{"pageNumber":"1628","pageRowStart":"40675","pageSize":"25","recordCount":41062,"records":[{"id":32796,"text":"pp372D - 1963 - Effects of drought in the Rio Grande basin: Chapter D in Drought in the Southwest, 1942-56","interactions":[],"lastModifiedDate":"2017-02-22T16:01:54","indexId":"pp372D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"372","chapter":"D","title":"Effects of drought in the Rio Grande basin: Chapter D in Drought in the Southwest, 1942-56","docAbstract":"

In headwater areas of the Rio Grande and its principal tributaries, variations in streamflow and in ground-water storage and discharge depend upon fluctuations in precipitation, with modifications by geologic factors and by the pattern of water development and use. In downstream areas the surfaceand ground-water resources are replenished not only by local precipitation but also by outflow from the headwaters areas; thus the effects of drought upon those water resources are complex and may be vague and indeterminate.

","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Drought in the Southwest, 1942-56 (Professional Paper 372)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp372D","usgsCitation":"Thomas, H.E., 1963, Effects of drought in the Rio Grande basin: Chapter D in Drought in the Southwest, 1942-56: U.S. Geological Survey Professional Paper 372, iii, 59 p., https://doi.org/10.3133/pp372D.","productDescription":"iii, 59 p.","numberOfPages":"63","costCenters":[],"links":[{"id":336022,"rank":9,"type":{"id":22,"text":"Related Work"},"url":"https://pubs.usgs.gov/publication/pp372H","text":"Chapter H: General summary of effects of the drought in the Southwest"},{"id":336021,"rank":8,"type":{"id":22,"text":"Related Work"},"url":"https://pubs.usgs.gov/publication/pp372G","text":"Chapter G: Effects of drought along Pacific Coast in California"},{"id":336020,"rank":7,"type":{"id":22,"text":"Related Work"},"url":"https://pubs.usgs.gov/publication/pp372F","text":"Chapter F: Effects of drought in the Colorado River basin"},{"id":336019,"rank":6,"type":{"id":22,"text":"Related Work"},"url":"https://pubs.usgs.gov/publication/pp372E","text":"Chapter E: Effects of drought in basins of interior drainage"},{"id":336018,"rank":5,"type":{"id":22,"text":"Related Work"},"url":"https://pubs.usgs.gov/publication/pp372C","text":"Chapter C: Effects of drought in central and south Texas"},{"id":336017,"rank":4,"type":{"id":22,"text":"Related Work"},"url":"https://pubs.usgs.gov/publication/pp372B","text":"Chapter B: General effects of drought on water resources of the Southwest"},{"id":336016,"rank":3,"type":{"id":22,"text":"Related Work"},"url":"https://pubs.usgs.gov/publication/pp372A","text":"Chapter A: The meteorologic phenomenon of drought in the 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E.","contributorId":12829,"corporation":false,"usgs":true,"family":"Thomas","given":"H.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":209192,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":32728,"text":"pp444 - 1963 - Geology of Mount Rainier National Park, Washington","interactions":[],"lastModifiedDate":"2012-02-02T00:09:10","indexId":"pp444","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"444","title":"Geology of Mount Rainier National Park, Washington","docAbstract":"Mount Rainier National Park includes 378 square miles of \r\nrugged terrain on the west slope of the Cascade Mountains \r\nin central Washington. Its mast imposing topographic and geologic feature is glacier-clad Mount Rainier. This volcano, \r\ncomposed chiefly of flows of pyroxene andesite, was built upon \r\nalt earlier mountainous surface, carved from altered volcanic \r\nand sedimentary rocks invaded by plutonic and hypabyssal \r\nigneous rocks of great complexity. \r\nThe oldest rocks in the park area are those that make up \r\nthe Olmnapecosh Formation of late Eocene age. This formation \r\nis more than 10,000 feet thick, and consists almost entirely of \r\nvolcanic debris. It includes some lensoid accumulations of \r\nlava and coarse mudflows, heaped around volcanic centers., but \r\nthese are surrounded by vastly greater volumes of volcanic \r\nclastic rocks, in which beds of unstratified coarse tuff-breccia, \r\nabout 30 feet in average thickness, alternate with thin-bedded \r\nbreccias, sandstones, and siltstones composed entirely of volcanic debris. The coarser tuff-breccias were probably deposited \r\nfrom subaqueous volcanic mudflows generated when eruption \r\nclouds were discharged directly into water, or when subaerial \r\nash flows and mudflows entered bodies of water. The less \r\nmobile mudflows and viscous lavas built islands surrounded \r\nby this sea of thinner bedded water-laid clastics. In compostion the lava flows and coarse lava fragments of the \r\nOhanapecosh Formation are mostly andesite, but they include \r\nless abundant dacite, basalt, and rhyolite. \r\nThe Ohanapecosh Formation was folded, regionally altered \r\nto minerals characteristic of the zeolite facies of metamorphism, uplifted, and deeply eroded before the overlying Stevens \r\nRidge Formation of Oligocene or early Miocene age was deposited upon it. The Stevens Ridge rocks, which are about \r\n3,000 feet in maximum total thickness, consist mainly of massive \r\nash flows. These are now devitrified and altered, but they \r\noriginally consisted of rhyodacite pumice lapilli and glass \r\nshards, which compacted and welded into thick massive units \r\nduring emplacement and cooling. Subordinate water-laid clastic rocks occur t(ward the top of the formation, and thin-bedded \r\npyroclastic layers occur between some of the ash flows. \r\nExposures on Backbone Ridge and on Carbon River below \r\nthe mouth of Cataract Creek show that in places the thick \r\nbasal Stevens Ridge ash flows swept with great violence over \r\nan old erosion surface developed on rocks of the Ohanapecosh \r\nFormation. Masses of mud, tree trunks, and other surface \r\ndebris were swirled upward into the base of the lowermost ash \r\nfiery, and lobes and tongues of hot ash were forced downward \r\ninto. the saprolitic mud. \r\nThe Stevens Ridge Formation is concordantly overlain by the Fifes Peak Formation of probable early Miocene age, which consists of lava flows, subordinate mudflows, and minor quantities of tuffaceous clastic rocks. The lavas are predominantly olivine basalt and basaltic andesite, but they include a little rhyolite. They are slightly to moderately altered: the ferromagnesian phenocrysts are generally replaced by saponite, chiprite, or carbonate ; the glass is devitrified ; and the rocks are locally permeated by veinlets of zeolite. Swarms of diabase sills and dikes are probably intrusive equivalents of the Fifes Peak lavas. \r\n\r\nThe upper part of the Fifes Peak Formation has been mostly eroded from Mount Rainier National Park, but farther north, in the Cedar Lake quadrangle, it attains a thickness of more than 5,000 feet. \r\n\r\nThe Fifes Peak and earlier formations were gently folded, faulted, uplifted, and eroded before the. late Miocene Tatoosh pluton worked its way upward to shallow depths and eventually broke through to the surface. The rise of the pluton was accompanied by .the injection of a complicated melange of satellitic stocks, sills, and dikes. A favored horizon for intrusion of sills was along or near the unconfo","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/pp444","usgsCitation":"Fiske, R.S., Hopson, C.A., and Waters, A.C., 1963, Geology of Mount Rainier National Park, Washington: U.S. Geological Survey Professional Paper 444, 93 p., https://doi.org/10.3133/pp444.","productDescription":"93 p.","costCenters":[],"links":[{"id":108388,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13187.htm","linkFileType":{"id":5,"text":"html"},"description":"13187"},{"id":121420,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0444/report-thumb.jpg"},{"id":60650,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0444/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":264626,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0444/plate-1.pdf","size":"21630","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db684242","contributors":{"authors":[{"text":"Fiske, Richard S.","contributorId":17984,"corporation":false,"usgs":true,"family":"Fiske","given":"Richard","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":209044,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hopson, Clifford Andrae","contributorId":16468,"corporation":false,"usgs":true,"family":"Hopson","given":"Clifford","email":"","middleInitial":"Andrae","affiliations":[],"preferred":false,"id":209043,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Waters, Aaron Clement","contributorId":8081,"corporation":false,"usgs":true,"family":"Waters","given":"Aaron","email":"","middleInitial":"Clement","affiliations":[],"preferred":false,"id":209042,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1111,"text":"wsp1577 - 1963 - Ground-water geology and pump irrigation in Frenchman Creek Basin above Palisade, Nebraska","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1577","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1577","title":"Ground-water geology and pump irrigation in Frenchman Creek Basin above Palisade, Nebraska","docAbstract":"This report describes the geography, geology, and ground-water resources of that part of the Frenchman Creek basin upstream from Palisade, Nebr., an area of about 4,900 square miles. The basin includes all of Phillips County, Colo., and Chase County, Nebr., and parts of Logan, Sedgwick, Washington, and Yuma Counties, Colo., and Dundy, Hayes, Hitchcock, and Perkins Counties, Nebr. The land surface ranges from nearly flat to rolling; choppy hills and interdune saddles are common in the areas of dune sand, and steep bluffs and gullies cut the edges of the relatively flat loess plateaus. Most of the basin is drained by tributaries of Frenchman Creek, but parts of the sandhills are undrained. Farming and livestock raising are the principal industries. Irrigation with ground water has expanded rapidly since 1934. \r\n\r\nThe rocks exposed in the basin are largely unconsolidated and range in age from Pliocene to Recent. They comprise the Ogallala formation (Pliocene), the Sanborn formation (Pleistocene and Recent?), dune sand (Pleistocene and Recent), and alluvium (Recent). The rocks underlying the Ogallala are the Pierre shale (Late Cretaceous) and the White River group (Oligocene). The Pierre shale is relatively impermeable and yields little or no water to wells. The White River group also is relatively impermeable and yields little or no water to wells; however, small to moderate quantities of water possibly may be obtained from wells that penetrate fractured or 'porous' zones in the upper part of the White River group or permeable channel deposits within the group. The Ogallala formation is the main aquifer in the basin and yields moderate to large quantities of water to wells. The Sanborn formation and the dune sand generally lie above the water table, but in areas of high water table the dune sand yields small quantities of water to wells for domestic and stock supplies. The alluvium, which includes the low terrace deposits bordering the major streams, yields small to large quantities of water to wells. \r\n\r\nThe ground-water reservoir is recharged only from precipitation on the basin. Of the average annual precipitation of 19.5 inches, about 0.9 inch infiltrates to the water table, thereby contributing about 220,000 acre-feet of water annually to the ground-water reservoir. About 81 million acre-feet of water that could drain under gravity, and thus theoretically is available to wells, is held in groundwater storage in the basin. Water is discharged from the ground-water reservoir by wells, evaporation and transpiration, springs, seepage into streams, and movement into adjacent areas to the east and southeast. Most of the domestic, stock, and irrigation water supplies and all the public supplies are pumped from wells.\r\n\r\nDuring 1953, 96 wells were used to irrigate 10,000 acres of land with 19,000 acre-feet of water. About 34,000 acre-feet of water is evaporated and transpired annually in the valleys of the main streams and in areas of shallow water table in the sandhills. \r\n\r\nFrom the projection of base-flow measurements made during 1952, it was estimated that the average annual flow of Frenchman Creek into the reservoir above Enders Dam is about 57,000 acre-feet. By similar determinations, the average annual flow of Frenchman Creek at the gaging station at Palisade, Nebr., about 22 miles downstream from Enders Dam, is about 76,000 acre-feet, and the flow of Stinking Water Creek at the gaging station near Palisade is about 22,000 acre-feet. The combined flow of Frenchman and Stinking Water Creeks at their confluence near Palisade thus is about 98,000 acre-feet per year. About 90,000 acre-feet of ground water is estimated to move eastward each year across the Colorado-Nebraska State line within the basin. \r\n\r\nAdditional irrigation wells that will tap the Ogallala formation and the alluvium in the major valleys undoubtedly will be drilled. On the basis of current estimates of future irrigation.withdrawals, it is concluded that by the ","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1577","usgsCitation":"Cardwell, W.D., and Jenkins, E., 1963, Ground-water geology and pump irrigation in Frenchman Creek Basin above Palisade, Nebraska: U.S. Geological Survey Water Supply Paper 1577, vii, 472 p. :illus., diagrs., maps ;24 cm., https://doi.org/10.3133/wsp1577.","productDescription":"vii, 472 p. :illus., diagrs., maps ;24 cm.","costCenters":[],"links":[{"id":109991,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24763.htm","linkFileType":{"id":5,"text":"html"},"description":"24763"},{"id":138010,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1577/report-thumb.jpg"},{"id":25858,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25859,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25860,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25861,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25862,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25863,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25864,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25865,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25866,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25867,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25868,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1577/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668e74","contributors":{"authors":[{"text":"Cardwell, W. D. E.","contributorId":69120,"corporation":false,"usgs":true,"family":"Cardwell","given":"W.","email":"","middleInitial":"D. E.","affiliations":[],"preferred":false,"id":143195,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jenkins, Edward D.","contributorId":17972,"corporation":false,"usgs":true,"family":"Jenkins","given":"Edward D.","affiliations":[],"preferred":false,"id":143194,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":32743,"text":"pp379 - 1963 - Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups","interactions":[],"lastModifiedDate":"2022-03-29T21:42:36.762876","indexId":"pp379","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"379","title":"Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups","docAbstract":"

