The increasing use of ground water from many major aquifers in the United States has required a more thorough understanding of gravity drainage, or specific yield. This report describes one phase of specific yield research by the U.S. Geological Survey's Hydrologic Laboratory in cooperation with the California Department of Water Resources.
An earlier phase of the research concentrated on the final distribution of moisture retained after drainage of saturated columns of porous media. This report presents the phase that concentrated on the distribution of moisture retained in similar columns after drainage for various periods of time.
Five columns, about 4 cm in diameter by 170 cm long, were packed with homogenous sand of very fine, medium, and coarse sizes, and one column was packed with alternating layers of coarse and medium sand. The very fine materials were more uniform in size range than were the medium materials. As the saturated columns drained, tensiometers installed throughout the length recorded changes in moisture tension. The relation of tension to moisture content, determined for each of the materials, was then used to convert the tension readings to moisture content. Data were then available on the distribution of retained moisture for different periods of drainage from 1 to 148 hours. Data also are presented on the final distribution of moisture content by weight and volume and on the degree of saturation.
The final zone of capillary saturation was approximately 12 cm for coarse sand, 13 cm for medium sand, and 52 cm for very fine sand. The data showed these zones were 92 to 100 percent saturated.
Most of the outflow from the columns occurred in the earlier hours of drainage--90 percent in 1 hour for the coarse materials, 50 percent for the medium, and 60 percent for the very fine. Although the largest percentage of the specific yield was reached during the early hours of drainage, this study amply demonstrates that a very long time would be required to reach drainage equilibrium.
In the layered columns the middle (medium sand) layer functioned as a hanging water column accelerating the drainage of the overlying coarse-sand layer. After the middle layer started to drain, the moisture distribution as retained in all three layers showed trends similar to that obtained when the same materials were tested in homogenous columns.
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1662B","collaboration":"Prepared in cooperation with the California Department of Water Resources","usgsCitation":"Prill, R.C., Johnson, A., and Morris, D.A., 1965, Specific yield - laboratory experiments showing the effect of time on column drainage: U.S. Geological Survey Water Supply Paper 1662, iv, 55 p., https://doi.org/10.3133/wsp1662B.","productDescription":"iv, 55 p.","costCenters":[],"links":[{"id":138581,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1662b/report-thumb.jpg"},{"id":28778,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1662b/report.pdf","text":"Report","size":"1.51 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7ee4b07f02db64853b","contributors":{"authors":[{"text":"Prill, Robert C.","contributorId":86317,"corporation":false,"usgs":true,"family":"Prill","given":"Robert","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":145366,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, A.I.","contributorId":82676,"corporation":false,"usgs":true,"family":"Johnson","given":"A.I.","email":"","affiliations":[],"preferred":false,"id":145365,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Morris, Donald Arthur","contributorId":13960,"corporation":false,"usgs":true,"family":"Morris","given":"Donald","email":"","middleInitial":"Arthur","affiliations":[],"preferred":false,"id":145364,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":940,"text":"wsp1576F - 1965 - Geology and hydrology of the Fort Belknap Indian Reservation, Montana","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1576F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1576","chapter":"F","title":"Geology and hydrology of the Fort Belknap Indian Reservation, Montana","docAbstract":"The Fort Belknap Indian Reservation includes an area of 970 square miles in north-central Montana. At its north edge is the Milk River valley, which is underlain by Recent alluvium of the Milk River, glacial deposits, and alluvial deposits of the preglacial Missouri River, which carved and occupied this valley before the Pleistocene Epoch. Rising gently to the south is an undulating glaciated plain broken only by three small syenite porphyry intrusions. Underlying the glacial till of the plain are Upper Cretaceous shale and sandstone of the Bearpaw and Judith River Formations. At the south end of the reservation, 40 miles from the Milk River, an intrusion of syenite porphyry in Tertiary time uplifted, tilted, and exposed the succession of sedimentary rocks overlying the Precambrian metamorphic basement. The sedimentary rocks include 1,000 feet of sandstone and shale of Cambrian age; 2,000 feet of limestone and dolomite of Ordovician, Devonian, and Mississippian age; 400 feet of shale and limestone of Jurassic age; and 3,500 feet of sandstone, siltstone, and shale of Cretaceous age. Extensive gravel terraces of Tertiary and Quaternary age bevel the upturned bedrock formations exposed around the Little Rocky Mountains. \r\n\r\nGround water under water-table conditions is obtained at present from alluvium, glaciofluvial deposits, and the Judith River Formation. The water table ranges in depth from a few feet beneath the surface in the Milk River valley alluvium to more than 100 feet deep in the Judith River Formation. Yields to wells are generally low but adequate for domestic and stock-watering use. Quality of the water ranges from highly mineralized and unusable to excellent; many wells in the Milk River valley have been abandoned because of the alkalinity of their water. Potential sources of additional ground-water supplies are the alluvial gravel of creeks issuing from the Little Rocky Mountains and some extensive areas of terrace gravel. \r\n\r\nThe uplift and tilting of the sedimentary sequence around the Little Rocky Mountains and the minor intrusions in the central plain have created artesian conditions within aquifers. Wells obtain artesian water from sandstone aquifers in the Judith River, Eagle, and Kootenai Formations. Other potential aquifers, near their outcrop areas, are the Ellis Group and the Mission Canyon Limestone. \r\n\r\nMost wells that flow at the surface have small yields, but discharges of as much as 150 gallons per minute have been noted. Quality of artesian water ranges from poor to good. Well depths range from less than 50 to more than 300 feet.","language":"ENGLISH","publisher":"United States Government Printing Office,","doi":"10.3133/wsp1576F","usgsCitation":"Alverson, D.C., 1965, Geology and hydrology of the Fort Belknap Indian Reservation, Montana: U.S. Geological Survey Water Supply Paper 1576, iv, 59 p. :ill. ;24 cm. & 1 map in pocket., https://doi.org/10.3133/wsp1576F.","productDescription":"iv, 59 p. :ill. ;24 cm. & 1 map in pocket.","costCenters":[],"links":[{"id":109989,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24758.htm","linkFileType":{"id":5,"text":"html"},"description":"24758"},{"id":137217,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1576f/report-thumb.jpg"},{"id":25425,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1576f/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25426,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1576f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b468d","contributors":{"authors":[{"text":"Alverson, Douglas C.","contributorId":68286,"corporation":false,"usgs":true,"family":"Alverson","given":"Douglas","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":142892,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1148,"text":"wsp1779U - 1965 - Geology and ground-water resources of Dane County, Wisconsin","interactions":[],"lastModifiedDate":"2015-10-02T13:08:12","indexId":"wsp1779U","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"U","title":"Geology and ground-water resources of Dane County, Wisconsin","docAbstract":"The purpose of the ground-water investigation of Dane County, Wis., was to determine the occurrence, movement, quantity, quality, and availability of ground water in the unconsolidated deposits and the underlying bedrock. The relationships between ground water and surface water were studied in general in Dane County and in detail in the Madison metropolitan area. An analysis was made of the hydrologic system of the Yahara River valley and of the effects of ground-water pumpage on that system.
