Waupaca County is in east-central Wisconsin. No serious ground-water problems existed in 1960 except in a few localities where crystalline rock is near land surface or is covered by nearly impermeable till. The use of ground water for irrigation has not appreciably affected ground-water levels.
\nThe county is covered by Pleistocene till, glaciolacustrine (lake), glaciofluvial (stream), and eolian (wind) deposits. In the northern three-quarters of the county these deposits overlie Precambrian crystalline rocks; in the remainder, they overlie sandstone of Cambrian age and, to a minor extent, dolomite of the Prairie du Chien Group of Ordovician age. The deposits of Pleistocene age, particularly outwash, are the principal sources of ground water except in those areas where the saturated thickness is slight or the permeability low. The sandstone of Cambrian age is an important aquifer in the southeastern part of the county. The crystalline rocks of Precambrian age yield little water except from fractures, joints, and weathered zones, and they are a source of water only in areas where better aquifers are absent.
\nGround water in Waupaca County occurs under both water-table and artesian conditions. The source of this ground water is precipitation that falls on the county and percolates downward to the zone of saturation. Regional movement of ground water is to the Wolf River. In most of the county the direction of movement is eastward or southeastward, except in the southeastern corner of the county, where the movement is westward.
\nWater-level fluctuations reflect the variations of ground-water storage or artesian pressure in response to variations in recharge and discharge. Declining water levels from 1956 to 1959 reflect a period of below-normal precipitation, and rising water levels in late 1959 and 1960 reflect above-normal precipitation. Average precipitation, runoff, and evapotranspiration in 1959 are estimated to be 1,000, 400, and 600 mgd (million gallons per day) respectively. Pumpage in the county was estimated to be about 4 mgd in 1959, and about half of this amount was used for public supplies.
\nA pumping test of a well in outwash deposits near Waupaca indicated that at that point the coefficient of transmissibility is about 100,000 gpd (gallons per day) per ft, the permeability is about 1,000 gpd per sq ft, the coefficient of storage is about 0.2, and the specific capacity is 41 gpm (gallons per minute) per ft of drawdown. These hydraulic characteristics are probably in the same order of magnitude as the characteristics of outwash deposits in the county in general.
\nThe water from wells in Waupaca County, although hard and generally containing iron, is good for most purposes.
","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. Geological Survey","doi":"10.3133/wsp1669U","collaboration":"Prepared in cooperation with the Wisconsin Geological and Natural History Survey, University of Wisconsin","usgsCitation":"Berkstresser, C., 1964, Ground-water resources of Waupaca County, Wisconsin: U.S. Geological Survey Water Supply Paper 1669, Report: iv, 38 p.; 7 Plates: 32.00 x 34.06 inches or smaller, https://doi.org/10.3133/wsp1669U.","productDescription":"Report: iv, 38 p.; 7 Plates: 32.00 x 34.06 inches or smaller","numberOfPages":"42","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":137935,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669u/report-thumb.jpg"},{"id":25641,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25642,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25643,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25644,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25645,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25646,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25647,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25648,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669u/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","county":"Waupaca County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-88.6062,44.5903],[-88.6152,44.5903],[-88.7371,44.5906],[-88.7368,44.5021],[-88.7365,44.4164],[-88.7381,44.3307],[-88.7397,44.2432],[-88.7658,44.2434],[-88.8609,44.2425],[-88.8871,44.2426],[-88.9821,44.243],[-89.007,44.2426],[-89.104,44.243],[-89.1288,44.243],[-89.2245,44.2433],[-89.2242,44.3308],[-89.2238,44.4174],[-89.2235,44.504],[-89.2231,44.5916],[-89.2234,44.6814],[-88.982,44.6798],[-88.8587,44.6797],[-88.7367,44.6791],[-88.6051,44.6783],[-88.6062,44.5903]]]},\"properties\":{\"name\":\"Waupaca\",\"state\":\"WI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d523","contributors":{"authors":[{"text":"Berkstresser, Charles F.","contributorId":33697,"corporation":false,"usgs":true,"family":"Berkstresser","given":"Charles F.","affiliations":[],"preferred":false,"id":143042,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2780,"text":"wsp1657 - 1964 - Hydrogeology of northwestern Nassau and northeastern Queens Counties, Long Island, New York","interactions":[],"lastModifiedDate":"2012-02-02T00:05:28","indexId":"wsp1657","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":"1657","title":"Hydrogeology of northwestern Nassau and northeastern Queens Counties, Long Island, New York","docAbstract":"A detailed investigation of the geology and ground-water occurrence in northwestern Nassau and northeastern Queens Counties, N.Y., has been completed by the U.S. Geological Survey, in cooperation with the Nassau County Department of Public Works and the New York State Water Resources Commission. The area, about 63 square miles, includes the peninsulas of Great Neck and Manhasset Neck and the western part of Nassau County as far south as Garden City. Unconsolidated sediments of Pleistocene and Cretaceous aged 200 to 800 feet thick, constitute the ground-water reservoir of the area. The reservoir includes three discrete aquifers, not all found in the same locality, which transect geologic boundaries. The shallow unconfined aquifer consists of those permeable Pleistocene and Cretaceous deposits that lie within the upper part of the zone of saturation, which extends from slightly below sea level to more than 110 feet above sea level. It is an abundant source of water in much of the area, particularly in the southern part, where the aquifer consists of coarse sand and gravel in a glacial-outwash plain. The intermediate or principal aquifer consists largely of that part of the Magothy(?) formation that occurs from about 50 feet below sea level downward to the top of the clay member of the Raritan formation. Locally, however, the aquifer includes Pleistocene deposits which blanket the Magothy(?) formation or lie in channels cut into it. Although the principal aquifer has limited extent to the north, it is the chief source of water in most of the area, except the peninsulas. The lower or deep confined aquifer is found beneath the entire project area, and consists of the Lloyd sand member of the Raritan formation and the hydraulically contiguous Jameco gravel. The lower limit of the aquifer is the bedrock surface; its upper limit is defined by the overlying clay member of the Raritan formation and the Gardiners clay, the latter abutting against the clay member on the north or, in some valleys and embankments, lying directly upon the clay member. Thus, hydraulic continuity exists between the Lloyd sand member of the Raritan formation (Cretaceous) and the Jameco gravel (Pleistocene) in the northern part of Manhasset and Great Necks. The two contiguous clay bodies overlying the aquifer, the clay member of the Raritan formation and the Gardiners clay, form an effective confining bed which probably extends beyond the shore lines of the project area. The deep confined aquifer is particularly important on Manhasset and Great Necks where locally it is the only source of water available for large public-supply or industrial needs. In general, ground-water supplies in sufficient quantity and of excellent quality can be obtained from the three aquifers underlying northwestern Nassau and northeastern Queens Counties, N.Y. Ground-water withdrawals for public supply have increased with population growth and expanded use from an average of about 10 millions of gallons per day in 1940 to 30 mgd in 1957. In addition, about 10 mgd are pumped for various industrial, institutional and private uses. Much of the water pumped by industry is returned to the ground by diffusion wells and recharge basins. However, an increasing amount of water is lost from the ground-water reservoir due to the expanding network of server systems discharging directly to the sea. \r\n\r\nIn the Manhasset Neck and Great Neck areas, ground-water resources are approaching full development in terms of the total available supply, if such development has not been reached already (1959). The chief limiting factor to further expansion lies in the geometry of the aquifers and the reduced thickness of permeable saturated sediments. In the northern part of both peninsulas, the ground-water reservoir is only about 200 to 400 feet thick, and, locally, as much as 75 percent of the strata in the reservoir consists of rather impermeable silt and clay of the Raritan formation or the Gardiners clay. I","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1657","usgsCitation":"Swarzenski, W.V., 1964, Hydrogeology of northwestern Nassau and northeastern Queens Counties, Long Island, New York: U.S. Geological Survey Water Supply Paper 1657, v, 90 p. :ill., maps ;24 cm. +, https://doi.org/10.3133/wsp1657.","productDescription":"v, 90 p. :ill., maps ;24 cm. +","costCenters":[],"links":[{"id":110002,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24849.htm","linkFileType":{"id":5,"text":"html"},"description":"24849"},{"id":138745,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1657/report-thumb.jpg"},{"id":29236,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29237,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29238,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29239,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29240,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29241,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29242,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29243,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29244,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29245,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29246,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29247,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29248,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1657/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29249,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1657/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a49e4b07f02db624617","contributors":{"authors":[{"text":"Swarzenski, Wolfgang V.","contributorId":30213,"corporation":false,"usgs":true,"family":"Swarzenski","given":"Wolfgang","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":145775,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1041,"text":"wsp1687 - 1964 - Magnitude and frequency of floods in the United States, part 12. Pacific Slope basins in Washington and Upper Columbia River basin","interactions":[{"subject":{"id":52070,"text":"ofr6014 - 1960 - Floods in Washington, magnitude and frequency","indexId":"ofr6014","publicationYear":"1960","noYear":false,"title":"Floods in Washington, magnitude and frequency"},"predicate":"SUPERSEDED_BY","object":{"id":1041,"text":"wsp1687 - 1964 - Magnitude and frequency of floods in the United States, part 12. Pacific Slope basins in Washington and Upper Columbia River basin","indexId":"wsp1687","publicationYear":"1964","noYear":false,"title":"Magnitude and frequency of floods in the United States, part 12. Pacific Slope basins in Washington and Upper Columbia River basin"},"id":1}],"lastModifiedDate":"2022-02-04T19:39:50.958645","indexId":"wsp1687","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":"1687","title":"Magnitude and frequency of floods in the United States, part 12. Pacific Slope basins in Washington and Upper Columbia River basin","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1687","usgsCitation":"Bodhaine, G., and Thomas, D.M., 1964, Magnitude and frequency of floods in the United States, part 12. Pacific Slope basins in Washington and Upper Columbia River basin: U.S. Geological Survey Water Supply Paper 1687, Report: xiii, 337 p.; 5 Plates: 39.50 × 23.46 inches or smaller, https://doi.org/10.3133/wsp1687.","productDescription":"Report: xiii, 337 p.; 5 Plates: 39.50 × 23.46 inches or smaller","costCenters":[],"links":[{"id":138006,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1687/report-thumb.jpg"},{"id":25687,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1687/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25692,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1687/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":395463,"rank":8,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24896.htm"},{"id":25691,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1687/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25690,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1687/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25689,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1687/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25688,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1687/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho, Montana, Washington","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124.8,\n 46\n ],\n [\n -112.5,\n 46\n ],\n [\n -112.5,\n 49.5\n ],\n [\n -124.8,\n 49.5\n ],\n [\n -124.8,\n 46\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6495c5","contributors":{"authors":[{"text":"Bodhaine, G. L.","contributorId":26671,"corporation":false,"usgs":true,"family":"Bodhaine","given":"G. L.","affiliations":[],"preferred":false,"id":143078,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Thomas, D. M.","contributorId":8827,"corporation":false,"usgs":true,"family":"Thomas","given":"D.