The Elmira-Williamsport region, lying south of the Finger Lakes in central New York and northern Pennsylvania, is part of the Appalachian Plateaus physiographic province. A small segment of the Valley and Ridge province is included near the south border. In 1953 and 1954, the authors, a geologist and a soil scientist, made a reconnaissance of about 5,000 square miles extending southward from the Finger Lakes, N.Y., to Williamsport, Pa., and eastward from Wellsboro, Pa., to Towanda, Pa. Glacial drift of Wisconsin age, covering the central and most of the northern parts of the region, belongs to the Olean substage of MacClintock and Apfel. This drift is thin and patchy, is composed of the relatively soft sandstones, siltstone, shales, and conglomerates of the plateaus, commonly has a low calcium carbonate content, and is deeply leached. Mantling its surface are extensive rubbly colluvial deposits. No conspicuous terminal moraine marks the relatively straight border of Olean drift. The Valley Heads moraine of Fairchild near the south ends of the Finger Lakes is composed of relatively thick drift containing a considerable amount of somewhat resistant sedimentary and crystalline rocks. Commonly this drift has a relatively high carbonate content and is leached to only shallow depths. The Valley Heads drift is younger than Olean, but its precise age is undetermined. The age of the Olean is perhaps between Sangamon and Farmdale, on the basis of, in part, a carbon-14 date from peat at Otto, N.Y. All differences in soil development on these two Wisconsin drifts are clearly related to the lithology of the parent material or the drainage, rather than to weathering differing in kind or in duration. The authors believe that the soils are relatively young, are in equilibrium with the present environment, and contain few, if any, features acquired during past weathering intervals. The effect of tree throw on soil profiles and the presence of soils on slopes clearly indicate that soils form rapidly. Sols Bruns Acides are the most extensive great soil group occurring throughout the region. Podzols and Gray-Brown Podzolic soils are also widespread, and on long, smooth slopes Low Humic-Gley soils are common. Organic soils are of small extent. South of the Wisconsin drift border, the surficial mantle consists chiefly of alluvial, colluvial, or residual deposits of Wisconsin or of Recent age, but there are many small isolated patches of older, strongly weathered materials of pre-Wisconsin age. Although such older materials are commonly overlain or mixed with less weathered mantle, the yellowish-red color, characteristic of the strongly weathered material, is generally not masked. Some of the older material is drift, presumed to be of Illionian age, that was probably strongly weathered to a considerable depth in Sangamon time and has been greatly eroded since the last interglacial period. No clear-cut exposure of Wisconsin drift resting on older drift or other strongly weathered mantle has been found. The old drift and the other strongly weathered materials apparently acquired their present red color in pre-Wisconsin time. Where exposed at the surface, such strongly weathered mantle is the parent material of modern Red-Yellow Podzolic soils. Sols Bruns Acides and Gray-Brown Podzolic soils, developed on slightly weathered parent materials, are found adjacent to these red soils. This suggests that these Red-Yellow Podzolic soils probably developed from strongly weathered parent materials. No buried soils were found nor were any soils recognized as relics from pre-Wisconsin time. Comparison of a map of the great soil groups with a map of the vegetation of the region, prepared by John C. Goodlett, does not reveal a close relation. Laboratory analyses of samples collected furnish data on textural, mineralogical, and chemical changes caused by weathering and soil formation. The results indicate that the amount of chemical weathering which the Wisconsin drift has undergone is slight. The Red-Yellow Podzolic soils on strongly weathered pre-Wisconsin drift have B2 horizons that have a finer texture than the A2 or C horizons. The parent materials of these soils seem to be strongly weathered because of the high chromas, reddish hues, friable condition of most rock fragments, relatively high kaolinite content, and presence of gibbsite in the clay fraction. Measurements at numerous localities show that the depth of leaching increases with decreasing carbonate content and is not a criterion of the age of the drift. Pebble counts of gravels also show that the depth of leaching of gravel is related to its limestone content. The location of the gravel deposits is probably due primarily to the presence of pebbles of resistant rock rather than to ice wastage involving abundant glacial melt water. The region is in the Susquehanna drainage basin except for its north fringe, which drains to Lake Ontario. Most of the region is a dissected plateau ranging in altitude from 700 to 2,500 feet and underlain by gently folded sedimentary rocks of Paleozoic age. Much of the region slopes moderately or steeply; the most extensive areas of gently sloping land are 011 the uplands. In the northern part are several straight and deep valleys the southern extension of the Finger Lakes basins separated by uplands with several low cuestas that face north. Similarly, some streams such as the Canisteo, Cohocton, and Chemung Rivers, and the part of the Susquehanna River that is in New York, trend at right angles to the Finger Lakes, flowing in valleys that parallel the regional strike of the bedrock. The Olean drift border is marked by a change from drift containing very few rounded or striated rock fragments to a mantle containing only angular rock fragments and traces of red, strongly weathered materials. A reconstruction of the surface of the ice sheet, at its maximum extent shows an inferred slope of its distal margin ranging from 100 to 500 feet per mile

