","title":"Hydrologic studies of small watersheds, Honey Creek basin, Collin and Grayson Counties, Texas, 1953-1959","docAbstract":"This report presents the results of an investigation into the effects of floodwaterretarding structures in the 39 square miles of the Honey Creek basin above the stream-gaging station near McKinney, during the period October 1952 to September 1959. The number of such structures in the study area was increased from 2 to 12 during the investigation.
\nData were collected which permit computation of basin and watershed precipitation, inflow to and outflow from each floodwater-retarding structure, evaporation and seepage from each pool, and a continuous record of discharge from the entire study area. Transpiration was not evaluated, but in the water-budget summary it is included in the item \"pool consumption\", together with evaporation and seepage.
\nDuring the 7-year study period, the annual inflow to the gaged pools ranged from 1.34 to 26.50 inches and averaged 7.39 inches, of which 0.73 inch was direct rainfall on the pool surface. The annual pool consumption ranged only from 1.33 to 1.85 inches, and averaged 1.62 inches. These results indicate that in a year of substantial runoff the floodwater-retarding structures would have only a minor effect on downstream water yield, but in a year of low runoff the structures would have a marked effect on downstream water yield.
\nThe effect on the flood regimen at a downstream point because of floodwaterretarding structures in the headwaters will vary with the amount and intensity of the precipitation and with antecedent conditions. The beneficial effects of the structures on Honey Creek during the floods of April and May 1957 is illustrative. During the period April 19 to May 31, 1957, the total volume of inflow to the floodwater-retarding structures was equivalent to 4.3 times the combined capacities of the pools from an average basin rainfall of 30.31 inches. The retarding effects of the structures limited the flooding on Honey Creek at the gage to minor flooding on only five occasions during that period.
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1964 - Ground water in the Sirte area, Tripolitania, United Kingdom of Libya","interactions":[],"lastModifiedDate":"2012-02-02T00:05:35","indexId":"wsp1757C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1757","chapter":"C","title":"Ground water in the Sirte area, Tripolitania, United Kingdom of Libya","docAbstract":"The present study of the ground-water conditions in the Sirte area was made during December 1961 and March-April 1962 at the request of officials of the Government of Libya. Particular attention was given to the potential of the fresh-water aquifer near Qasr Bu Itadi as a source of water for Sirte. \r\n\r\nThe Sirte area lies on the southern coast of the Mediterranean Sea about 450 kilometers east-southeast of Tripoli, cocapital of Libya. Although the area receives some winter precipitation, the climate is arid. The surface rocks of the area are chiefly Miocene limestone containing marl, clay, and some sandstone, though Quaternary deposits occur along the wadis and mantle the Miocene rocks in the coastal plain. \r\n\r\nFresh ground water occurs locally in Recent sand dunes near Zaafran and in Miocene limestone near Qasr Bu Hadi, south of a probable fault. Elsewhere in the Sirte area, ground water occurs generally in Tertiary rocks but contains 3,000 or more parts per million of dissolved solids. \r\n\r\nTo establish the hydraulic characteristics of the fresh-water aquifer in the Qasr Bu Itadi area, two test wells were drilled and a controlled pumping test was made. The coefficient of transmissibility was found to be about 25,000 gallons per day per foot (13.68 cubic meters per hour per meter), and the coefficient of storage, about 0.00055. The pumping test also established the presence of two barrier-type hydraulic boundaries for the aquifer, one about 250 meters westward and another about 535 meters northward from well 9a. The first boundary is probably the small anticline on which stands the fort of Qasr Bu Itadi; the second boundary is probably a northwest trending fault. Using the transmissibility and storage coefficients derived from the pumping test, the writer concludes that (1) the total draft from the fresh-water aquifer should not exceed 13.5 cubic meters per hour and (2) production wells should be at least 3 kilometers south of well 9a.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1757C","usgsCitation":"Ogilbee, W., 1964, Ground water in the Sirte area, Tripolitania, United Kingdom of Libya: U.S. Geological Survey Water Supply Paper 1757, iii, 14 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1757C.","productDescription":"iii, 14 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":139075,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1757c/report-thumb.jpg"},{"id":28414,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1757c/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66d914","contributors":{"authors":[{"text":"Ogilbee, William","contributorId":106093,"corporation":false,"usgs":true,"family":"Ogilbee","given":"William","email":"","affiliations":[],"preferred":false,"id":145160,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2421,"text":"wsp1499F - 1964 - Water resources of the Baltimore area, Maryland","interactions":[],"lastModifiedDate":"2012-02-02T00:05:34","indexId":"wsp1499F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1499","chapter":"F","title":"Water resources of the Baltimore area, Maryland","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1499F","usgsCitation":"Otton, E., Martin, R., and Durum, W.H., 1964, Water resources of the Baltimore area, Maryland: U.S. Geological Survey Water Supply Paper 1499, vi, 105 p., https://doi.org/10.3133/wsp1499F.","productDescription":"vi, 105 p.","costCenters":[],"links":[{"id":138941,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499f/report-thumb.jpg"},{"id":28430,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499f/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28431,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499f/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28432,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499f/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28433,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f4e4b07f02db5f064f","contributors":{"authors":[{"text":"Otton, E. G.","contributorId":22311,"corporation":false,"usgs":true,"family":"Otton","given":"E. G.","affiliations":[],"preferred":false,"id":145171,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Martin, R.O.R.","contributorId":40193,"corporation":false,"usgs":true,"family":"Martin","given":"R.O.R.","email":"","affiliations":[],"preferred":false,"id":145172,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Durum, W. H.","contributorId":78311,"corporation":false,"usgs":true,"family":"Durum","given":"W.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":145173,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}