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":143077,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1042,"text":"wsp1779N - 1964 - Geology and ground-water resources in eastern Cheyenne and Kiowa Counties, Colorado","interactions":[],"lastModifiedDate":"2022-12-30T21:06:03.016628","indexId":"wsp1779N","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":"N","title":"Geology and ground-water resources in eastern Cheyenne and Kiowa Counties, Colorado","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1779N","usgsCitation":"Boettcher, A.J., and Horr, C.A., 1964, Geology and ground-water resources in eastern Cheyenne and Kiowa Counties, Colorado: U.S. Geological Survey Water Supply Paper 1779, Report: iv, 32 p.; 3 Plates: 17.00 x 35.70 inches or smaller, https://doi.org/10.3133/wsp1779N.","productDescription":"Report: iv, 32 p.; 3 Plates: 17.00 x 35.70 inches or smaller","costCenters":[],"links":[{"id":110016,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24963.htm","linkFileType":{"id":5,"text":"html"},"description":"24963"},{"id":25695,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779n/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25694,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779n/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25696,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1779n/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25693,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779n/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138007,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1779n/report-thumb.jpg"}],"country":"United States","state":"Colorado","county":"Cheyenne County, Kiowa County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -103.164,\n 39.042\n ],\n [\n -103.164,\n 38.265\n ],\n [\n -102.044,\n 38.265\n ],\n [\n -102.044,\n 39.042\n ],\n [\n -103.164,\n 39.042\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a61e4b07f02db635b3e","contributors":{"authors":[{"text":"Boettcher, Arnold J.","contributorId":93025,"corporation":false,"usgs":true,"family":"Boettcher","given":"Arnold","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":143080,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Horr, C. Albert","contributorId":43333,"corporation":false,"usgs":true,"family":"Horr","given":"C.","email":"","middleInitial":"Albert","affiliations":[],"preferred":false,"id":143079,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2796,"text":"wsp1608D - 1964 - Artesian water in the Malabar coastal plain of southern Kerala, India","interactions":[],"lastModifiedDate":"2012-02-02T00:05:28","indexId":"wsp1608D","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":"1608","chapter":"D","title":"Artesian water in the Malabar coastal plain of southern Kerala, India","docAbstract":"The present report is based on a geological and hydrological reconnaissance during 1954 of the Malabar Coastal Plain and adjacent island area of southern Kerala to evaluate the availability of ground water for coastal villages and municipalities and associated industries and the potentialities for future development. The work was done in cooperation with the Geological Survey of India and under the auspices of the U.S. Technical Cooperation Mission to India. The State of Kerala, which lies near the southern tip of India and along the eastern shore of the Caspian Sea, contains a total area of 14,937 square miles. The eastern part of the state is s rugged mountainous highland which attains \r\naltitudes of more than 6,000 feet. This highland descends westward through piedmont upland to s narrow coastal plain, which reaches a maximum width of about 16 miles in the latitude of Shertalli. A tropical monsoon rain-forest climate prevails in most of Kerala, and annual rainfall ranges from 65 to 130 inches in the southern part of the coastal plain to as much a 200 inches in the highland. \r\n\r\nThe highland and piedmont upland tracts of Kerala are underlain by Precambrian meamorphic and igneous rocks belonging in large parabola-the so-called Charnockite Series. Beneath ahe coastal plain are semiconsolidated asunconsolidated sedimentary deposits whose age ranges from Miocene to Recent. These deposits include sofa sandstone and clay shale containing some marl or limestone and sand, and clay and pea containing some gravel. The sofa sandstone, sand, and gravel beds constitute important aquifers a depths ranging from a few tens of feet to 400 feet or more below the land surface. The shallow ground war is under water-able or unconfined conditions, but the deeper aquifers contain water under artesian pressure. Near the coast, drilled wells tapping the deeper aquifers commonly flow with artesian heads as much as 10 to 12 feet above the land surface. \r\n\r\nThe draft from existing wells in the coastal belt between Quilon and Alleppy was estimated at 1 to 1 1/2 million imperial gallons a day. However, favorable conations exist for considerable further ground-water development in the coastal plain provided that sufficient attention is given to the potential hazards of saltwater encroachment and local overdevelopment. It is estimated that the overall potential for development of water from wells is probably at least several tens of millions of gallons a day, and perhaps more, in the Malabar Coastal Plain of southern Kera. Such a draft would have to be well dispersed to avoid overdevelopment and salt-war encroachment.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1608D","usgsCitation":"Taylor, G., and Ghosh, P., 1964, Artesian water in the Malabar coastal plain of southern Kerala, India: U.S. Geological Survey Water Supply Paper 1608, iii, 14 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1608D.","productDescription":"iii, 14 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138615,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1608d/report-thumb.jpg"},{"id":29292,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29293,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608d/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29294,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1608d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abbe4b07f02db672c6d","contributors":{"authors":[{"text":"Taylor, George C.","contributorId":45693,"corporation":false,"usgs":true,"family":"Taylor","given":"George C.","affiliations":[],"preferred":false,"id":145806,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ghosh, P.K.","contributorId":53771,"corporation":false,"usgs":true,"family":"Ghosh","given":"P.K.","email":"","affiliations":[],"preferred":false,"id":145807,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2797,"text":"wsp1608B - 1964 - Ground water in folded Cretaceous sandstone of the Bhachau area, Kutch, India, with reference to the Kandla Port water supply","interactions":[],"lastModifiedDate":"2012-02-02T00:05:28","indexId":"wsp1608B","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":"1608","chapter":"B","title":"Ground water in folded Cretaceous sandstone of the Bhachau area, Kutch, India, with reference to the Kandla Port water supply","docAbstract":"This report is based on an investigation of the availability of ground-water supplies in the Bhachau area for the nearby Kandla Port and township development undertaken by the Government of India. This seaport lies on an estuary of the Gulf of Kutch in western India and in the eastern part of the State of Kutch. The fieldwork on the investigation was carried on from November 1952 through April 1953 with continuing hydrologic observations through 1954-55. The fieldwork included: geologic mapping and delimitation of the principal aquifers of the region; preparation of water-table maps; a detailed inventory of existing wells and springs; observations of significant water table fluctuations; preparation of isobicarb, isochlor and isosulf maps to show the areal distribution of ground-water salinity. \r\n\r\nThe Bhachau area includes about 116 square miles in eastern Kutch and lies in a belt of semiarid low-latitude steppes. The