","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp379","usgsCitation":"Denny, C.S., Lyford, W.H., and Goodlett, J.C., 1963, Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups: U.S. Geological Survey Professional Paper 379, Report: iv, 59 p.; 6 Plates: 41.94 × 24.00 inches or smaller, https://doi.org/10.3133/pp379.","productDescription":"Report: iv, 59 p.; 6 Plates: 41.94 × 24.00 inches or smaller","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":60663,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60662,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60661,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60660,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60659,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60664,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60665,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0379/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397823,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4377.htm"},{"id":121752,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0379/report-thumb.jpg"}],"scale":"250000","country":"United States","state":"New York, Pennsylvania","otherGeospatial":"Elmira-Williamsport region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.5,\n 41.1667\n ],\n [\n -76.25,\n 41.1667\n ],\n [\n -76.25,\n 42.5\n ],\n [\n -77.5,\n 42.5\n ],\n [\n -77.5,\n 41.1667\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae2e4b07f02db688b83","contributors":{"authors":[{"text":"Denny, Charles Storrow","contributorId":86331,"corporation":false,"usgs":true,"family":"Denny","given":"Charles","email":"","middleInitial":"Storrow","affiliations":[],"preferred":false,"id":209081,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lyford, Walter Henry","contributorId":43824,"corporation":false,"usgs":true,"family":"Lyford","given":"Walter","email":"","middleInitial":"Henry","affiliations":[],"preferred":false,"id":209080,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Goodlett, J. C.","contributorId":98771,"corporation":false,"usgs":true,"family":"Goodlett","given":"J.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":209082,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":57724,"text":"ofr63147 - 1963 - Tests of crest-stage gage intakes","interactions":[],"lastModifiedDate":"2026-01-26T16:54:15.528383","indexId":"ofr63147","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"63-147","title":"Tests of crest-stage gage intakes","docAbstract":"

Various types of c rest-stage gages have been used by the Geological Survey. Most installations consist of a vertically mounted metal pipe, a wooden rod, an intake device, and a small amount of granulated cork. These gages are placed where elevations of flood crests are desired. Water rising and then falling in the gage leaves a high-water mark of granulated cork on the wooden rod. The elevation of this mark can be determined at a date subsequent to the date of the crest.

It has been found that the high-water mark left on the rod may not represent the true elevation of the flood crest in the stream at the gage site. The difference between the true elevation of the crest at the gage and the recorded elevation will be designated drawdown if the recorded elevation is less than the true elevation, or pileup if the recorded elevation is greater than the true elevation. Tests of drawdown and pileup effects have been made in the past by Survey personnel and others. (See p. 8.) These investigations have sometimes brought forth conflicting results, probably due to the varied conditions under which the gages were tested.

The purpose of this investigation was (1) to determine the pileup and drawdown characteristics of the intakes now being used by the Survey and (2) to design a better intake if existing models were found unsuitable. It was further prescribed that any new design that might result should be easily fabricated from standard pipe fittings, and should be unaffected by pileup or drawdown in excess of 0.1 foot for velocities up to about 8 feet per second.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr63147","usgsCitation":"Carter, J.R., and Gamble, C.R., 1963, Tests of crest-stage gage intakes: U.S. Geological Survey Open-File Report 63-147, 10 p., https://doi.org/10.3133/ofr63147.","productDescription":"10 p.","numberOfPages":"10","costCenters":[],"links":[{"id":499023,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1963/0147/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":184244,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1963/0147/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad7e4b07f02db6845d0","contributors":{"authors":[{"text":"Carter, Jack R.","contributorId":71632,"corporation":false,"usgs":true,"family":"Carter","given":"Jack","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":257644,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gamble, Charles R.","contributorId":6822,"corporation":false,"usgs":true,"family":"Gamble","given":"Charles","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":257643,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":64960,"text":"i331 - 1963 - Preliminary glacial map of North Dakota","interactions":[],"lastModifiedDate":"2022-04-12T18:13:19.871184","indexId":"i331","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":320,"text":"IMAP","code":"I","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"331","title":"Preliminary glacial map of North Dakota","docAbstract":"

Data used for map compilation based in part upon maps listed below with modifications by the authors.  Data for remaining areas from aerial photographs and reconnaissance studies by the authors.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/i331","usgsCitation":"Colton, R.B., Lemke, R.W., and Lindvall, R.M., 1963, Preliminary glacial map of North Dakota: U.S. Geological Survey IMAP 331, 1 Plate: 57.64 x 36.26 inches, https://doi.org/10.3133/i331.","productDescription":"1 Plate: 57.64 x 36.26 inches","costCenters":[],"links":[{"id":189317,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/imap/0331/report-thumb.jpg"},{"id":360513,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/imap/0331/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":398560,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_1676.htm"}],"scale":"500000","country":"United States","state":"North 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Dakota\",\"nation\":\"USA \"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abce4b07f02db673477","contributors":{"authors":[{"text":"Colton, R. B.","contributorId":40186,"corporation":false,"usgs":true,"family":"Colton","given":"R.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":272423,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lemke, R. W.","contributorId":92319,"corporation":false,"usgs":true,"family":"Lemke","given":"R.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":272425,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lindvall, R. M.","contributorId":53797,"corporation":false,"usgs":true,"family":"Lindvall","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":272424,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":959,"text":"wsp1588 - 1963 - Ground-water geology of Bexar County, Texas","interactions":[],"lastModifiedDate":"2016-08-22T10:56:34","indexId":"wsp1588","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1588","title":"Ground-water geology of Bexar County, Texas","docAbstract":"

The investigation in Bexar County was part of a comprehensive study of a large area in south-central Texas underlain by the Edwards and associated limestones (Comanche Peak and Georgetown) of Cretaceous age. The limestones form an aquifer which supplies water to the city of San Antonio, several military installations, many industrial plants, and many irrigated farms.

\n

The geologic formations that yield water to wells in Bexar County are sedimentary rocks of Mesozoic and Cenozoic age. The rocks strike northeastward and dip southeastward toward the Gulf of Mexico. In the northern part of the county, in an erosional remnant of the Edwards Plateau, the rocks are nearly flat and free from faulting. In the central and southern parts of the county, however, the rocks dip gulfward at gentle to moderately steep angles and are extensively faulted in the Balcones and Mexia fault zones. Individual faults or shatter zones were traced as much as 25 miles; the maximum displacement is at least 600 feet. In general, the formations are either monoclinal or slightly folded; in the western part of the county the broad Culebra anticline plunges southwestward.

\n

Most of the large-capacity wells in Bexar County draw water from the Edwards and associated limestones, but a few draw from the Glen Rose limestone, the Austin chalk, and surficial sand and gravel. The Hosston formation, Glen Rose limestone, Buda limestone, and Austin chalk, all of Cretaceous age, generally yield small to large supplies of water; the Wilcox group and Carrizo sand of Tertiary age yield moderate supplies and alluvium of Pleistocene and Recent age generally yield small supplies.

\n

The Edwards and associated limestones are recharged primarily by groundwater underflow into Bexar County from the west, and secondarily by seepage from streams that cross the outcrop of the aquifer in Bexar County. During the period 1934-47 the recharge to the aquifer in Bexar County is estimated to have averaged between 400,000 and 430,000 acre-feet per year.

\n

Discharge from the aquifer takes place by means of wells and springs and by underflow into Comal and Guadalupe Counties on the northeast. During the period 1934-47 the estimated average discharge from wells and springs was about 174,000 acre-feet per year. The discharge by underflow out of the county during the same period is estimated to have averaged between 220,000 and 260,000 acre-feet per year. Probably only a small amount of water moves downdip southeast of San Antonio. The presence of highly mineralized water in that area suggests that the circulation of water is poor because of the low permeability of the aquifer.