","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/wsp1779U","collaboration":"Prepared in cooperation with the University of Wisconsin Geological and Natural History Survey","usgsCitation":"Cline, D.R., 1965, Geology and ground-water resources of Dane County, Wisconsin: U.S. Geological Survey Water Supply Paper 1779, Report: v, 64 p.; 8 Plates: 27.00 x 19.50 inches or smaller, https://doi.org/10.3133/wsp1779U.","productDescription":"Report: v, 64 p.; 8 Plates: 27.00 x 19.50 inches or smaller","numberOfPages":"64","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":25936,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779u/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137642,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1779u/report-thumb.jpg"},{"id":25937,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779u/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25931,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779u/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25930,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779u/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25932,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779u/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25933,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779u/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25934,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779u/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25935,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779u/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25938,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1779u/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","county":"Dane County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-89.0094,43.286],[-89.0084,43.2555],[-89.0094,43.2],[-89.01,43.1131],[-89.0109,43.0849],[-89.0107,43.0271],[-89.0132,42.9353],[-89.013,42.8762],[-89.0119,42.8471],[-89.132,42.8479],[-89.2488,42.8478],[-89.3689,42.8484],[-89.3688,42.8575],[-89.4832,42.858],[-89.6026,42.8575],[-89.7196,42.8587],[-89.8377,42.8598],[-89.8375,42.9471],[-89.8386,43.0317],[-89.8384,43.1181],[-89.8394,43.205],[-89.8325,43.2123],[-89.825,43.2187],[-89.8175,43.226],[-89.8125,43.2342],[-89.8088,43.2369],[-89.8012,43.2365],[-89.7874,43.2356],[-89.771,43.237],[-89.7579,43.2379],[-89.7529,43.2443],[-89.7485,43.2507],[-89.7391,43.2548],[-89.7259,43.2644],[-89.7171,43.2739],[-89.714,43.2821],[-89.7165,43.2867],[-89.7235,43.2935],[-89.7209,43.2935],[-89.6008,43.2932],[-89.4819,43.2942],[-89.3617,43.2954],[-89.3624,43.2832],[-89.246,43.2834],[-89.1271,43.2827],[-89.0094,43.286]]]},\"properties\":{\"name\":\"Dane\",\"state\":\"WI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685b40","contributors":{"authors":[{"text":"Cline, Denzel R.","contributorId":87910,"corporation":false,"usgs":true,"family":"Cline","given":"Denzel","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143258,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2771,"text":"wsp1809B - 1965 - Geology and ground-water resources of Waushara County, Wisconsin","interactions":[],"lastModifiedDate":"2015-10-02T13:14:56","indexId":"wsp1809B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1809","chapter":"B","title":"Geology and ground-water resources of Waushara County, Wisconsin","docAbstract":"Abundant ground water for irrigation is available in the outwash deposits in western Waushara County, and many more large-capacity wells can be developed in these deposits without seriously lowering the water level. Pumping for irrigation temporarily lowers water levels in the vicinity of the wells but has not lowered regional water levels. Pumpage has probably intercepted and utilized some of the recharge that would have been rapidly discharged from the aquifer. Ground water is continuously being discharged to streams and to the atmosphere by evapotranspiration, but intermittent recharge from precipitation replaces the discharged water. Recharge and discharge are in approximate balance, maintaining about the same amount of ground water in storage. Further recharge to the aquifer is rapidly discharged to streams. The sandstones, till, and glaciolacustrine deposits in Waushara County generally yield small to moderate amounts of water to wells but do not produce enough water for irrigation ; recent alluvium may yield large quantities of water to wells. In general, the ground water is of good quality, except for hardness and local high-iron concentrations.
","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/wsp1809B","collaboration":"Prepared in cooperation with the University of Wisconsin Geological and Natural History Survey","usgsCitation":"Summers, W.K., 1965, Geology and ground-water resources of Waushara County, Wisconsin: U.S. Geological Survey Water Supply Paper 1809, Report: iv, 32 p.; 3 Plates: 41.96 x 22.00 inches and 39.5 x 22.5 inches, https://doi.org/10.3133/wsp1809B.","productDescription":"Report: iv, 32 p.; 3 Plates: 41.96 x 22.00 inches and 39.5 x 22.5 inches","numberOfPages":"40","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":29216,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29217,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29218,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809b/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29219,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138609,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809b/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","county":"Waushara County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-89.5977,44.2458],[-89.488,44.244],[-89.4835,44.244],[-89.3649,44.2439],[-89.3464,44.2439],[-89.2469,44.2438],[-89.2245,44.2433],[-89.1288,44.243],[-89.104,44.243],[-89.007,44.2426],[-88.9821,44.243],[-88.8871,44.2426],[-88.8859,44.1587],[-88.8882,44.1136],[-88.8861,44.0713],[-88.8862,43.9833],[-88.944,43.9836],[-89.0063,43.9834],[-89.1283,43.9833],[-89.1658,43.983],[-89.2472,43.9827],[-89.3654,43.9824],[-89.4823,43.982],[-89.598,43.9824],[-89.5981,44.0685],[-89.5976,44.156],[-89.5977,44.2458]]]},\"properties\":{\"name\":\"Waushara\",\"state\":\"WI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685374","contributors":{"authors":[{"text":"Summers, William Kelly","contributorId":69532,"corporation":false,"usgs":true,"family":"Summers","given":"William","email":"","middleInitial":"Kelly","affiliations":[],"preferred":false,"id":145756,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2475,"text":"wsp1809N - 1965 - Effects of waste water from A.E.C. plant on the hydrology of Glowegee Creek at West Milton, New York, 1958-61","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"wsp1809N","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1809","chapter":"N","title":"Effects of waste water from A.E.C. plant on the hydrology of Glowegee Creek at West Milton, New York, 1958-61","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1809N","usgsCitation":"Pauszek, F.H., and Ruggles, F., 1965, Effects of waste water from A.E.C. plant on the hydrology of Glowegee Creek at West Milton, New York, 1958-61: U.S. Geological Survey Water Supply Paper 1809, iv, 29 p. :ill., map ;24 cm., https://doi.org/10.3133/wsp1809N.","productDescription":"iv, 29 p. :ill., map ;24 cm.","costCenters":[],"links":[{"id":138748,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809n/report-thumb.jpg"},{"id":28551,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809n/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a26e4b07f02db60fc24","contributors":{"authors":[{"text":"Pauszek, F. H.","contributorId":61399,"corporation":false,"usgs":true,"family":"Pauszek","given":"F.