mean annual rainfall is about 15 inches, most of which falls from late June to late September during the southwest monsoon. The area includes a central sandy upland ranging from about 100 to 250 feet above sea level ; a northern lowland of between about 50 to 125 feet altitude that slopes north to the Great Rann of Kutch; a belt of low buttes and discontinuous ridges ranging from about 200 to 275 feet above sea level; and southern lowland which slopes in a southerly to southeasterly direction from an altitude of about 125 feet to 25 feet or less near the Gulf of Kutch. The principal streams are Kageshwar Vokra and Kara Vokra which drain north to the Great Rann and Kotwala Vokra and Dalwala Vokra which drain south toward the Gulf of Kutch. \r\n\r\nThe rocks of the Bhachau area include nonmarine and marine sediments of Mesozoic, Tertiary, and Quaternary age and volcanic rocks of late Mesozoic to early Tertiary age. The oldest rocks in the area are medium- to coarse-grained white to buff current-bedded friable sandstone with occasional partings of white silty shale of the Upper Bhuj series that has been assigned to the Early Cretaceous. The soft friable sandstone of the Upper Bhuj series constitutes the most productive ground-water reservoir in the Bhachau area. At present (1955) there are nine irrigated tracts for which water is obtained from dug wells less than 90 feet deep in the Upper Bhuj. These wells are worked by bullocks and 'motes' (leather bags) at withdrawal rates ranging from about 6,000 to 24,000imperial gallons per day; however, many existing individual wells if equipped with mechanical pumps are capable of yielding 100,000 gallons per day. The Deccan trap of Late Cretaceous to Eocene age occurs in a sequence of basaltic lava flows in the Bhachau area, but trap dikes, sills and plugs that are common in other parts of Kutch have not been observed in the area. Laterite of probable Eocene age is extensive at the top of the Deccan trap, and in places where the lava flows are thin the parent rock has been almost completely lateritized. The Deccan lava flows or the laterite, where the trap is absent, rest disconformably on the Upper Bhuj. No wells have been observed in the Deccan trap of the Bhachau area, but it is possible that locally small supplies of good water may be obtained from these rocks. \r\n\r\nThe Tertiary sediments, which are assigned to the Manchhar series of Pliocene age, generally rest on the laterite or the Deccan trap ; but where both are absent, the Manchhar rests directly on the Upper Bhuj. The Manchhar series includes massive reddish-brown gypseous clay shales, laminated gray siltstones, some limestone, mottled sandstone, and laterite trap gravel. Only meager supplies of brackish water are obtained from wells in these sediments. \r\n\r\nAlong the channels of Kotwala, Dalwala, Kageshwar, and Kara Vokras are narrow bands of unconsolidated coarse sand with fine gravel of Quaternary age. No wells were observed in these deposits, but it is possible that locally they may contain small supplies of bracki","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1608B","usgsCitation":"Taylor, G., Osa, H., Mitra, A., and Sen, B., 1964, Ground water in folded Cretaceous sandstone of the Bhachau area, Kutch, India, with reference to the Kandla Port water supply: U.S. Geological Survey Water Supply Paper 1608, iv, 31 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1608B.","productDescription":"iv, 31 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138616,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1608b/report-thumb.jpg"},{"id":29295,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29296,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29297,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608b/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29298,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608b/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29299,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1608b/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66da12","contributors":{"authors":[{"text":"Taylor, George C.","contributorId":45693,"corporation":false,"usgs":true,"family":"Taylor","given":"George C.","affiliations":[],"preferred":false,"id":145810,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Osa, H.M.","contributorId":15594,"corporation":false,"usgs":true,"family":"Osa","given":"H.M.","email":"","affiliations":[],"preferred":false,"id":145809,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mitra, A.","contributorId":97077,"corporation":false,"usgs":true,"family":"Mitra","given":"A.","email":"","affiliations":[],"preferred":false,"id":145811,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Sen, B.N.","contributorId":8079,"corporation":false,"usgs":true,"family":"Sen","given":"B.N.","email":"","affiliations":[],"preferred":false,"id":145808,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1054,"text":"wsp1695 - 1964 - Geology and ground-water resources of southeastern New Hampshire","interactions":[{"subject":{"id":51806,"text":"ofr5516 - 1955 - Preliminary report on the investigation of ground-water resources of the seacoast region of New Hampshire","indexId":"ofr5516","publicationYear":"1955","noYear":false,"title":"Preliminary report on the investigation of ground-water resources of the seacoast region of New Hampshire"},"predicate":"SUPERSEDED_BY","object":{"id":1054,"text":"wsp1695 - 1964 - Geology and ground-water resources of southeastern New Hampshire","indexId":"wsp1695","publicationYear":"1964","noYear":false,"title":"Geology and ground-water resources of southeastern New Hampshire"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1695","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":"1695","title":"Geology and ground-water resources of southeastern New Hampshire","docAbstract":"The continued growth and development of southeastern New Hampshire, an area of about 390 square miles adjacent to the Atlantic Ocean, will depend partly on effectively satisfying the demand for water, which has increased rapidly since World War II. \r\n\r\nThe report identifies and describes the principal geologic units with respect to the occurrence of ground water. These units include bedrock and the various unconsolidated deposits that mantle the bedrock surface discontinuously throughout the area. \r\n\r\nThe bedrock formations, consisting of igneous and metamorphic rocks, chiefly of Paleozoic age, form a single water-bearing unit. Ground water is in joints and fractures. The fractures are small and scattered and therefore impart only a low permeability to the rocks. Wells in the bedrock commonly produce small but reliable supplies of ground water at depths of less than 150 feet. The yields of about 80 wells inventoried for this report ranged from 1? to 100 gpm (gallons per minute) and the median was 912 gpm. Depths ranged from 45 to 600 feet. The unconsolidated deposits consist of glacial drift of Pleistocene age; swamp deposits, alluvium, and beach deposits of Recent age; and eolian deposits of Pleistocene -and Recent age. For this report the glacial drift is divided into till, ice-contact deposits, marine deposits, and outwash and shore deposits. Glacial till forms a discontinuous blanket, commonly less than 15 but in some hills (drumlins) as much as about 200 feet thick. It has a low permeability but, because