\n

During the period 1934-56 the discharge from the Edwards and associated limestones greatly exceeded the recharge; consequently, water levels in wells declined. The decline was greatest in the northwestern part of the county, where the water levels in wells dropped as much as 100 feet. The decline was progressively less toward the east, averaging 40 feet along the Bexar-Comal County line. The area of the greatest concentration of discharge, which includes San Antonio and extends to the southwest and northeast, coincides with the area of maximum faulting and maximum recorded yields from wells and is not the area of greatest decline. The ability of the Edwards and associated limestones to transmit and store water in the San Antonio area apparently is so great that the discharge from wells results in much smaller declines of water level than do similar or even smaller discharges in other areas.

\n

The water from the Edwards is almost uniformly a calcium bicarbonate water of good quality, although hard. In the southern part of the San Antonio area the water is charged with hydrogen sulfide; farther downdip it becomes highly mineralized.

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1588","usgsCitation":"Arnow, T., 1963, Ground-water geology of Bexar County, Texas: U.S. Geological Survey Water Supply Paper 1588, Report: v, 36 p.; 12 Plates, https://doi.org/10.3133/wsp1588.","productDescription":"Report: v, 36 p.; 12 Plates","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":25489,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25490,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25491,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25492,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25493,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25494,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1588/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109993,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24774.htm","linkFileType":{"id":5,"text":"html"},"description":"24774"},{"id":137509,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1588/report-thumb.jpg"},{"id":25482,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25483,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25484,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25485,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25486,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25487,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25488,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668dc9","contributors":{"authors":[{"text":"Arnow, Ted","contributorId":84733,"corporation":false,"usgs":true,"family":"Arnow","given":"Ted","affiliations":[],"preferred":false,"id":142918,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2744,"text":"wsp1536H - 1963 - Electric analog of three-dimensional flow to wells and its application to unconfined aquifers","interactions":[],"lastModifiedDate":"2012-02-02T00:05:34","indexId":"wsp1536H","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1536","chapter":"H","title":"Electric analog of three-dimensional flow to wells and its application to unconfined aquifers","docAbstract":"Electric-analog design criteria are established from the differential equations of ground-water flow for analyzing pumping-test data. A convenient analog design was obtained by transforming the cylindrical equation of flow to a rectilinear form. The design criteria were applied in the construction of an electric analog, which was used for studying pumping-test data collected near Grand Island, Nebr. \r\n\r\nData analysis indicated (1) vertical flow components near pumping wells in unconfined aquifers may be much more significant in the control of water-table decline than radial flow components for as much as a day of pumping; (2) the specific yield during the first few minutes of pumping appears to be a very small fraction of that observed after pumping for more than 1 day; and (3) estimates of specific yield made from model studies seem much more sensitive to variations in assumed flow conditions than are estimates of permeability. Analysis of pumping-test data where vertical flow components are important requires that the degree of anisotropy be known. A procedure for computing anisotropy directly from drawdowns observed at five points was developed. Results obtained in the analog study emphasize the futility of calculating unconfined aquifer properties from pumping tests of short duration by means of equations based on the assumptions that vertical flow components are negligible and specific yield is constant.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1536H","usgsCitation":"Stallman, R., 1963, Electric analog of three-dimensional flow to wells and its application to unconfined aquifers: U.S. Geological Survey Water Supply Paper 1536, iv, 37 p. :ill. ;23 cm., https://doi.org/10.3133/wsp1536H.","productDescription":"iv, 37 p. :ill. ;23 cm.","costCenters":[],"links":[{"id":139040,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1536h/report-thumb.jpg"},{"id":29170,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1536h/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a25e4b07f02db60ede1","contributors":{"authors":[{"text":"Stallman, Robert W.","contributorId":32903,"corporation":false,"usgs":true,"family":"Stallman","given":"Robert W.","affiliations":[],"preferred":false,"id":145698,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2044,"text":"wsp1606 - 1963 - Geology and ground-water resources of Montgomery County, Alabama","interactions":[],"lastModifiedDate":"2022-02-02T15:02:35.456462","indexId":"wsp1606","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1606","title":"Geology and ground-water resources of Montgomery County, Alabama","docAbstract":"

Montgomery County includes an area of 790 square miles in east-central Alabama. The economy of Montgomery County is related primarily to the growing and processing of agricultural products.

The county is in the northern part of the Coastal Plain. It consists of parts of four divisions of the Coastal Plain: the terraces, the Black Prairie, the Chunnennuggee Hills, and the flood plains. The county drains north and northwest into the Alabama and Tallapoosa Rivers, except for a small area in the southern part of the county that is drained by tributaries of the Conecuh River.

Sedimentary rocks of Late Cretaceous age underlie Montgomery County. They are divided, in ascending order, into the following: Coker and Gordo formations of the Tuscaloosa group; Eutaw formation; and Mooreville and Demopolis chalks, Ripley formation, Prairie Bluff chalk, and Providence sand of the Selma group. The Clayton formation of Tertiary age crops out in a small area in the southern part of the county. Pleistocene terrace deposits of the ancestral Alabama River overlie the older rocks in the northern part of the county. Recent alluvium underlies the flood plains of the larger streams. The Cretaceous and younger rocks consist chiefly of clay, chalk, sandstone, sand, and gravel, and a few thin beds of limestone. These deposits are underlain by a basement complex of pre-Cretaceous crystalline rocks.

Large-scale withdrawals of water began in the Montgomery area about 1885. Pumpage by the city of Montgomery in 1958 averaged about 15 million gallons per day. It is estimated that an additional 10 to 15 million gallons per day was pumped in the county for industrial, irrigation, domestic, and stock use.

The principal aquifer in the country is the Eutaw formation. It supplies water to the city of Montgomery municipal wells, to industrial wells in the Montgomery area, and to most domestic and stock wells in the northern two-thirds of the county. Irrigation wells also tap the Eutaw. Yields from wells range from 350 to 600 gallons per minute.

The Gordo formation, the upper part of the Coker formation, and the Pleistocene terrace deposits in the Montgomery area also yield moderate to large quantities of water to municipal and industrial wells. The lower part of the Coker formation is not developed as a source of water supply, but information obtained during the investigation rthat led to this report indicates that it may be a potential source of water to wells of large capacity. Sand beds in the Ripley formation, Providence sand, and Recent alluvium in -the southern part of the county yield adequate amounts of water to domestic and stock wells.

Most of the ground water used in Montgomery County occurs under artesian conditions, although water-table conditions occur in the Pleistocene terrace deposits and Recent alluvium, and in the outcrop areas of the Eutaw and Eipley formations and the Providence sand.

Most of the water recharging the Ooker, Gordo, and Eutaw formations in their areas of outcrop also is discharged in these areas; only a small quantity of water moves downdip beneath the overlying chalk beds. The natural discharge, and hence the natural recharge, is estimated to be 0.2 to 0.3 million gallons per day per square mile of outcrop.

All ground water in the county is of chemical quality that is satisfactory for most uses, although locally it is high in iron or chloride content and is hard. Water from the Eutaw formation a few miles southwest of Montgomery's West well field is very high in chloride content. This water moves toward the cone of depression in the piezometric surface produced by pumping in the West well field.