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":145254,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ruggles, Frederick H.","contributorId":96665,"corporation":false,"usgs":true,"family":"Ruggles","given":"Frederick H.","affiliations":[],"preferred":false,"id":145255,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":929,"text":"wsp1771 - 1965 - Geology and ground water in the central part of Apache County, Arizona","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1771","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1771","title":"Geology and ground water in the central part of Apache County, Arizona","docAbstract":"The central part of Apache County, Ariz., includes an area of about 3,300 \r\nsquare miles between the Navajo Indian Reservation to the north and U.S. \r\nHighway 60 to the south. Sedimentary rocks in the area range from Pennsylvanian to Quaternary in age and from 2,000 to more than 6,000 feet in \r\nthickness. The strata were tilted to the northeast, and part of the Upper \r\nTriassic and all the Jurassic and Lower Cretaceous rocks were eroded away \r\nbefore strata of Late Cretaceous age were deposited. Basaltic lava flows and \r\ncinder cones, representing four general periods of eruption in late Miocene to \r\nQuaternary time, are widespread in the southern part of the area. \r\nPennsylvanian and Permian rocks overlie basement rocks of granite and \r\ndiorite and include the Supai Formation, the Coconino Sandstone, and the \r\nKaibab Limestone. The Supai Formation is 1,000 to 2,000 feet thick and consists of interbedded red and brown mudstone, siltstone, sandstone, limestone, \r\nand evaporites. It contains water of very poor quality outside Apache County. \r\nThe Coconino Sandstone is 200 to 250 feet thick and consists of light-gray \r\nfine- to medium-grained sandstone. It contains water suitable for domestic \r\nuse in the south and water unsuitable for most purposes in the north. The \r\nCoconino Sandstone underlies all Central Apache County in the subsurface. \r\nThe yellowish-gray to dark-gray Kaibab Limestone is present in the southern \r\ntwo-thirds of the area and is 0 to 350 feet thick. It contains water where it \r\nis fractured and combines with the Coconino Sandstone to form a single hydrologic unit that yields from 6 to 74 gpm (gallons per minute) of water per foot \r\nof drawdown. \r\n\r\nAn unconformity Heparates the Permian rocks from the overlying Triassic \r\nrocks, which comprise the Moenkopi and Chinle Formations and the Wingate \r\nSandstone. The Moenkopi Formation is 35 to 250 feet thick and consists of \r\nintercalated brownish-red siltstone, sandstone, and conglomerate. It contains \r\nsalty water in some areas but is dry in most. The Chinle Formation is 0 to 1,550 \r\nfeet thick and unconformably overlies the Moenkopi. The Chiule consists of \r\nmulticolored claystone, mudstone, siltstone, sandstone, and conglomerate. \r\nSome of the sandstone units yield small amounts of water, usually of a quality \r\nunsuitable for domestic use. The Wingate Sandstone is about 250 feet thick \r\nand is present only in the extreme northeastern corner of the area. It consists \r\nof intercalated, reddish-brown sandstone and siltstone and does not contain \r\nwater. \r\n\r\nThe Upper Cretaceous rocks comprise the Dakota Sandstone, from 50 to \r\n115 feet thick; the Mancos Shale, about 150 feet thick; and the Mesaverde Group, \r\nas much as 200 feet thick. These rocks consist of yellowish-gray, light-green, and reddish-brown sandstone and carbonaceous siltstone. Some of the sandstone units contain water of suitable quality for domestic use, and wells in these units yield from 10 to 1,000 gpm.\r\n\r\nSedimentary rocks of Eocene(?) age are about 800 feet thick and unconformably overlie Cretaceous rocks. They consist of light-brown and medium-red conglomerate, sandstone, and siltstone. These sedimentary rocks contain small amounts of water suitable for domestic use and yield from 10 to 25 gpm in the Springerville area. The Datil Formation of Miocene(?) Tertiary age consists of more than 800 feet of sedimentary rocks, which are composed largely of volcanic fragments. The Datil Formation does not contain water in the one small area where it crops out.\r\n\r\nThe Bidahochi Formation of Pliocene age consists of 0 to 800 feet of white, green, and brown claystone, mudstone, and sandstone. Locally it yields from 10 to 50 gpm of water suitable for domestic use.\r\n\r\nQuaternary rocks consist of as much as 500 feet of alluvium, sand, gravel, travertine, cinders, and lava. The alluvium along the large drainages contains water that differs in quality from place to place. In most areas where it occurs, the lava ","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1771","usgsCitation":"Akers, J.P., 1965, Geology and ground water in the central part of Apache County, Arizona: U.S. Geological Survey Water Supply Paper 1771, vi, 107 p. :illus., maps (3 fold., 1 col., in pocket) ;24 cm., https://doi.org/10.3133/wsp1771.","productDescription":"vi, 107 p. :illus., maps (3 fold., 1 col., in pocket) ;24 cm.","costCenters":[],"links":[{"id":138033,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1771/report-thumb.jpg"},{"id":25400,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1771/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25401,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1771/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25402,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1771/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25399,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1771/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db686039","contributors":{"authors":[{"text":"Akers, J. P.","contributorId":82678,"corporation":false,"usgs":true,"family":"Akers","given":"J.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":142870,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2906,"text":"wsp1791 - 1965 - Hydrologic conditions near Glendo, Platte County, Wyoming","interactions":[{"subject":{"id":52143,"text":"ofr60152 - 1960 - Hydrologic conditions in the Horseshoe Creek Valley near Glendo, Platte County, Wyoming","indexId":"ofr60152","publicationYear":"1960","noYear":false,"title":"Hydrologic conditions in the Horseshoe Creek Valley near Glendo, Platte County, Wyoming"},"predicate":"SUPERSEDED_BY","object":{"id":2906,"text":"wsp1791 - 1965 - Hydrologic conditions near Glendo, Platte County, Wyoming","indexId":"wsp1791","publicationYear":"1965","noYear":false,"title":"Hydrologic conditions near Glendo, Platte County, Wyoming"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:21","indexId":"wsp1791","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1791","title":"Hydrologic conditions near Glendo, Platte County, Wyoming","docAbstract":"The Glendo area of Platte and Carbon Counties, Wyo., about 250 square miles in extent, is in the Great Plains physiographic province. It is bordered on the west by the Laramie Range and on the east by the Hartville uplift. The North Platte River and Horseshoe and Middle Bear Creeks are the principal streams that drain the area. Gentle to steep hills, which lie between 4,450 and 6,360 feet above sea level, characterize the topography. Approximately 7,600 acres of land is cultivated in the Horseshoe Creek valley and 1,000 or more acres in the Cassa Flats of the North Platte River and Middle Bear Creek valleys. The average annual precipitation of 13.15 inches and the streamflow diverted for irrigation from Horseshoe Creek and the North Platte River are usually inadequate to sustain crops during the entire growing season. \r\n\r\nSedimentary rocks, which underlie about 99 percent of the Glendo area, range in age from Cambrian(?) to Recent and in thickness from about 3,000 to 4,700 feet. Beds of Paleozoic and Mesozoic age dip steeply away from the Laramie Range and the Hartville uplift to form a large syncline, which is interrupted by the Elkhorn anticline in the central part of the area. Beds of Tertiary and Quaternary age that were deposited over the older structural features and later were partly removed by erosion have dips of less than 6 ? . The 'Converse sand' of local usage at the top of the Hartville Formation of Mississippian(7), Pennsylvanian, and Permian age, the White River Formation of Oligocene age, and the flood-plain deposits of Recent .age are the most important aquifers in the Glendo area. \r\n\r\nThe Hartville Formation consists predominantly of hard limestone and dolomite and of lesser amounts of sandstone and shale ; its thickness ranges from 850 to 1,050 feet throughout most of the area. The 'Converse sand' is an artesian aquifer consisting of fine- to medium-grained porous sandstone having an average thickness of about 80 feet. \r\n\r\nRecharge to the Hartville Formation is mainly from seepage of surface water from Glendo Reservoir and Spring Creek; ground water is discharged from the formation to the overlying White River Formation and the alluvium in the North Platte River valley near Cassa and to four wells in the Horseshoe Creek valley. Flowing wells yielding from a few gallons per minute to 175 gpm (gallons per minute) or more from the 'Converse sand' can probably be located in an area from ? mile to 1? miles wide and about 4? miles long in the lower Horseshoe Creek valley. The depth to the 'Converse sand' in this area depends upon the topographic relief and distance from the outcrop and ranges from 250 to about 1,000 feet. The discharge induced by pumping a well in the aquifer in the 'Converse sand' would probably amount to about 2 gpm per foot of drawdown. Values of 2,000, 2,100, and 10,300 gpd (gallons per day) per ft for the coefficient of transmissibility of