of its widespread outcrop area, it has been utilized as a source of water for numerous domestic supplies. Because most wells in till are shallow, many fail to meet modern demands during dry summers. \r\n\r\nIce-contact deposits locally form kames, kame terraces, kame plains, and ice-channel fillings throughout the area. They overlie bedrock and till and range in thickness from less than 1 foot to as much as 190 feet. In general, the ice-contact deposits are coarse textured and permeable, but variations in- the physical and hydrologic properties of a single deposit and from deposit to deposit are common. Ice-contact deposits are the source of the larger ground-water supplies in southeastern New Hampshire. \r\n\r\nMarine deposits underlie lowlands and valleys to a distance of about 20 miles inland from the present coastline. They commonly overlie bedrock and till and at places overlie or are interbedded with ice-contact deposits. Marine deposits range in thickness from less than 1 foot to possibly 75 feet. They are fine textured and impermeable; they do not yield water to wells in southeastern New Hampshire but generally act as a barrier to ground-water movement. Outwash and shore deposits form broad sand plains or gently sloping terraces of small extent. At most places the outwash and shore deposits, which range in thickness from less than 1 foot to about 50 feet, overlie marine deposits, but at some places they overlie bedrock, till, or ice-contact deposits. The outwash and shore deposits are fine textured and moderately permeable. They commonly yield enough ground water to meet the needs of farms, homes, and small industries. Alluvium underlies the flood plains and channels of the principal streams and overlies bedrock and older unconsolidated deposits wherever streams cross the older units. The alluvium generally is not tapped by wells. \r\n\r\nBeach deposits occupy areas along the Atlantic Ocean between promontories of bedrock or till. In general beach deposits are permeable and are a source of water supplies for domestic use. Yields of wells are limited, however, by the danger of drawing in salty water. \r\n\r\nRecharge in southeastern New Hampshire is derived principally from precipitation on outcrop areas of ice-contact deposits and outwash and shore deposits during the nongrowing season. Ground water is discharged naturally by springs, by effluent seepage to streams and other bodies of surface water, and by evapotranspiration. It ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1695","usgsCitation":"Bradley, E., 1964, Geology and ground-water resources of southeastern New Hampshire: U.S. Geological Survey Water Supply Paper 1695, v, 80 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1695.","productDescription":"v, 80 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":25720,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25721,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25722,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25723,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25724,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25725,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25726,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25727,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1695/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137945,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1695/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685601","contributors":{"authors":[{"text":"Bradley, Edward","contributorId":67071,"corporation":false,"usgs":true,"family":"Bradley","given":"Edward","email":"","affiliations":[],"preferred":false,"id":143098,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2043,"text":"wsp1669J - 1964 - Ground-water conditions in the Green Bay area, Wisconsin, 1950-60","interactions":[],"lastModifiedDate":"2015-10-02T13:57:06","indexId":"wsp1669J","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":"J","title":"Ground-water conditions in the Green Bay area, Wisconsin, 1950-60","docAbstract":"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":2905,"text":"wsp1584 - 1964 - Geology and ground-water resources of Uvalde County, Texas","interactions":[],"lastModifiedDate":"2016-08-22T10:54:28","indexId":"wsp1584","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":"1584","title":"Geology and ground-water resources of Uvalde County, Texas","docAbstract":"The principal aquifer in Uvalde County is the Edwards and associated limestones of Cretaceous age. The aquifer underlies an extensive area in south-central Texas extending along the Balcones fault zone from Kinney County eastward to San Antonio, and thence northeastward to Hays County. The hydrologic unit making up the Edwards and associated limestones consists of the Comanche Peak limestone, the Edwards limestone, the Kiamichi formation, and the Georgetown limestone. Other less important aquifers in Uvalde County include the Glen Rose limestone, the Buda limestone, the Austin chalk, and the Leona formation.
\n\n
Uvalde County occupies parts of two physiographic provinces, the Edwards Plateau on the north and the Coastal Plain on the south; the two provinces are separated by the Balcones fault zone. In the Edwards Plateau the formations of the Edwards and associated limestones crop out on the plateau surface; in the Coastal Plain where the formations have been down-faulted, they underlie younger rocks. In both provinces the formations dip gently toward the south and southeast; the dips are greatest in the Coastal Plain. Igneous intrusions have penetrated the formations in many places in the Coastal Plain, and locally have formed barriers to ground-water movement.
\n\n
The aquifers in Uvalde County are recharged by precipitation within the county and in the drainage areas of streams entering the county from the north and west. In the Edwards Plateau, the Edwards and associated limestones are recharged by precipitation that falls on the outcrop. The aquifer is drained by springs at the contact with the underlying Glen Rose limestone where streams have cut through the Edwards at the edge of the plateau. These springs maintain the base flow of the streams that drain the plateau. Most of the base flow and much of flood flow of the streams is lost to the Edwards and associated limestones where they crop out in streambeds in the Balcones fault zone. This stream loss to the aquifer constitutes the greatest part of the recharge in the county, although some of the recharge from the West Nueces River enters the county as underflow from Kinney County. The normal annual recharge to the Edwards in Uvalde County is estimated to be about 200,000 acre-feet.
\n\n
Discharge from the Edwards and associated limestones in Uvalde County can be divided into two .major segments: discharge by underflow from the county to the east and south and discharge to the surface through wells and springs. Discharge by underflow during the period 1934-47, when changes in storage were small, is estimated to have been about 190,000 acre-feet per year. During the drought years 1947-56 the underflow was somewhat less. The discharge to the surface during 1934-47 averaged about 17,000 acre-feet per year. During the 1947-56 drought the rate of discharge to the surface increased principally because of increased use of water for irrigation, reaching a maximum of 58,000 acre-feet in 1956.