Much additional ground water could be pumped from the Eutaw formation, especially south of Montgomery's West well field. Additional water also is available from the upper part of the Coker formation. Before large groundwater developments are planned, however, the problems of well spacing and pumping rates should be studied in order to determine the maximum development permitted by the supply. Observation wells should be installed in the Eutaw formation southwest of Montgomery's West well field to detect encroachment of water of high chloride content from adjacent Lowndes County.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1606","collaboration":"Prepared in cooperation with the Water Works and Sanitary Sewer Board of the City of Montgomery and the Geological Survey of Alabama","usgsCitation":"Knowles, D.B., Reade, H., and Scott, J.C., 1963, Geology and ground-water resources of Montgomery County, Alabama: U.S. Geological Survey Water Supply Paper 1606, Report: v, 76 p.; 15 Plates: 45.58 x 25.01 inches or smaller, https://doi.org/10.3133/wsp1606.","productDescription":"Report: v, 76 p.; 15 Plates: 45.58 x 25.01 inches or smaller","costCenters":[],"links":[{"id":27553,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1606/plate-15.pdf","text":"Plate 15","size":"544.75 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 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kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 12"},{"id":27551,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1606/plate-13.pdf","text":"Plate 13","size":"516.93 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 13"},{"id":27552,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1606/plate-14.pdf","text":"Plate 14","size":"548.80 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 14"}],"country":"United States","state":"Alabama","county":"Montgomery 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Doyle Blewer","contributorId":9633,"corporation":false,"usgs":true,"family":"Knowles","given":"Doyle","email":"","middleInitial":"Blewer","affiliations":[],"preferred":false,"id":144580,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reade, H. L.","contributorId":80244,"corporation":false,"usgs":true,"family":"Reade","given":"H. L.","affiliations":[],"preferred":false,"id":144582,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Scott, J. C.","contributorId":75901,"corporation":false,"usgs":true,"family":"Scott","given":"J.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":144581,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1009,"text":"wsp1579 - 1963 - Progress report on the ground-water resources of the Louisville area, Kentucky, 1949-55","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1579","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1579","title":"Progress report on the ground-water resources of the Louisville area, Kentucky, 1949-55","docAbstract":"In the Louisville area, the principal water-bearing formations are the glacial-outwash sand and gravel and, in places, the underlying limestone. During the period 1949 through 1955 pumpage from the two aquifers averaged about 30 mgd (million gallons per day). The pumpage was approximately in balance with the normal net recharge to the area but was only about 8 percent of the estimated potential supply of ground water, including induced infiltration from the river. In the Louisville area, ground water is used chiefly for air conditioning and for industrial cooling. In the part of the area southwest of the city, ground water is used also for public supply. \r\n\r\nHigh ground-water levels in 1937 resulted from the greatest flood of record. Subsequently, water levels generally declined in the entire Louisville area. In downtown Louisville, where ground water is used for air conditioning, the water level fluctuates seasonally in response to variations in the rate of pumping. In the heavily pumped industrial areas, where ground water is used for cooling, water-level fluctuations correlate with changes in rates of pumping caused by variations in production schedules. Levels were lowest during the years of World War II. During the period 1952-55, relatively low levels throughout the area reflected the effects of less than normal rainfall, summer drought, and sustained pumping. \r\n\r\nGround water in the Louisville area is very hard and generally of the calcium bicarbonate or calcium sulfate type. It is high in iron and sulfate content but is moderately low in chloride content. In water of the sand and gravel aquifer, the concentration of sulfate has increased gradually during the period 1949-54.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1579","usgsCitation":"Bell, E., Kellogg, R.W., and Kulp, W.K., 1963, Progress report on the ground-water resources of the Louisville area, Kentucky, 1949-55: U.S. Geological Survey Water Supply Paper 1579, iv, 47 p. :ill., maps ;24 cm. + separate portfolio with plates., https://doi.org/10.3133/wsp1579.","productDescription":"iv, 47 p. :ill., maps ;24 cm. + separate portfolio with plates.","costCenters":[],"links":[{"id":137977,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1579/report-thumb.jpg"},{"id":25589,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25590,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25591,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25592,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25593,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25594,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25595,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25596,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25597,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25598,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25599,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25600,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25601,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25602,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25603,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1579/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25604,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1579/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9be4b07f02db65dbab","contributors":{"authors":[{"text":"Bell, Edwin A.","contributorId":96660,"corporation":false,"usgs":true,"family":"Bell","given":"Edwin A.","affiliations":[],"preferred":false,"id":143018,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kellogg, Robert W.","contributorId":61793,"corporation":false,"usgs":true,"family":"Kellogg","given":"Robert","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":143017,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kulp, Willis K.","contributorId":8076,"corporation":false,"usgs":true,"family":"Kulp","given":"Willis","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":143016,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1371,"text":"wsp1655 - 1963 - Ground water in the Pullman area, Whitman County, Washington","interactions":[{"subject":{"id":55768,"text":"ofr5746 - 1957 - Ground water in the Pullman area, Whitman county, Washington","indexId":"ofr5746","publicationYear":"1957","noYear":false,"title":"Ground water in the Pullman area, Whitman county, Washington"},"predicate":"SUPERSEDED_BY","object":{"id":1371,"text":"wsp1655 - 1963 - Ground water in the Pullman area, Whitman County, Washington","indexId":"wsp1655","publicationYear":"1963","noYear":false,"title":"Ground water in the Pullman area, Whitman County, Washington"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1655","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1655","title":"Ground water in the Pullman area, Whitman County, Washington","docAbstract":"This report presents the results of an investigation of the ground-water resources of the Pullman area, Whitman County, Wash. The investigation war made in cooperation with the State of Washington, Department of Conservation, Division of Water Resources, to determine whether the 1959 rate of ground-water withdrawal exceeded the perennial yield of the developed aquifers, and if so, (1) whether additional aquifers could be developed in the area, and (2) whether the yield of the developed aquifers could be increased by artificial recharge. The Pullman area includes the agricultural district surrounding the city of Pullman, in southeastern Whitman County, and the western two-thirds of the Moscow-Pullman basin, which extends into Latah County, Idaho. The mapped area comprises shout 250 square miles. \r\n\r\nThe area is in a region of smooth rolling hills formed by erosion of thick deposits of loess, which cover a dissected lava plain. The loess (Palouse formation of Pleistocene age) ranges in thickness from less than 1 foot to more than 150 feet. The underlying lava flows, part of the Columbia River basalt of Tertiary age, are nearly horizontal and form bluffs and low cliffs along the major streams. The total thickness of the basalt sequence in the area is not known, but it may be considerably greater than 1,000 feet beneath the city of Pullman. The basalt sequence is underlain by a basement mass of granite, granite gneiss, and quartzite, of pre-Tertiary age. \r\n\r\nThe most productive aquifers in the area are in the Columbia River basalt. They consist of the permeable zones, commonly occurring at the tops of individual lava flows, which may contain ground water under either artesian or water-table conditions. Two such permeable zones have produced more than 95 percent of the ground water used in the Pullman area, or as much as 870 million gallons per year (1957). These two zones are hydraulically connected and lie at depths ranging from about 50 to 170 feet below the land surface at Pullman. The area receives about 21 inches of precipitation annually, about two-thirds of it from October through March. 0nly a fraction of the precipitation reaches the aquifers; the remainder is returned to the atmosphere by evapotranspiration or leaves the area as surface runoff. The basalt is recharged mainly by infiltration from streams and downward percolation from the overlying loess. \r\n\r\nThe ground water moves generally westward. However, most water in the artesian aquifers tapped by wells in the vicinity of Pullman may move toward the city of Pullman, which is the center of major pumping. The rate of movement ranges from extremely slow in the loess and the massive basalt to very rapid in the permeable zones of basalt. The principal modes of discharge from the artesian aquifers are seepage to streams and pumpage from wells. The amount of natural discharge is unknown, but the pumpage ranged from about 340 to 870 million gallons per year, and during 1949-59 it averaged about 800 million gallons (2,500 ac-ft) per year. For about the last 25 years at least, the piezometric surface of the artesian zones has declined each year, indicating that the annual ground-water discharge from the artesian aquifers (including pumpage and natural discharge) has exceeded the recharge in the Pullman area. An analysis of the relation of pumpage to the decline in artesian level indicates that during 1952-59 an average of about 65 million gallons per year was removed from storage. Although the decline in artesian pressures has resulted in an increase in the recharge to the aquifers, the present rate of pumping may be equal to or even exceed the perennial yield of the artesian aquifer in the report area under natural conditions. \r\n\r\nGeologic and hydrologic conditions seem favorable for the existence of potentially good aquifers below those which are now extensively developed. The deep aquifers seem to have only a slight hydraulic connection with the overlying artesian basalt ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1655","usgsCitation":"Foxworthy, B., and Washburn, R., 1963, Ground water in the Pullman area, Whitman County, Washington: U.S. Geological Survey Water Supply Paper 1655, iv, 71 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1655.","productDescription":"iv, 71 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":110001,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24847.htm","linkFileType":{"id":5,"text":"html"},"description":"24847"},{"id":137288,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1655/report-thumb.jpg"},{"id":26462,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1655/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26463,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1655/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26464,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1655/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26465,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1655/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66d89c","contributors":{"authors":[{"text":"Foxworthy, B. L.","contributorId":45686,"corporation":false,"usgs":true,"family":"Foxworthy","given":"B. L.","affiliations":[],"preferred":false,"id":143651,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Washburn, R.L.","contributorId":89114,"corporation":false,"usgs":true,"family":"Washburn","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":143652,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1916,"text":"wsp1539T - 1963 - Geology and ground-water resources of the Lake Dakota Plain area, South Dakota","interactions":[],"lastModifiedDate":"2016-04-05T09:58:33","indexId":"wsp1539T","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"T","title":"Geology and ground-water resources of the Lake Dakota Plain area, South Dakota","docAbstract":"

The Lake Dakota plain area is a nearly flat surface that includes parts of Spink, Brown, Marshall, and Day Counties in northeastern South Dakota. Agriculture is the principal occupation. Because precipitation often is insufficient for maximum crop production, the U.S. Bureau of Reclamation has developed a plan for irrigation of the area. Most of the irrigation water would be conveyed by canal from a reservoir on the Missouri River, about 100 miles to the west, but some would be obtained locally from the James River.