the 'Converse sand' were obtained from aquifer tests at three wells. \r\n\r\nThe chemical analyses of samples from the Hartville Formation ('Converse. sand' included) indicate that the water in the formation is of fairly good quality and adequate for domestic, stock, and irrigation uses, although the fluoride content is low and the water is hard. \r\n\r\nThe White River Formation is composed of as much as 575 feet of fractured siltstone and claystone, and the flood-plain deposits include up to 65 feet of silt, sand, and gravel. Precipitation is the main type of recharge to the rocks of Tertiary age. Recharge to the alluvium in the valleys of Horseshoe Creek and the North Platte River occurs mainly by seepage of ground water from. underlying beds, by infiltration of irrigation water, and by infiltration of streamflow as bank storage. Ground water is discharged naturally from the area \r\n\r\nby seepage to streams, by underflow, and by evapotranspiration and artificially by wells. In 1961, the total discharge from 38 wells in the White River and Arikaree Formations and 2","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1791","usgsCitation":"Welder, G.E., and Weeks, E.P., 1965, Hydrologic conditions near Glendo, Platte County, Wyoming: U.S. Geological Survey Water Supply Paper 1791, v, 82 p. :illus., maps (2 col.) ;24 cm., https://doi.org/10.3133/wsp1791.","productDescription":"v, 82 p. :illus., maps (2 col.) ;24 cm.","costCenters":[],"links":[{"id":138406,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1791/report-thumb.jpg"},{"id":29597,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1791/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29598,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1791/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29599,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1791/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29600,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1791/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad4e4b07f02db6832bd","contributors":{"authors":[{"text":"Welder, G. E.","contributorId":100814,"corporation":false,"usgs":true,"family":"Welder","given":"G.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":145989,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weeks, Edwin P. epweeks@usgs.gov","contributorId":2576,"corporation":false,"usgs":true,"family":"Weeks","given":"Edwin","email":"epweeks@usgs.gov","middleInitial":"P.","affiliations":[],"preferred":true,"id":145988,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5712,"text":"pp498C - 1965 - Relation of electrochemical potentials and iron content to ground-water flow patterns","interactions":[],"lastModifiedDate":"2017-04-25T14:05:37","indexId":"pp498C","displayToPublicDate":"1993-01-01T10:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"498","chapter":"C","title":"Relation of electrochemical potentials and iron content to ground-water flow patterns","docAbstract":"This study was undertaken to develop means of measuring oxidation potentials in aquifer systems and to use the measured values in interpreting the behavior of iron in ground water. Anne Arundel County, Md., was selected as the area of study because of the wide range of concentration of iron-nearly zero to about 35 ppm-in the ground water and the rather complete information on the geology and hydrology. The regional geology consists of coastal plain sediments ranging in age from Early Cretaceous through the Recent. Most of the pH and oxidation-potential measurements were made in nonmarine Cretaceous deposits, only a few in the marine Eocene. Iron-bearing minerals in the area are primarily hematite or limonite and glauconite with a small amount of pyrite.
Equipment was developed that permits the measurement of oxidation potentials by use of saturated calomel and platinum electrodes in ground-water samples uncontaminated by oxygen of the atmosphere. Measured Eh values range from about +700 mv to -40 mv. Approximately 2 to 3 hours are required to measure a stable or nearly stable oxidation potential.
The mineralogy and organic content of the deposits and the ground-water flow pattern are the primary controls on the oxidation potential and pH of the water. A correlation exists between the oxidation potential and the concentration of iron in ground water; the higher concentrations occur in waters with the lowest values of Eh. The concentration of iron in the water tested shows little correlation with the pH of the water. The highest oxidation potentials were measured in water produced from shallow wells and those wells in recharge areas. The lowest potentials were measured farthest downgradient in water associated with gray and green sediments. The Eh values measured in the field are between values predicted from the solubility of Fe(OH)2(c) and values predicted from the solubility of hematite.
","largerWorkTitle":"Hydrology of aquifer systems","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp498C","usgsCitation":"Back, W., and Barnes, I., 1965, Relation of electrochemical potentials and iron content to ground-water flow patterns: U.S. Geological Survey Professional Paper 498, Report: iii, p. C1-C16; 3 Plates: 10.09 x 17.13 inches or less, https://doi.org/10.3133/pp498C.","productDescription":"Report: iii, p. C1-C16; 3 Plates: 10.09 x 17.13 inches or less","costCenters":[],"links":[{"id":32284,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0498c/report.pdf","text":"Report","size":"4.44 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":139891,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0498c/report-thumb.jpg"},{"id":340291,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0498c/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":340289,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0498c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":340290,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0498c/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Maryland","county":"Anne Arundel County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.87957763671875,\n 38.69408504756833\n ],\n [\n -76.387939453125,\n 38.69408504756833\n ],\n [\n -76.387939453125,\n 39.25352462727606\n ],\n [\n -76.87957763671875,\n 39.25352462727606\n ],\n [\n -76.87957763671875,\n 38.69408504756833\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67c2c3","contributors":{"authors":[{"text":"Back, William","contributorId":59007,"corporation":false,"usgs":true,"family":"Back","given":"William","email":"","affiliations":[],"preferred":false,"id":151472,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Barnes, Ivan","contributorId":56619,"corporation":false,"usgs":true,"family":"Barnes","given":"Ivan","email":"","affiliations":[],"preferred":false,"id":151471,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":6378,"text":"pp498B - 1965 - Variations in chemical character of water in the Englishtown Formation, New Jersey","interactions":[{"subject":{"id":52280,"text":"ofr62123 - 1962 - Variations in the chemical character of the water in the Englishtown formation, New Jersey","indexId":"ofr62123","publicationYear":"1962","noYear":false,"title":"Variations in the chemical character of the water in the Englishtown formation, New Jersey"},"predicate":"SUPERSEDED_BY","object":{"id":6378,"text":"pp498B - 1965 - Variations in chemical character of water in the Englishtown Formation, New Jersey","indexId":"pp498B","publicationYear":"1965","noYear":false,"chapter":"B","title":"Variations in chemical character of water in the Englishtown Formation, New Jersey"},"id":1}],"lastModifiedDate":"2017-03-15T12:57:36","indexId":"pp498B","displayToPublicDate":"1992-01-01T08:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"498","chapter":"B","title":"Variations in chemical character of water in the Englishtown Formation, New Jersey","docAbstract":"This investigation describes the variations in the chemical character of the water in the Englishtown Formation of Late Cretaceous age in the Atlantic Coastal Plain of New Jersey, and demonstrates the application of the concept of hydrochemical mapping to the study and evaluation of water-bearing materials. The chemistry of ground water is responsive to the physical environment and lends support to available geologic and hydrologic data. A study of the ground-water chemistry may even suggest concepts for which additional geologic or hydrologic data may not be obtainable by conventional methods of study. Hydrochemical mapping is particularly important in evaluating an aquifer satisfactorily, but it could be equally useful in regional geologic studies concerned with continuity of units or mineralogic differences and similarities.