\n\n
The chemical quality. of the ground water in Uvalde County ranges between wide limits. Except in the extreme southern part of the county where the water is saline, the water in the Edwards and associated limestones is of good chemical quality except that it is hard. The water in the Glen Rose limestone is saline in many places; the principal objectionable constituents are high concentrations of calcium and magnesium sulfate. The water in the Leona formation is generally of good chemical quality. The water from the other formations varies widely in quality from place to place and no generalizations can be made.
\n\n
Ground-water withdrawals from the Edwards and associated limestones in Uvalde County probably could be maintained indefinitely at a rate of about 200,000 acre-feet per year, provided that withdrawals north and west of the county were not increased. However, continued withdrawals at this rate-would cause wells in structurally high areas to go dry, and underflow into Medina County would cease. Furthermore, saline water might invade the fresh-water part of the aquifer from the south, and perennial spring flow in the Leona River valley would cease.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1584","collaboration":"Prepared in cooperation with the Texas Board of Water Engineers and the City of San Antonio","usgsCitation":"Welder, F., and Reeves, R., 1964, Geology and ground-water resources of Uvalde County, Texas: U.S. Geological Survey Water Supply Paper 1584, Report: v, 49 p.; 12 Plates: 28 x 28 inches or smaller, https://doi.org/10.3133/wsp1584.","productDescription":"Report: v, 49 p.; 12 Plates: 28 x 28 inches or smaller","numberOfPages":"57","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":29585,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":110058,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25579.htm","linkFileType":{"id":5,"text":"html"},"description":"25579"},{"id":29586,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29587,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29588,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29589,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29590,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29591,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29592,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29593,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29594,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29595,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29596,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138405,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1584/report-thumb.jpg"},{"id":277928,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1584/report.pdf"}],"scale":"125000","country":"United States","state":"Texas","county":"Uvalde County","city":"San Antonio","otherGeospatial":"Coastal Plain;Edwards Plateau;West Nueces River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -101.0,28.0 ], [ -101.0,31.0 ], [ -97.0,31.0 ], [ -97.0,28.0 ], [ -101.0,28.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685977","contributors":{"authors":[{"text":"Welder, F.A.","contributorId":104878,"corporation":false,"usgs":true,"family":"Welder","given":"F.A.","email":"","affiliations":[],"preferred":false,"id":145987,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reeves, R.D.","contributorId":95043,"corporation":false,"usgs":true,"family":"Reeves","given":"R.D.","email":"","affiliations":[],"preferred":false,"id":145986,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"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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Off.,","doi":"10.3133/wsp1669S","usgsCitation":"Busby, M., 1964, Yearly variations in runoff for the conterminous United States, 1931-1960: U.S. Geological Survey Water Supply Paper 1669, iii, 49 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1669S.","productDescription":"iii, 49 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":137917,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669s/report-thumb.jpg"},{"id":25827,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669s/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d6e4b07f02db5de56d","contributors":{"authors":[{"text":"Busby, Mark W.","contributorId":83099,"corporation":false,"usgs":true,"family":"Busby","given":"Mark W.","affiliations":[],"preferred":false,"id":143172,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2983,"text":"wsp1499E - 1964 - Water resources of the Flint area, Michigan","interactions":[],"lastModifiedDate":"2017-02-06T15:45:12","indexId":"wsp1499E","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":"E","title":"Water resources of the Flint area, Michigan","docAbstract":"This report describes the water resources of Genesee County, Mich., whose principal city is Flint. The sources of water available to the county are the Flint and Shiawassee Rivers and their tributaries, inland lakes, ground water, and Lake Huron. The withdrawal use of water in the county in 1958 amounted to about 45 mgd. Of this amount, 36 mgd was withdrawn from the Flint River by the Flint public water-supply system. The rest was supplied by wells. At present (1959) the Shiawassee River and its tributaries and the inland lakes are not used for water supply.
Flint River water is used for domestic, industrial, and waste-dilution requirements in Flint. About 60 percent of the water supplied by the Flint public water system is used by Flint industry. At least 30 mgd of river water is needed for waste dilution in the Flint River during warm weather.
Water from Holloway Reservoir, which has a storage capacity of 5,760 million gallons, is used to supplement low flows in the Flint River to meet water-supply and waste-dilution requirements. About 650 million gallons in Kearsley Reservoir, on a Flint River tributary, is held in reserve for emergency use. Based on records for the lowest flows during the period 1930-52, the Flint River system, with the two reservoirs in operation, is capable of supplying about 60 mgd at Flint, less evaporation and seepage losses. The 1958 water demands exceeded this amount. Development of additional storage in the Flint River basin is unlikely because of lack of suitable storage sites. Plans are underway to supply Flint and most of Genesee County with water from Lake Huron.
The principal tributaries of the Flint River in and near Flint could furnish small supplies of water. Butternut Creek, with the largest flow of those studied, has an estimated firm yield of 0.054 mgd per sq mi for 95 percent of the time. The Shiawassee River at Byron is capable of supplying at least 29 mgd for 95 percent of the time.
Floods are a serious problem in Flint. The April 1947 flood, the largest on record, caused nearly $4 million flood damage in Flint. A proposed flood-control plan for Flint calls for channel, floodwall, and levee improvements and the removal or modification of some bridges.
Analyses of water samples taken from selected streams and lakes in the Flint area indicate that the waters are of the calcium bicarbonate type and generally hard to very hard. Flint River water is relatively uniform in quality although a progressive increase in iron, sodium, and chloride concentrations was noted between Otisville and Montrose. Downstream from Flint, the dissolved oxygen
content may be low during low flows. At times, concentrations of iron, manganese, phenols, color, and turbidity in Flint River water exceed the limits recommended in drinking water standards. Water temperatures ranged from freezing to 86°F in a 4-year period. The finished water supplied by the Flint water-treatment plant is fairly uniform in quality, moderately soft, alkaline, and low in color and turbidity. The pH is nearly always above 10. Further softening and removal of iron and related minerals would be desirable for certain industrial uses.