\n

The surface of the Precambrian rocks, which underlie the area at a depth of 1,200 to 1,500 feet, is the lower limit to which water wells are drilled. Most of the producing wells in the area tap the Dakota sandstone, which has an average thickness of about 400 feet and rests on the Precambrian rocks. The Dakota is not recharged locally; water percolates into the Lake Dakota plain area principally from areas of recharge to the west. Because the aggregate discharge from wells tapping the Dakota exceeds the estimated rate of lateral percolation into the area, some of the discharged water probably is derived from storage. Although the artesian pressure is still sufficient to cause wells to flow, it is much less now than it was when the first wells were drilled in the 1880's. Water from the Dakota is highly mineralized; the specific conductance of water from 71 wells ranged from 2,590 to 4,380 micromhos per centimeter. Most of the water was of the sodium sulfate type and was soft. By recognized standards the water is chemically unsuitable for most uses, but for many years it has been the principal source of supply both on farms and in the municipalities. Use of the water for irrigation is reported to have made the soil unproductive.

\n

The Dakota is overlain by younger Cretaceous rocks aggregating 700 to 800 feet in thickness. These rocks, which consist of shale and limestone, generally are too nearly impermeable to be a source of water supply.

\n

Unconsolidated deposits of Quaternary age mantle the Cretaceous rocks. Although they consist mostly of material that is too fine grained to yield water freely to wells, the Quaternary deposits contain bodies of moderately to highly permeable material that yield water copiously. Such bodies may be located only by exploratory drilling or, possibly, geophysical methods. The water differs widely in amount of mineralization and in chemical composition; the specific conductance of water from 322 wells ranged from 246 to 13,300 micromhos per centimeter. In most of the report area the water is of unsuitable quality for irrigation and domestic use. The principal source of recharge to the Quaternary deposits is infiltrating precipitation. Evapotranspiration accounts for nearly all the water discharged; the amount of water discharging into stream channels and withdrawn from wells is almost negligible by comparison. Irrigation of the area would increase the rate of recharge to the Quaternary deposits and would cause the water table to rise. Probably it would also cause an increase in the concentration of dissolved minerals in much of the ground water. Artificial drainage would be necessary to prevent waterlogging of cropland.

","language":"English","publisher":"U.S. Government Print Office","publisherLocation":"Washington, DC","doi":"10.3133/wsp1539T","usgsCitation":"Hopkins, W.B., and Petri, L., 1963, Geology and ground-water resources of the Lake Dakota Plain area, South Dakota: U.S. Geological Survey Water Supply Paper 1539, Report: v, 68 p.; 3 Plates: 26.00 x 40.33 inches or smaller, https://doi.org/10.3133/wsp1539T.","productDescription":"Report: v, 68 p.; 3 Plates: 26.00 x 40.33 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":137686,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1539t/report-thumb.jpg"},{"id":27236,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539t/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27237,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539t/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27238,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539t/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27239,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1539t/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109986,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24741.htm","linkFileType":{"id":5,"text":"html"},"description":"24741"}],"country":"United States","state":"South Dakota","otherGeospatial":"Lake Dakota Plain","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -98.525390625,\n 44.68427737181225\n ],\n [\n -98.525390625,\n 45.82879925192134\n ],\n [\n -97.6025390625,\n 45.82879925192134\n ],\n [\n -97.6025390625,\n 44.68427737181225\n ],\n [\n -98.525390625,\n 44.68427737181225\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6854ff","contributors":{"authors":[{"text":"Hopkins, William B.","contributorId":54574,"corporation":false,"usgs":true,"family":"Hopkins","given":"William","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":144361,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Petri, Lester R.","contributorId":19534,"corporation":false,"usgs":true,"family":"Petri","given":"Lester R.","affiliations":[],"preferred":false,"id":144360,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2390,"text":"wsp1757A - 1963 - Ground-water exploration in Al Marj area, Cyrenaica, United Kingdom of Libya","interactions":[],"lastModifiedDate":"2012-02-02T00:05:33","indexId":"wsp1757A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1757","chapter":"A","title":"Ground-water exploration in Al Marj area, Cyrenaica, United Kingdom of Libya","docAbstract":"The present report, based largely on fieldwork during 1959-61, describes the results of reconnaissance hydrogeologic studies and exploratory drilling to evaluate the general water-bearing properties of the rocks and the availability of groundwater supplies for irrigation, stock, and village uses in Al Marj area. These studies and the drilling were conducted under the auspices of the U.S. Operations Mission of the International Cooperation Administration. \r\n\r\nAl Marj area, located in the Province of Cyrenaica on the southern coast of the Mediterranean Sea, contains a land area of about 6,770 square kilometers. Along the Mediterranean shore is a narrow coastal plain that rises evenly to the base of an escarpment that forms the seaward front of an undulating plateau known as. Al Jabal al Akhgiar. The climate is semiarid; seasonal rainfall occurs during the winter months. Owing to orographic effects, the rainfall is somewhat higher in the Jabal than in the coastal plain. The average annual rainfall ranges from about 250 millimeters in the coastal plain to 450 millimeters on the Jabal. All the streams (wadis) of the area are ephemeral and flow only in response to heavy rains of the winter season. From a drainage divide on the Jabal some streams flow north and northwest toward the sea and the others, south and southeast to the interior desert. Solution features, such as limestone sink holes, are common in the coastal plain and a large solution depression occurs near Al Marj. \r\n\r\nThe rocks of A1 Marj area consist predominantly of limestone and some sandstone and shale; they range from Cretaceous to Miocene age. On the coastal plain Miocene limestone is locally mantled by Quaternary alluvial, beach and lagoonal deposits. The Miocene and older beds have a regional southerly dip. These rocks are broken by northeast-trending normal faults in the coastal and inland escarpments. \r\n\r\nThe ground-water reservoir is contained chiefly in fractures, bedding planes, and solution openings in the limestone country rock. The upper limit of this reservoir is marked by a water table which generally lies within 40 meters of the land surface in the coastal plain but is 100 meters or more below the surface of most of the Jabal and the interior desert. The ground-water reservoir is replenished chiefly by infiltration from surface-water runoff in wadis and to less extent by direct infiltration of rainfall. Ground water moves north and northwest toward the Mediterranean Sea and south toward the interior desert from a ground-water divide near the crest of A1 Jabal al Akhgiar. Discharge of ground water takes place by submarine outflow, spring flow, evapotranspiration, and withdrawals from wells. \r\n\r\nWells, springs, and cisterns furnish almost all water supplies for municipal, village, stock and irrigation purposes. Bengasi, A1 Marj, and A1 Abyar are the only centers of population with municipal distribution systems. Drafts from individual dug wells used for irrigation in the coastal plain generally are no more than 10 to 15 cubic meters per day. In the Jabal and the interior desert drafts from individual stock and village wells are generally less than 10 cubic meters per day and from most wells only a few thousand liters per day. \r\n\r\nSome 21 test wells were put down during the present investigation to depths ranging from 30 to 309 meters. The yields obtained by test pump and bailer ranged from 45 to 0.6 cubic meters per hour. With few exceptions, well yields sufficient for stock and village requirements were obtained. Well yields sufficient for irrigation even on a moderate scale, however, are not everywhere available. In the Jabal and the interior desert the ground water is generally of good to fair chemical quality and suitable for most purposes. In the coastal plain, however, the ground water is in places moderately to highly mineralized, and consequently for irrigation use it must be applied to the land under optimum crop soil, and drainage conditions.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1757A","usgsCitation":"Newport, T., and Haddor, Y., 1963, Ground-water exploration in Al Marj area, Cyrenaica, United Kingdom of Libya: U.S. Geological Survey Water Supply Paper 1757, iii, 24 p. :ill., maps ;24 cm. + plates folded in pocket., https://doi.org/10.3133/wsp1757A.","productDescription":"iii, 24 p. :ill., maps ;24 cm. + plates folded in pocket.","costCenters":[],"links":[{"id":139184,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1757a/report-thumb.jpg"},{"id":28365,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28366,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757a/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28367,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1757a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66ce76","contributors":{"authors":[{"text":"Newport, T.G.","contributorId":80258,"corporation":false,"usgs":true,"family":"Newport","given":"T.G.","email":"","affiliations":[],"preferred":false,"id":145123,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Haddor, Yousef","contributorId":78722,"corporation":false,"usgs":true,"family":"Haddor","given":"Yousef","email":"","affiliations":[],"preferred":false,"id":145122,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":971,"text":"wsp1646 - 1963 - Ground-water geology of Grayson County, Texas","interactions":[],"lastModifiedDate":"2016-08-22T11:15:53","indexId":"wsp1646","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1646","title":"Ground-water geology of Grayson County, Texas","docAbstract":"

Grayson County in north-central Texas is near the north edge of the West Gulf Coastal Plain. The county has an area of 927 square miles and had an estimated population of 79,500 in 1957. The major town is Sherman, which has an estimated population of 31,000. The northern two-thirds of the county is drained by tributaries of the Red River; the southern one-third is drained by tributaries of the Trinity River

\n

Sedimentary rocks exposed at the surface in Grayson County are of Cretaceous and Quaternary age. Sand, clay, marl, and limestone of Cretaceous age, having a maximum thickness of about 3,600 feet, underlie the county; the beds dip regionally to the southeast. Quaternary alluvium mantles part of the surface along the Red River and occurs in scattered patches elsewhere in the county.