","largerWorkTitle":"Hydrology of aquifer systems","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp498B","collaboration":"Prepared in cooperation with New Jersey Division of Water Policy and Supply","usgsCitation":"Seaber, P.R., 1965, Variations in chemical character of water in the Englishtown Formation, New Jersey: U.S. Geological Survey Professional Paper 498, iii, p. B1-B35, https://doi.org/10.3133/pp498B.","productDescription":"iii, p. B1-B35","costCenters":[],"links":[{"id":33751,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0498b/report.pdf","text":"Report","size":"5.30 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":121598,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0498b/report-thumb.jpg"}],"country":"United States","state":"New Jersey","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -74.28955078125,\n 40.50753459933616\n ],\n [\n -74.72351074218749,\n 40.13899044275822\n ],\n [\n -75.1519775390625,\n 39.882342585755744\n ],\n [\n -75.3497314453125,\n 39.806426117299374\n ],\n [\n -75.44860839843749,\n 39.688167045890395\n ],\n [\n -75.42938232421875,\n 39.58029027440865\n ],\n [\n -75.3826904296875,\n 39.56970506644249\n ],\n [\n -74.11651611328125,\n 39.816975090490004\n ],\n [\n -74.05334472656249,\n 39.87391156801293\n ],\n [\n -74.0093994140625,\n 40.134790883048524\n ],\n [\n -73.97918701171875,\n 40.361195540839\n ],\n [\n -73.99566650390625,\n 40.40094763151963\n ],\n [\n -74.058837890625,\n 40.44276659332215\n ],\n [\n -74.15496826171874,\n 40.478292268560175\n ],\n [\n -74.28955078125,\n 40.50753459933616\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a14e4b07f02db602af9","contributors":{"authors":[{"text":"Seaber, Paul R.","contributorId":67492,"corporation":false,"usgs":true,"family":"Seaber","given":"Paul","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":152609,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70112254,"text":"70112254 - 1965 - Infrared photography and imagery in water resources research","interactions":[],"lastModifiedDate":"2025-01-07T16:16:02.375348","indexId":"70112254","displayToPublicDate":"1990-06-12T09:49:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2136,"text":"Journal - American Water Works Association","active":true,"publicationSubtype":{"id":10}},"title":"Infrared photography and imagery in water resources research","docAbstract":"This article briefly describes the characteristics of infrared radiation and demonstrates how infrared photography and infrared imagery can be applied to water resources research, specifically to the identification and description of hydrologic features.
","language":"English","publisher":"American Water Works Association","publisherLocation":"Denver, CO","doi":"10.1002/j.1551-8833.1965.tb01472.x","usgsCitation":"Robinove, C.J., 1965, Infrared photography and imagery in water resources research: Journal - American Water Works Association, v. 57, no. 7, p. 834-840, https://doi.org/10.1002/j.1551-8833.1965.tb01472.x.","productDescription":"7 p.","startPage":"834","endPage":"840","numberOfPages":"7","costCenters":[{"id":222,"text":"Earth Resources Observation and Science (EROS) Center","active":true,"usgs":true}],"links":[{"id":288445,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"57","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"539acc04e4b0e83db6d08f6f","contributors":{"authors":[{"text":"Robinove, Charles J.","contributorId":16983,"corporation":false,"usgs":true,"family":"Robinove","given":"Charles","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":494582,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221204,"text":"70221204 - 1965 - The drill‐stem test: The petroleum industry's deep‐well pumping test","interactions":[],"lastModifiedDate":"2021-06-04T21:44:46.914029","indexId":"70221204","displayToPublicDate":"1965-07-01T16:42:04","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"The drill‐stem test: The petroleum industry's deep‐well pumping test","docAbstract":"Drill‐stem tests provide the petroleum industry information on three critical properties of subsurface formations —pressure head, permeability, and water chemistry –that the ground‐water hydrologist also seeks in making pumping tests of water wells. As it is increasingly necessary to study the hydraulic and geochemical properties of deep‐lying rocks in order to understand the behavior of ground water, data on drill‐stem tests made by the petroleum industry become an important source of information which otherwise is unobtainable because of the high cost. Data from these tests made by methods currently in use are highly useful in water studies. An obvious conclusion is that both petroleum engineering and ground‐water hydrology stand to profit substantially from an increase in the interchange of ideas and techniques.
","language":"English","publisher":"Wiley Blackwell","doi":"10.1111/j.1745-6584.1965.tb01218.x","usgsCitation":"Bredehoeft, J., 1965, The drill‐stem test: The petroleum industry's deep‐well pumping test: Groundwater, v. 3, no. 3, p. 31-36, https://doi.org/10.1111/j.1745-6584.1965.tb01218.x.","productDescription":"6 p.","startPage":"31","endPage":"36","costCenters":[],"links":[{"id":386249,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"3","issue":"3","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Bredehoeft, J.D.","contributorId":12836,"corporation":false,"usgs":true,"family":"Bredehoeft","given":"J.D.","affiliations":[],"preferred":false,"id":817044,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221197,"text":"70221197 - 1965 - Natural controls involved in shallow aquifer contamination","interactions":[],"lastModifiedDate":"2021-06-04T21:03:19.909849","indexId":"70221197","displayToPublicDate":"1965-07-01T16:00:52","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Natural controls involved in shallow aquifer contamination","docAbstract":"Shallow aquifers, commonly the most important sources of ground water, are also those most susceptible to contamination. The mode of entry of contaminants to shallow aquifers is (1) directly, via wells or secondary openings in consolidated rocks, (2) percolation through the zone of aeration, (3) induced infiltration through the zone of saturation, and (4) interaquifer leakage or flow through open holes. Natural removal or degradation of contaminants is by filtration, dispersion, sorption, ion exchange, oxidation, and various biochemical processes. These phenomena are controlled by the physical environment, structure; mineralogy, and hydraulic characteristics of the earth materials contacted by the liquid wastes. When liquid wastes enter an aquifer directly, there is little or no natural treatment by filtration, sorption, or oxidation. Purification is only by those processes that operate within the aquifer under anaerobic conditions. Contaminants from natural sources that enter aquifers under saturated‐flow conditions are degraded primarily by dilution. The natural processes effective in reducing contamination from surface‐water sources depend on the hydraulic regimen involved, which vary with individual cases. Liquid wastes percolating through the zone of aeration are those most likely to be purified by natural environment processes. Natural processes, however, do not effectively remove or degrade all contaminants, especially some of the many highly stable compounds that have gained widespread use in recent years, such as synthetic detergents. Comprehensive interdisciplinary research into the ability of various earth materials to remove many types of contaminants under varying hydrologic conditions is needed.