The quality of the water sampled in the Flint River tributaries was generally similar to that of the Flint River. However, no phenols or oils and waxes were found. Softening and other treatment dependent upon use would be required if these streams were developed for water supply.
Waters sampled in the Shiawassee River and selected lakes were generally less mineralized than Flint River water. Water from the lakes showed the lowest concentrations of dissolved solids. Softening would be required for nearly all uses. Additional treatment would depend upon contemplated use.
Shallow deposits of sand and gravel deposited as outwash along glacial meltwater streams and as deltas in the glacial lakes that covered the northwestern part of the county are sources of water to moderate- and large-capacity wells. Thick deposits of sand and gravel also fill some of the valleys in the bedrock surface and yield moderate to large supplies of water. Production from public supply wells tapping the drift aquifers in the area ranges from about 50 to 1,200 gpm. The water from the drift aquifer is hard or very hard and commonly contains objectionable amounts of iron.
The Saginaw formation is a source of water to wells supplying some of the small communities and industries in the county. The Saginaw, which is the uppermost bedrock formation in the area, underlies most of the county. It is composed of layers of sandstone, shale, and limestone and some beds of coal. The formation is composed principally of sandstone in some areas of the county, and shale in others. Production from wells tapping the Saginaw ranges from a few to about 500 gpm. The water produced is generally moderately hard or hard and commonly contains objectionable amounts of chloride. The quality of the water limits its development for water supply. Overdrafts from the Saginaw result in a lowering of the piezometric surface and commonly cause an upward migration of water high in chloride.
The Michigan and Marshall formations are generally not sources of fresh water where they are overlain by the Saginaw formation. In the southern and eastern parts of the county where they are overlain by glacial deposits, they are a source of water of good quality. The quantity of water obtainable from these formations is not fully known. However, the Marshall may be a source of large supplies of water in the southeastern part of the county.
An ample supply of water is available in lakes, ponds, and streams in the metropolitan area of Flint to meet requirements for domestic, sanitary, and firefighting use in civil defense emergencies. The extent of emergency use of water from these sources would depend upon the pumping, distribution, and treatment facilities available. Enough private industrial and commercial, and public wells are present in the area normally supplied by the Flint public water system to meet emergency requirements for domestic and sanitary use. Use of these wells would also depend upon available pumping and distribution facilities. Water from many of these wells contains objectionable amounts of chloride, but it could be used without treatment in an emergency.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1499E","usgsCitation":"Wiitala, S.W., Vanlier, K., and Krieger, R.A., 1964, Water resources of the Flint area, Michigan: U.S. Geological Survey Water Supply Paper 1499, Document: viii, 86 p.; 6 Plates: 20.00 x 18.29 inches or smaller, https://doi.org/10.3133/wsp1499E.","productDescription":"Document: viii, 86 p.; 6 Plates: 20.00 x 18.29 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":139431,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499e/report-thumb.jpg"},{"id":29743,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29744,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29745,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29746,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29747,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29748,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29749,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Michigan","county":"Genesee County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-83.4607,43.2235],[-83.4593,43.1425],[-83.4589,43.1365],[-83.455,42.9681],[-83.4553,42.9617],[-83.4546,42.8798],[-83.4541,42.8766],[-83.5737,42.8744],[-83.6902,42.871],[-83.6863,42.7822],[-83.9225,42.7812],[-83.928,42.8677],[-83.9309,42.9574],[-83.9283,43.0451],[-83.9294,43.1334],[-83.9318,43.2204],[-83.8154,43.2212],[-83.694,43.2223],[-83.5809,43.2226],[-83.4607,43.2235]]]},\"properties\":{\"name\":\"Genesee\",\"state\":\"MI\"}}]}\n","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a14e4b07f02db602df3","contributors":{"authors":[{"text":"Wiitala, Sulo Werner","contributorId":20315,"corporation":false,"usgs":true,"family":"Wiitala","given":"Sulo","email":"","middleInitial":"Werner","affiliations":[],"preferred":false,"id":146097,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Vanlier, K.E.","contributorId":24332,"corporation":false,"usgs":true,"family":"Vanlier","given":"K.E.","affiliations":[],"preferred":false,"id":146098,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Krieger, Robert A.","contributorId":99954,"corporation":false,"usgs":true,"family":"Krieger","given":"Robert","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":146099,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1106,"text":"wsp1669W - 1964 - The yield of sedimentary aquifers of the coastal plain, southeast river basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1669W","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":"W","title":"The yield of sedimentary aquifers of the coastal plain, southeast river basins","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. G.P.O.,","doi":"10.3133/wsp1669W","usgsCitation":"Callahan, J.T., 1964, The yield of sedimentary aquifers of the coastal plain, southeast river basins: U.S. Geological Survey Water Supply Paper 1669, iv, 56 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1669W.","productDescription":"iv, 56 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":137882,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669w/report-thumb.jpg"},{"id":25841,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669w/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25842,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669w/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a57e4b07f02db62e816","contributors":{"authors":[{"text":"Callahan, Joseph Thomas","contributorId":45689,"corporation":false,"usgs":true,"family":"Callahan","given":"Joseph","email":"","middleInitial":"Thomas","affiliations":[],"preferred":false,"id":143186,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2900,"text":"wsp1539J - 1964 - Geology and ground-water resources of Yuma County, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:05:21","indexId":"wsp1539J","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":"1539","chapter":"J","title":"Geology and ground-water resources of Yuma County, Colorado","language":"ENGLISH","publisher":"United States Government Printing Office,","doi":"10.3133/wsp1539J","usgsCitation":"Weist, W., 1964, Geology and ground-water resources of Yuma County, Colorado: U.S. Geological Survey Water Supply Paper 1539, iv, 56 p. :ill., map ;24 cm. & 7 maps in pocket., https://doi.org/10.3133/wsp1539J.","productDescription":"iv, 56 p. :ill., map ;24 cm. & 7 maps in