\n

The Trinity group and Woodbine formation of Cretaceous age are the principal water-bearing formations. Other stratigraphic units that yield water to wells are, in order of importance, the Quaternary alluvium and the Pawpaw formation, Eagle Ford shale, and Austin chalk of Cretaceous age.

\n

Ground water in Grayson County generally moves eastward and southward from areas of recharge to areas of discharge. Average rates of water movement in the Trinity group and Woodbine formation are estimated to be about 1.5 and 15 feet per year, respectively. The chief source of recharge to these aquifers is precipitation on the outcrop, although Lake Texoma contributed some recharge to the Trinity where it crops out in the lake. Ground water discharges naturally by evapotranspiration, by vertical leakage, through springs, artificially through wells, and by underflow out of the county to the southeast.

\n

The withdrawal of ground water in Grayson County in 1957 was about 5 mgd. Of this amount, about 61 percent came from the Woodbine formation, about 36 percent from the Trinity group, and about 3 percent from the other water-bearing formations. About 65 percent of the ground water pumped in Grayson County is withdrawn in the Sherman area.

\n

Increased withdrawal of water since World War II has resulted in a rapid decline of the water levels in parts of Grayson County. The maximum decline in the Trinity group at Sherman from 1945 to 1958 was 113 feet, or about 8 feet per year. During the same period, water levels in the Woodbine formation at Sherman declined as much as 156 feet, an average of 12 feet per year. Total declines since the early part of the 20th century were at least 180 feet in the Trinity group and about 240 feet in the Woodbine formation. Water levels in the area of outcrop of the principal aquifers, fluctuating chiefly in response to rainfall or changes in the natural rate of recharge, showed no appreciable decline from 1957 to 1959.

\n

Coefficients of transmissibility, determined from pumping tests in Grayson County, averaged 2,800 gpd per ft for the Trinity group and 3,200 gpd per ft for the Woodbine formation.

\n

Kesults of chemical analyses of water samples indicate that the ground water in Grayson County is suitable for most purposes. The Trinity group generally yields soft water that has a high sodium bicarbonate content and is of questionable quality for irrigation. The water from the Woodbine formation ranges more widely in chemical composition than the water from the Trinity. It generally is soft but has a high iron content; it is usually suitable for irrigation in the outcrop area but unsuitable in the downdip area. Water from the other water-bearing formation, though generally hard, is suitable for most purposes, judging from the few analyses available.

\n

The ground-water resources of Grayson County have been only partly developed. The volume of fresh water in transient storage in the Trinity group and Woodbine formation is estimated to be about 60 and 25 million acre-feet, respectively. Most of this water is not practicably recoverable because of the depth at which it occurs, but relatively high artesian heads and large available drawdowns in much of the county are favorable to future development within economic limits of pumping lift. In the Sherman area, however, concentrated pumping has caused large declines in the water levels, resulting in some dewatering of the Woodbine. Because of the large margin of 'safety before dewatering of the Trinity group begins, the Trinity is the most favorable source of additional ground water for Sherman. However, the higher lifting costs should be considered.

\n

Large to moderate amounts of additional ground water can be obtained from the Trinity group and Woodbine formation in most presently undeveloped areas in the county. Water suitable for irrigation is available in moderate to large amounts from the Woodbine formation in places on its outcrop. A limiting factor to any large ground-water development, however, is the extent and thickness of saturated fresh-water sand available in the area. The thickness of saturated fresh-water sand in the Trinity decreases northward; the thickness of the sand in the Woodbine is more erratic and has little definite pattern.

\n

Moderate to large supplies of water may be available from the alluvium near the Red River, but more information is needed before definite conclusions can be reached.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1646","isbn":"pbk","usgsCitation":"Baker, E., 1963, Ground-water geology of Grayson County, Texas: U.S. Geological Survey Water Supply Paper 1646, Report: v, 61 p.; 6 Plates, https://doi.org/10.3133/wsp1646.","productDescription":"Report: v, 61 p.; 6 Plates","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":25516,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25517,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1646/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137044,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1646/report-thumb.jpg"},{"id":25511,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109998,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24841.htm","linkFileType":{"id":5,"text":"html"},"description":"24841"},{"id":25512,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25513,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25514,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25515,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668e7c","contributors":{"authors":[{"text":"Baker, E.T.","contributorId":11584,"corporation":false,"usgs":true,"family":"Baker","given":"E.T.","email":"","affiliations":[],"preferred":false,"id":142944,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":66799,"text":"i380 - 1963 - The Indian Ocean: The geology of its bordering lands and the configuration of its floor","interactions":[],"lastModifiedDate":"2017-05-18T11:44:38","indexId":"i380","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":320,"text":"IMAP","code":"I","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"380","title":"The Indian Ocean: The geology of its bordering lands and the configuration of its floor","docAbstract":"

The ocean realm, which covers more than 70 percent of the earth's surface, contains vast areas that have scarcely been touched by exploration. The best known parts of the sea floor lie close to the borders of the continents, where numerous soundings have been charted as an aid to navigation. Yet, within this part of the sea floor, which constitutes a border zone between the toast and the ocean deeps, much more detailed information is needed about the character of the topography and geology. At many places, stratigraphic and structural features on the coast extend offshore, but their relationships to the rocks of the shelf and slope are unknown, and the geology of the coast must be projected seaward across the continental shelf and slope.

The Indian Ocean, the third largest ocean of the world, has been selected for intensive study by an international group using all modern techniques to determine its physical characteristics. This report, with accompanying illustrations, has been prepared as a very generalized account of some aspects of the geology of the vast coastal areas of the northern Indian Ocean in relation to the bordering shelves and ocean deeps. Its general purpose is to serve as background reading.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/i380","usgsCitation":"Pepper, J., and Everhart, G.M., 1963, The Indian Ocean: The geology of its bordering lands and the configuration of its floor: U.S. Geological Survey IMAP 380, Report: 33 p; 1 Plate: 46.05 x 36.57 inches, https://doi.org/10.3133/i380.","productDescription":"Report: 33 p; 1 Plate: 46.05 x 36.57 inches","numberOfPages":"34","costCenters":[],"links":[{"id":115186,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/imap/0380/report.pdf","size":"2617","linkFileType":{"id":1,"text":"pdf"}},{"id":115187,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/imap/0380/plate-1.pdf","size":"9321","linkFileType":{"id":1,"text":"pdf"}},{"id":188292,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/imap/0380/report-thumb.jpg"}],"scale":"1365000","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c345","contributors":{"authors":[{"text":"Pepper, James F.","contributorId":10086,"corporation":false,"usgs":true,"family":"Pepper","given":"James F.","affiliations":[],"preferred":false,"id":275101,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Everhart, Gail M.","contributorId":42640,"corporation":false,"usgs":true,"family":"Everhart","given":"Gail","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":275102,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70221118,"text":"70221118 - 1963 - Early pennsylvanian currents in the southern Appalachian Mountains","interactions":[],"lastModifiedDate":"2021-06-04T12:02:11.312222","indexId":"70221118","displayToPublicDate":"1963-11-01T11:00:12","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Early pennsylvanian currents in the southern Appalachian Mountains","docAbstract":"

Measurement of more than 1200 cross-beds in lower Pennsylvanian sandstones of the southern Appalachian Mountains reveals a broad pattern of sediment transport to the southwest and west. Most of the sand appears to have been derived from the east and to have moved south-westward parallel to the axis of the Appalachian geosyncline. The pattern has a similar alignment to that in the Illinois basin, but it is at right angles to earlier Paleozoic dispersal directions in the Appalachian geosyncline. Little or no sand has been contributed from the Cincinnati arch.