","language":"English","publisher":"Wiley Blackwell","doi":"10.1111/j.1745-6584.1965.tb01219.x","usgsCitation":"Deutsch, M., 1965, Natural controls involved in shallow aquifer contamination: Groundwater, v. 3, no. 3, p. 37-40, https://doi.org/10.1111/j.1745-6584.1965.tb01219.x.","productDescription":"4 p.","startPage":"37","endPage":"40","costCenters":[],"links":[{"id":386242,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"3","issue":"3","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Deutsch, M.","contributorId":19707,"corporation":false,"usgs":true,"family":"Deutsch","given":"M.","email":"","affiliations":[],"preferred":false,"id":817035,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70207282,"text":"70207282 - 1965 - Relation of carbon 14 concentrations to saline water contamination of coastal aquifers","interactions":[],"lastModifiedDate":"2019-12-17T07:00:43","indexId":"70207282","displayToPublicDate":"1965-03-31T16:24:40","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3721,"text":"Water Resources Management","onlineIssn":"1573-1650","printIssn":"0920-4741","active":true,"publicationSubtype":{"id":10}},"title":"Relation of carbon 14 concentrations to saline water contamination of coastal aquifers","docAbstract":"Naturally occurring stable or radioactive isotopes may be used in some places to identify the origin of saline water that contaminates some coastal aquifers. In a recent study to determine the origin of saline water in the Ocala Limestone aquifer near Brunswick, Georgia, the following sources were analyzed for C14 and deuterium concentrations: potable water from the Ocala Limestone, contaminated water from the Ocala Limestone, saune water from the underlying Claiborne Group, and nearby ocean water. The chloride concentration of the groundwater ranges from about 25 ppm in the potable water to more than 2000 ppm in the deeper part of the Claiborne Group. From an interpretation of piezometric maps and other hydrologic data, previous investigators had concluded that the source of the contaminating water was the Claiborne Group and not the nearby ocean. The essentially uniform range of low values of −965 to −987‰ of the modern standard (National Bureau Standard C14 oxalic acid) for the C14 activity of the groundwater samples (regardless of the degree of contamination) is in agreement with this conclusion. If recent ocean water, which had a C14 value of +285‰, were the source of contamination, the contaminated water would have had a C14 activity higher than the activity of the fresh water. Deuterium analyses are not inconsistent with the interpretation that water from the Claiborne Group, rather than recent ocean water, is the source of the contaminating water. The concurrence of the hydrologic and the isotopic data in this area where the hydrology is well known suggests that isotopic analysis may be used to identify the origin of water in different portions of a hydrologic environment.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/WR001i001p00109","issn":"00431397","usgsCitation":"Hanshaw, B., Back, W., Rubin, M., and Wait, R.L., 1965, Relation of carbon 14 concentrations to saline water contamination of coastal aquifers: Water Resources Management, v. 1, no. 1, p. 109-114, https://doi.org/10.1029/WR001i001p00109.","productDescription":"6 p. ","startPage":"109","endPage":"114","costCenters":[],"links":[{"id":370289,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Georgia","county":"Glynn County","city":"Brunswick","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.73828125,\n 30.92107637538488\n ],\n [\n -81.221923828125,\n 30.92107637538488\n ],\n [\n -81.221923828125,\n 31.39115752282472\n ],\n [\n -81.73828125,\n 31.39115752282472\n ],\n [\n -81.73828125,\n 30.92107637538488\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"1","issue":"1","noUsgsAuthors":false,"publicationDate":"2010-07-09","publicationStatus":"PW","contributors":{"authors":[{"text":"Hanshaw, B.B.","contributorId":25928,"corporation":false,"usgs":true,"family":"Hanshaw","given":"B.B.","email":"","affiliations":[],"preferred":false,"id":777532,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Back, W.","contributorId":33839,"corporation":false,"usgs":true,"family":"Back","given":"W.","email":"","affiliations":[],"preferred":false,"id":777533,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rubin, Meyer","contributorId":107283,"corporation":false,"usgs":true,"family":"Rubin","given":"Meyer","email":"","affiliations":[],"preferred":false,"id":777690,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wait, Robert L.","contributorId":12839,"corporation":false,"usgs":true,"family":"Wait","given":"Robert","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":777691,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70199507,"text":"70199507 - 1965 - Mathematical models of catchment behavior","interactions":[],"lastModifiedDate":"2025-02-27T18:37:54.196925","indexId":"70199507","displayToPublicDate":"1965-01-01T16:01:10","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2550,"text":"Journal of the Hydraulics Division","active":true,"publicationSubtype":{"id":10}},"title":"Mathematical models of catchment behavior","docAbstract":"After an examination of trends in the modeling of hydrologic systems, a review of some recent studies is given. The authors' preliminary studies on the feasibility and efficiency of the automatic evaluation of catchment model parameters by use of a digital computer are described and some results presented.
","language":"English","publisher":"American Society of Civil Engineers","doi":"10.1061/JYCEAJ.0001271","usgsCitation":"Dawdy, D.R., and O’Donnell, T., 1965, Mathematical models of catchment behavior: Journal of the Hydraulics Division, v. 91, no. 4, p. 123-137, https://doi.org/10.1061/JYCEAJ.0001271.","productDescription":"15 p.","startPage":"123","endPage":"137","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"links":[{"id":357514,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"91","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Dawdy, David R.","contributorId":75125,"corporation":false,"usgs":true,"family":"Dawdy","given":"David","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":745630,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"O’Donnell, Terence","contributorId":208019,"corporation":false,"usgs":false,"family":"O’Donnell","given":"Terence","email":"","affiliations":[],"preferred":false,"id":745631,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70048263,"text":"70048263 - 1965 - Directional hydraulic behavior of a fractured-shale aquifer in New Jersey","interactions":[],"lastModifiedDate":"2021-02-17T22:57:35.415612","indexId":"70048263","displayToPublicDate":"1965-01-01T09:15:00","publicationYear":"1965","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Directional hydraulic behavior of a fractured-shale aquifer in New Jersey","docAbstract":"The principal source of ground water throughout a large part of central and northeastern New Jersey is the aquifer in the Brunswick Shale -- the youngest unity of the Newark Group of Triassic Age. Large-diameter public-supply and industrial wells tapping the Brunswick Shale commonly yield several hundred gallons per minute each. Virtually all ground water in this aquifer occurs in interconnecting fractures; the formation has practically no effective primary porosity. Numerous pumping tests have shown that the aquifer exhibits directional, rather than isotropic, hydraulic behavior. Water levels in wells alined along the strike of the formation show greater magnitude of interference than those in wells alined in transverse directions. Drawdown data evaluated by standard time-drawdown methods indicate computed coefficient of transmissibility in all cases is least in the direction of strike. Because of the distribution of observation wells available for the tests, distance-drawdown methods of evaluation could be used in only one instance -- for just one direction; the computed coefficient compared favorably with that calculated from the time-drawdown method. Computed values of transmissibility may be unreliable owing to the departure of the aquifer from the ideal model. It is even possible that the direction of minimum computed transmissiblity is actually indicative of the alinement of fractures with the greatest permeability. However, the relation of the directional behavior to the structure of the formation has practical significance when locating the new wells near existing wells. Well interference can be greatly minimized, generally, by alining wells perpendicular to the strike.","largerWorkTitle":"Proceedings of the international symposium on hydrology of fractured rocks","conferenceTitle":"International Symposium on Hydrology of Fractured Rocks","conferenceDate":"October 1965","conferenceLocation":"Dubrovnik, Croatia","language":"English","publisher":"International Association of Scientific Hydrology","usgsCitation":"Vecchioli, J., 1965, Directional hydraulic behavior of a fractured-shale aquifer in New Jersey, in Proceedings of the international symposium on hydrology of fractured rocks, Dubrovnik, Croatia, October 1965, 9 p.","productDescription":"9 p.","numberOfPages":"9","costCenters":[],"links":[{"id":277842,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Jersey","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -75.2082,40.2451 ], [ -75.2082,41.3574 ], [ -73.9931,41.3574 ], [ -73.9931,40.2451 ], [ -75.2082,40.2451 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"523c1ce6e4b024b60d4072a3","contributors":{"authors":[{"text":"Vecchioli, John","contributorId":36113,"corporation":false,"usgs":true,"family":"Vecchioli","given":"John","email":"","affiliations":[],"preferred":false,"id":484210,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70175593,"text":"70175593 - 1965 - Selected ground water data in the Eola-Amity Hills area, northern Willamette Valley, Oregon","interactions":[],"lastModifiedDate":"2016-08-17T12:04:25","indexId":"70175593","displayToPublicDate":"1965-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":115,"text":"Ground Water Report","active":false,"publicationSubtype":{"id":2}},"title":"Selected ground water data in the Eola-Amity Hills area, northern Willamette Valley, Oregon","docAbstract":"Occurrence, quality, and availability of ground water differ considerably from place to place in the Eola-Amity Hills area because of the highly diversified geologic and hydrologic conditions. A table relates the geologic situation to the availability of ground water for four areas--Eola-Amity Hills, east and west valley plains, and Willamette River flood plain. Tables show well and spring records, drillers' logs, and chemical analyses of ground water. The final interpretive report will be published by the U.S. Geological Survey.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, DC","usgsCitation":"Price, D., and Johnson, N.A., 1965, Selected ground water data in the Eola-Amity Hills area, northern Willamette Valley, Oregon: Ground Water Report.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":326670,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Oregon","otherGeospatial":"Willamette Valley","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57b58b58e4b03bcb0104bc68","contributors":{"authors":[{"text":"Price, Don","contributorId":30608,"corporation":false,"usgs":true,"family":"Price","given":"Don","email":"","affiliations":[],"preferred":false,"id":645787,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, Nyra A.","contributorId":173771,"corporation":false,"usgs":false,"family":"Johnson","given":"Nyra","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":645788,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70185670,"text":"70185670 - 1965 - Vigil Network sites: A sample of data for permanent filing","interactions":[],"lastModifiedDate":"2017-03-27T13:03:24","indexId":"70185670","displayToPublicDate":"1965-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5334,"text":"International Association of Scientific Hydrology - Bulletin ","onlineIssn":"2150-3435","printIssn":"0262-6667","active":false,"publicationSubtype":{"id":10}},"title":"Vigil Network sites: A sample of data for permanent filing","docAbstract":"The Vigil Network consists of places where observations are made through time to record changes in landscape features over a long period. Resurveys will usually be made once each year or every few years and the period of observation, hopefully, will extend through and beyond the International Hydrological Decade.