pocket.","costCenters":[],"links":[{"id":109977,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24732.htm","linkFileType":{"id":5,"text":"html"},"description":"24732"},{"id":138381,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1539j/report-thumb.jpg"},{"id":29567,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539j/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29568,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539j/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29569,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539j/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29570,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539j/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29571,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539j/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29572,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539j/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29573,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539j/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29574,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1539j/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685789","contributors":{"authors":[{"text":"Weist, William G.","contributorId":21526,"corporation":false,"usgs":true,"family":"Weist","given":"William G.","affiliations":[],"preferred":false,"id":145979,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1122,"text":"wsp1773 - 1964 - Geology and ground-water resources of the Anchorage area, Alaska","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1773","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":"1773","title":"Geology and ground-water resources of the Anchorage area, Alaska","docAbstract":"The Anchorage area, at the head of Cook Inlet in south-central Alaska, \r\noccupies 150 square miles of a glaciated lowland and lies between two estuaries and the Chugach Mountains. Two military bases are in the area; \r\nAnchorage is the largest city in Alaska and the chief transportation center \r\nfor this part of the State. \r\nThe bedrock in the Anchorage area is chiefly Tertiary shale in the lowland \r\nand metamorphic rocks of Mesozoic age beneath the adjacent mountain \r\nslopes. Glacial drift which underlies nearly the entire area has an average \r\nthickness of several hundred feet and appears to include at least five sheets \r\nof deposits, two of which are exposed. The drift consists of till, outwash stream and lake deposits (sand and gravel), and estuarine (and lake) deposits \r\n(clay and silt). The stratigraphy and lateral distribution of the deposits are \r\ncomplex, but data at hand s, how that the thickest deposits, including all the \r\nestuarine and lake sediment and most of the stream-deposited sediment, \r\nare beneath the lowland away from the mountain wall, and that the deposits \r\nnear the mountains are till and subordinate outwash sediments. \r\nDeposits of sand and gravel laid down by outwash streams in channels and \r\non outwash plains are the most important aquifers, and the only \r\nones which yield large quantities of ground water from single beds. Thin \r\nlayers of sandy or gravelly material in till are also important aquifers although they yield relatively small quantities of water. Bedded sand and \r\nsilt associated with the estuarine and lake(?) clay commonly becomes unstable during drilling and pumping, and has been successfully developed in \r\nonly a few wells. Unconfined aquifers are extensive, but permeable saturated \r\nmaterial is thin in many places and water supplies available from them are \r\nsmall or undependable in those places. The most important aquifers are confined or artesian. Clay and till form the confining beds: the till is somewhat 'leaky' in many places. Near Anchorage the buried water-bearing \r\nbeds appear to be interconnected and to form a single artesian system. The \r\nwater table and piezometric surface slope from the mountain wall of the \r\nlowland toward the estuaries, and the flow of the ground water is in that \r\ndirection. The aquifers are recharged by the infiltration of precipitation \r\nat the land surface and of surface water through stream beds: near the mountains the artesian aquifers are probably recharged in part by percolation from \r\nthe water-table aquifer, and far from the mountains the water-table aquifer \r\nis probably recharged in part by upward flow from the underlying artesian \r\naquifers. In several valleys and in a few other places, in the lowland, artesian wells flow at the land surface. \r\nThe outwash sand and gravel are moderately to very permeable; most \r\nof the other water-bearing material are much less permeable. The co- efficient of transmissibility for some single beds of sandy gravel is as high \r\nas 60,000 to I00,000 gpd per ft (gallons per day per foot); for the entire \r\nsection of glacial drift at and near Anchorage it is believed to be of the \r\norder of 200,000 gpd per ft. Calculations based on this value for the total \r\nsection and on the slope of the piezometric surface indicate that in the \r\nimmediate vicinity of Anchorage about 5 million gpd flows through each \r\nmile-wide section of the drift (measured in a northeast-southwest direction, perpendicular to the direction of flow), under normal (nonpumping) conditions. Under conditions of continuous heavy pumping the slope of the piezometric surface is steepened, flow is increased, and additional recharge is induced. \r\n\r\nThe highest yield reported from a well in this area is 2.600 gpm (gallons per minute) with 35 feet of drawdown: the highest reported specific capacity is 180 gpm per ft of drawdown, for a well pumped at. 270 gpm. \r\n\r\nOnly a few wells in the area have been developed for high yields. Well screens have been used ","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1773","usgsCitation":"Cederstrom, D.J., Trainer, F.W., and Waller, R.M., 1964, Geology and ground-water resources of the Anchorage area, Alaska: U.S. Geological Survey Water Supply Paper 1773, vi, 108 p. :illus., maps (1 col.) diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1773.","productDescription":"vi, 108 p. :illus., maps (1 col.) diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":138014,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1773/report-thumb.jpg"},{"id":25887,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25888,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25889,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25890,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25891,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1773/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6855f4","contributors":{"authors":[{"text":"Cederstrom, Dagfin John","contributorId":90287,"corporation":false,"usgs":true,"family":"Cederstrom","given":"Dagfin","email":"","middleInitial":"John","affiliations":[],"preferred":false,"id":143212,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Trainer, Frank W.","contributorId":103655,"corporation":false,"usgs":true,"family":"Trainer","given":"Frank","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":143213,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Waller, Roger Milton","contributorId":22320,"corporation":false,"usgs":true,"family":"Waller","given":"Roger","email":"","middleInitial":"Milton","affiliations":[],"preferred":false,"id":143211,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"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}]}} ]}