Vigil Network sites will usually be chosen to represent some typical feature of a given landscape. In the example shown here, the feature is a small ephemeral channel in a basin of moderate relief underlain by silty sandstone typical of the surrounding area. Vigil sites are not protected from man's influence and indeed may be selected because of the possible or portending cultural influences. In this respect they differ from the Bench Mark Network whose purpose is to make precise observations of hydrologic factors in areas uninfluenced by and protected from man's use.
The factors which might be observed are many and varied. A few might be mentioned here, others are explained at length elsewhere (Miller and Leopold, 1963; Leopold, 1962). Streamchannel position, form, depth, and profile; vegetation in form of transects or quadrats; soil movement on slopes; rock movement on slopes or in channels. These and many more would yield valuable information on changes with time.
To assure permanence of initial field observations, including reference points, bench marks, and cross sections, brief descriptions, maps, and initial data should be filed identically in designated repositories where the data will be made available for inspection by any interested scientist. It is recommended that the designation of two such locations where records of the type here attached will be filed be taken up by the Coordinating Council of the International Hydrological Decade. In designating such repositories it should be recognized that there is no need for elaborate indexing. The main requirement is merely the maintenance of a simple file where the data are stored and can be inspected or copied by any scientist. There need be no special provision for lending or reproduction services.
The present document is an example showing what data, maps, and descriptions should be included in those permanent files at the two repositories. The material in these repositories should be sufficient to permit someone in the indefinite future to find and remeasure the same features described now. Thus the scientific value of the original surveys increases with time, - provided that the descriptions are sufficient to allow a person to find with assurance the original feature in the field.
It must be visualized that a permanent repository must economize in space. Thus, as the example here shows, the filed material is not all of the original field notes but a summary, brief but descriptive.
","language":"English","publisher":"Taylor & Francis","doi":"10.1080/02626666509493401","usgsCitation":"Leopold, L.B., and Emmett, W.W., 1965, Vigil Network sites: A sample of data for permanent filing: International Association of Scientific Hydrology - Bulletin , v. 10, no. 3, p. 12-21, https://doi.org/10.1080/02626666509493401.","productDescription":"10 p.","startPage":"12","endPage":"21","costCenters":[],"links":[{"id":480681,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1080/02626666509493401","text":"Publisher Index Page"},{"id":338379,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"10","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"58da253fe4b0543bf7fda87d","contributors":{"authors":[{"text":"Leopold, Luna Bergere","contributorId":93884,"corporation":false,"usgs":true,"family":"Leopold","given":"Luna","email":"","middleInitial":"Bergere","affiliations":[],"preferred":false,"id":686308,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Emmett, William W.","contributorId":68715,"corporation":false,"usgs":true,"family":"Emmett","given":"William","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":686309,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1718,"text":"wsp1809I - 1965 - Ground-water pumpage and water-level changes in the Milwaukee-Waukesha area, Wisconsin, 1950-61","interactions":[],"lastModifiedDate":"2023-03-13T20:10:12.868331","indexId":"wsp1809I","displayToPublicDate":"1965-01-01T00:00:00","publicationYear":"1965","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":"1809","chapter":"I","title":"Ground-water pumpage and water-level changes in the Milwaukee-Waukesha area, Wisconsin, 1950-61","docAbstract":"Artesian water pressure in the deep sandstone aquifer continued to decline throughout most of the Milwaukee-Waukesha area, Wisconsin between 1950 and 1961. Areas of greatest water-level decline were in northeast Waukesha County and in northwest Milwaukee County. The chief cause of the decline was continued heavy pumpage. The major aquifers of southeastern Wisconsin are the Niagara aquifer, which is primarily Niagara Dolomite of Silurian age, and the sandstone aquifer, which consists of sandstones of Cambrian and Ordovician ages. Locally, the glacial sands and gravels ,of Pleistocene age also are important aquifers. In the Milwaukee-Waukesha area, the sandstone aquifer is completely artesian, confined above by the Maquoketa Shale. The Niagara aquifer is generally unconfined. Pumpage from the sandstone aquifer in the Milwaukee-Waukesha area de- creased from about 23.3 million gallons per day in 1950 to about 20.9 million gallons per day in 1961. The principal reason for decreased pumpage was sub- stitution of surface-water supply from Lake Michigan. Between 1950 and 1961, the water-level changes in wells in the sandstone aquifer ranged from plus 10 feet at Town of Lake to minus 98 feet in northwest Milwaukee. Except for a small area near Town of Lake, water levels in wells in the Milwaukee-Waukesha area were lower in 1961 than in 1950. Water-level changes were directly related to the pumpage pattern and pump- age changes. Increased pumpage at Waukesha and in northwest Milwaukee and continued heavy pumpage at Wauwatosa caused widespread water-level declines in northeast Waukesha County and in northwest Milwaukee County. Locally, decreased pumpage at West Milwaukee allowed limited recovery of water levels since 1957. Estimates of pumpage through the year 1975 indicate a pumpage decrease in the middle 1960's, followed by an increase in the late 1960's and early 1970's. Additional conversion to surface-water supply in Milwaukee County will account for most pumpage decreases. Increased pumpage is most likely in Waukesha County where the population is expanding rapidly and an adequate surface-water supply is not readily accessible. The westward shift of the pumpage pattern may cause an additional water-level decline of about 50 feet at Waukesha but will permit water levels to recover about 100 feet at West Allis by 1975. Partial or complete conversion to surface-water supplies by municipalities that depend entirely on water from the sandstone aquifer would allow greater use of the sandstone aquifer by isolated suburban developments and industries.
","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/wsp1809I","collaboration":"Prepared in cooperation with the University of Wisconsin, Geological and Natural History Survey","usgsCitation":"Green, J.H., and Hutchinson, R.D., 1965, Ground-water pumpage and water-level changes in the Milwaukee-Waukesha area, Wisconsin, 1950-61: U.S. Geological Survey Water Supply Paper 1809, Report: iii, 19 p. ; 2 Plates: 19.50 x 24.00 inches and 18.50 x 24.00 inches, https://doi.org/10.3133/wsp1809I.","productDescription":"Report: iii, 19 p. ; 2 Plates: 19.50 x 24.00 inches and 18.50 x 24.00 inches","numberOfPages":"23","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":26806,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809i/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":136940,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809i/report-thumb.jpg"},{"id":26805,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809i/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26804,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809i/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":414041,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25008.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Wisconsin","city":"Milwaukee, Waukesha","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -88.82011978710044,\n 43.6048598948214\n ],\n [\n -88.82011978710044,\n 42.619688745253114\n ],\n [\n -87.76500461016991,\n 42.619688745253114\n ],\n [\n -87.76500461016991,\n 43.6048598948214\n ],\n [\n -88.82011978710044,\n 43.6048598948214\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa8e4b07f02db6673ff","contributors":{"authors":[{"text":"Green, J. H.","contributorId":43312,"corporation":false,"usgs":true,"family":"Green","given":"J.","email":"","middleInitial":"H.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":144010,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hutchinson, R. D.","contributorId":99112,"corporation":false,"usgs":true,"family":"Hutchinson","given":"R.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":144011,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2897,"text":"wsp1811 - 1965 - Hydrology of the Little Plover River basin, Portage County, Wisconsin, and the effects of water resource development","interactions":[],"lastModifiedDate":"2023-04-13T20:54:27.826245","indexId":"wsp1811","displayToPublicDate":"1965-01-01T00:00:00","publicationYear":"1965","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":"1811","title":"Hydrology of the Little Plover River basin, Portage County, Wisconsin, and the effects of water resource development","docAbstract":"The Little Plover River basin is in the sand-plain area of central Wisconsin. The basin and the surrounding sand-plain area provide a good fish and wildlife habitat and is a popular locale for sport fishing. Good yields may be obtained in the area from irrigated crops, and the irrigated acreage has been increasing rapidly in recent years. Sportsmen and conservationists are concerned about the effects of increased development of the water resources on the streams as trout habitat. In the past, many political and legal conflicts among water users have arisen from erroneous opinions as to the behavior of water. Many of these conflicts would be diminished or eliminated if the participants were cognizant of fundamental hydrologic principles.
This study was made to demonstrate the extent and nature of the interrelation of ground water and surface water and the fundamental hydrologic principles governing water movement. The study was also made to determine the hydrologic changes that might occur following development, to provide information that might be used as a basis for planning water development, and for drafting legislation that recognizes the relation between ground water and surface water.
Water has been developed in the Little Plover River basin for industry, for domestic and stock supplies, and for irrigation. Irrigated acreage is increasing in the area, and the use of water for irrigation may alter the hydrology of the basin somewhat. About 4,000-4,500 acres of land within the basin, or 50-60 percent of the basin area, is suitable for irrigated farming, but probably no more than 2,500 acres will be under irrigation in any one year, unless present crop-rotation practices are changed.
Most of the Little Plover River basin is underlain by from 40 to 100 feet of glacial outwash consisting of highly permeable sand and gravel. The glacial outwash is the main aquifer in the area and is capable of yielding large quantities of water to wells. An aquifer test in the area indicated that the coefficient of transmissibility of the glacial outwash is about 140,000 gallons per day per foot. The specific yield of the outwash is about 20 percent, as determined from water-level and streamfiow data. Morainal deposits occur locally with the glacial outwash. These deposits transmit water readily and do not form barriers to ground water in the outwash. Relatively impermeable crystalline rocks underlie the glacial deposits, and a sandstone ridge of low permeability impedes the movement of ground water from the basin by underflow.
The glacial outwash and morainal deposits are recharged by infiltration of 9-10 inches of the 31 inches of precipitation that falls on the area in an average year. If it is not withdrawn by wells for consumptive use or by phreatophytes, water that infiltrates the sand and gravel discharges later into the Little Plover River. This ground-water discharge constitutes 90-95 percent of the total flow of the Little Plover River.
Annual evapotranspiration varies considerably, but generally ranges from 2 to 8 inches less than the potential evapotranspiration of 24 inches. Consumptive use of irrigation water averages about 4 inches per year. Most of the water pumped from wells otherwise would be discharged to the stream, and consumptive use of irrigation water will deplete streamflow by the amount of evapotranspiration.
Pumping wells have little effect on the water level in the highly permeable sand and gravel. Significant interference between wells would occur only if large capacity wells were within a few tens of feet of each other.
Ground water and surface water are closely interrelated in the sand-plain area and ground-water withdrawals near the Little Plover River may cause a measurable streamflow depletion. In a test, a well that was pumping about 1,120 gpm (gallons per minute) and that was 300 feet from the stream derived about 30 percent of its flow from the stream after 3 days of pumping.
For this study, the effects of increased ground-water development were evaluated from a hypothetical development schedule, for which it was assumed that 500 acres were irrigated the first year and that an additional 50 acres were irrigated in each succeeding year for 10 years. It also was assumed that the average annual consumptive-use requirement for irrigation water would be one- third of an acre-foot per acre. Calculations indicate that the maximum monthly rate of depletion due to the consumptive use of 4 inches of ground water per year on 500 acres would be about 0.4 cfs (cubic feet per second) the first year and 0.5 cfs after 10 years of pumping. Other computations indicate that the maximum monthly rate of depletion due to irrigating 500 acres the first year and 50 additional acres each year for 10 years would be about 0.8 cfs. Maximum depletion would occur during the summer months, concurrent with the irrigation withdrawals.
Because of the close interrelation between ground and surface water, surface- water withdrawals will cause an increased inflow of ground water to the stream and a decline in ground-water levels near the stream. These effects were demonstrated by pumping from the stream. After 29 hours of pumping, a depletion of 1,120 gpm at a site 7,000 feet downstream was about 200 gpm less than the diversion at the pump. Most of the 200 gpm was supplied from the stream-banks, and ground-water levels near the stream declined as much as 0.3 foot. Computations indicated that ground-water inflow, following a streamflow diver- sion that lowered the stage 0.15 foot, would be 0.14 cfs after 5 days and 0.06 cfs after 30 days.
The demonstration of the quantitative relation between ground water and surface water, as given by this study, should provide a sound basis for planning water development to minimize conflicts of interest. The demonstrations also should provide a basis for drafting legislation that recognizes the interrelation of ground water and surface water.
Because the geology and the hydrology are relatively uniform throughout the sand plains, many of the methods and hydrologic values determined for this detailed study of the Little Plover River basin may be applied to other basins in the sand-plain area.
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The fresh ground water represents recharge localized, during infrequent, torrential rain storms, in areas of concentrated runoff where sediments in the vadose zone are moderately permeable and depth to the water table is generally less than a hundred feet. Concentration of runoff appears to be the primary control in the localization of recharge. The fresh water percolates downward to the ground-water reservoir following rare storms, then flows in the direction of hydraulic gradient and gradually becomes brackish.
Theoretical delineation of the recharge area and ground-water flow pattern in Rawdatain was confirmed by tritium and C14 dating of the water.
Brackish ground-water conditions prevail from water table downward in areas where rainfall infiltrates essentially where it falls, permeability of sediments in the vadose zone is low, or the water table is several hundred feet below land surface. In these areas, rainfall is retained and lost within the soil zone or becomes mineralized during deep percolation.
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