The cross-beds are in sheetlike sandstone formations; the sandstone is conglomeratic, contains plant impressions, and is composed of lenticular, channeling, quartzose sedimentation units. The variation in thickness and lateral persistence of sedimentation units is also reflected in a moderate variability of mean cross-bedding directions between adjacent formations, and even within the same formation. Cross-bedding variability between adjacent units is thought to be due to regional changes in the position and orientation of channel-way systems from deposition of one sandstone formation to the next. Changes of cross-bedding azimuths within the same formation may result from channel curvature of local meanderlike deposits or from channel migration as the sands coalesced into a blanket deposit.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[1439:EPCITS]2.0.CO;2","usgsCitation":"Schlee, J., 1963, Early pennsylvanian currents in the southern Appalachian Mountains: Geological Society of America Bulletin, v. 74, no. 12, p. 1439-1451, https://doi.org/10.1130/0016-7606(1963)74[1439:EPCITS]2.0.CO;2.","productDescription":"13 p.","startPage":"1439","endPage":"1451","costCenters":[],"links":[{"id":386190,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Kentucky, Tennessee, Alabama, Georgia","otherGeospatial":"southern Appalachian Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.23291015625,\n 37.85750715625203\n ],\n [\n -84.52880859375,\n 36.155617833818525\n ],\n [\n -86.63818359375,\n 34.470335121217474\n ],\n [\n -85.93505859374999,\n 33.815666308702774\n ],\n [\n -84.17724609375,\n 34.903952965590065\n ],\n [\n -80.52978515625,\n 36.27970720524017\n ],\n [\n -81.23291015625,\n 37.85750715625203\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"74","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Schlee, J.","contributorId":45821,"corporation":false,"usgs":true,"family":"Schlee","given":"J.","affiliations":[],"preferred":false,"id":816939,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221115,"text":"70221115 - 1963 - Factors influencing the pore volume of fine-grained sediments under low-to-moderate overburden loads","interactions":[],"lastModifiedDate":"2021-06-02T15:40:56.925074","indexId":"70221115","displayToPublicDate":"1963-09-01T10:34:45","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3369,"text":"Sedimentology","active":true,"publicationSubtype":{"id":10}},"title":"Factors influencing the pore volume of fine-grained sediments under low-to-moderate overburden loads","docAbstract":"

An anomalous increase of pore volume with increasing depth in the range 0—1,900 ft. occurs in fine‐grained sediments along the east side of the San Joaquin Valley of Cali‐ fornia. Several possible causes for the anomaly were inferred from a literature search and from study of the core samples. Statistical analyses of the core sample data suggest the principle causes to be variations in particle size, the diatom‐skeleton content, and the type of exchangeable cation adsorbed by the clay‐mineral constituents of the sediments. 

","language":"English","publisher":"Wiley Blackwell","doi":"10.1111/j.1365-3091.1963.tb01217.x","usgsCitation":"Meade, R., 1963, Factors influencing the pore volume of fine-grained sediments under low-to-moderate overburden loads: Sedimentology, v. 2, no. 3, p. 235-242, https://doi.org/10.1111/j.1365-3091.1963.tb01217.x.","productDescription":"8 p.","startPage":"235","endPage":"242","costCenters":[],"links":[{"id":386129,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"San Joaquin Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121.6241455078125,\n 36.721273880045004\n ],\n [\n -119.7344970703125,\n 36.721273880045004\n ],\n [\n -119.7344970703125,\n 38.26406296833961\n ],\n [\n -121.6241455078125,\n 38.26406296833961\n ],\n [\n -121.6241455078125,\n 36.721273880045004\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"2","issue":"3","noUsgsAuthors":false,"publicationDate":"2006-06-14","publicationStatus":"PW","contributors":{"authors":[{"text":"Meade, R.H.","contributorId":27449,"corporation":false,"usgs":true,"family":"Meade","given":"R.H.","email":"","affiliations":[],"preferred":false,"id":816793,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221120,"text":"70221120 - 1963 - Two pollen diagrams from southeastern Minnesota: Problems in the regional late-glacial and postglacial vegetational history","interactions":[],"lastModifiedDate":"2021-06-02T16:23:13.324044","indexId":"70221120","displayToPublicDate":"1963-08-01T11:18:24","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Two pollen diagrams from southeastern Minnesota: Problems in the regional late-glacial and postglacial vegetational history","docAbstract":"

Kirchner Marsh and Lake Carlson are located 3 miles apart in Dakota County about 15 miles south of Minneapolis in the St. Croix moraine, which was formed by the Superior lobe during the Gary phase of the Wisconsin glaciation. During the Mankato phase that followed, the Des Moines lobe advanced to within a few miles of the sites. The region today is in a mixed-oak forest, with a maplebasswood forest 15 miles to the west and a re-entrant of the prairie on the sand plain south of the moraine. The general limit of coniferous trees is about 50 miles northeast of the sites, although outliers, especially of Pinus strobus, may be found along the Mississippi Valley a few miles to the east. One sediment core 12-13 m long from each site was analyzed for pollen content at 5-25-cm intervals. Diagrams based on percentage of total pollen (trees, shrubs, wind-pollinated herbs) show essentially identical sequences at the two sites, starting with the late-glacial phase of ice retreat. The diagrams have been subdivided into pollen zones according to the A-B-C sequence introduced by Deevey for New England. The late-glacial pollen record starts at Kirchner Marsh with a short Picea-Cyperaceae-Gramineae phase (Zone K), believed to represent a spruce parkland. Its C-14 date of 13,270 BP and the stratigraphy indicate a pre-Two Creeks and post- Gary correlation. Apparently the Kirchner site did not become established as a lake until this time owing to persistence of dead ice in the moraine. The absence of pollen of specific tundra indicators and the presence of pollen of such thermophilous plants as Fraxinus, Quercus, Corylus, Ambrosia, Humulus, and Typha latifolia imply that the climate was cool rather than cold. Zone A-a, which follows, correlates with the Two Creeks interstade. It is marked by the dominance of Picea, with appreciable percentages of Fraxinus and Ambrosia and with minor amounts of other thermophilous plants and the normal boreal associates of spruce like Betula, Larix, and Salix. Zone A-b, starting 12,050 C-14 years ago, correlates with the Valders ice advance. It is represented at both Kirchner and Carlson and shows the withdrawal of Fraxinus and Ambrosia and the slight rise of Artemisia. Except for the absence of pine in the late-glacial assemblage the vegetation implied by these three zones seems to have its closest modern counterpart in the southern fringe of the Boreal Forest of the Riding Mountain region of southwest Manitoba. It is concluded that pine did not migrate southward with the spruce during the Wisconsin glaciation, at least in the western Great Lakes region, and was thus eliminated from this region. During the lateglacial phases of ice retreat, herbs and spruce pioneered on the deglaciated terrain; pine did not follow until the destruction of the spruce forest at the end of the late-glacial phase. Zone B introduces postglacial time. It represents the time of rapid Vegetational succession following the deterioration of the spruce forest. Simultaneous maxima of Betula, Alnus, Fraxinus, and Abies occurred 10,230 years ago at Kirchner Marsh. These were followed rapidly by a Pinus maximum and then a rise of Ulmus, Quercus, and other deciduous types, dated as 9300 years ago at the correlative site of Madeha. This succession may represent differential rates of migration from refuges south and east of Minnesota. Deciduous trees dominate the C Zones. Zone C-a shows Ulmus and Ostrya /Carpinus followed by Quercus; it probably represents principally a mesic maple-basswood forest changing to oak. Zone C-b represents the advance of prairie into the region at the expense of the oak woodland or savanna. The large and abrupt fluctuations in the curves for Ambrosia-type and Chenopodiineae, especially at the Carlson site, may record encroachment of annual weeds onto intermittently dried lake bottoms. C-14 dates place Zone C-b between 7100 and 5100 years ago. In Zone C-c the Quercus again dominates until the abrupt increase in Ambrosiatype and Chenopodiineae that marks the time of forest clearance and land settlement 50-75 years ago. 

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[1371:TPDFSM]2.0.CO;2","usgsCitation":"Wright, H., Winter, T.C., and Patten, H.L., 1963, Two pollen diagrams from southeastern Minnesota: Problems in the regional late-glacial and postglacial vegetational history: Geological Society of America Bulletin, v. 74, no. 11, p. 1371-1396, https://doi.org/10.1130/0016-7606(1963)74[1371:TPDFSM]2.0.CO;2.","productDescription":"26 p.","startPage":"1371","endPage":"1396","costCenters":[],"links":[{"id":386134,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Minnesota","otherGeospatial":"southeastern Minnesota","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -94.39453125,\n 43.58039085560784\n ],\n [\n -91.14257812499999,\n 43.58039085560784\n ],\n [\n -91.14257812499999,\n 45.182036837015886\n ],\n [\n -94.39453125,\n 45.182036837015886\n ],\n [\n -94.39453125,\n 43.58039085560784\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"74","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Wright, H.E. Jr.","contributorId":56369,"corporation":false,"usgs":true,"family":"Wright","given":"H.E.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":816797,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Winter, Thomas C.","contributorId":84736,"corporation":false,"usgs":true,"family":"Winter","given":"Thomas","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":816798,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Patten, Harvey L.","contributorId":259197,"corporation":false,"usgs":false,"family":"Patten","given":"Harvey","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":816799,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70221119,"text":"70221119 - 1963 - Early pennsylvanian currents in the southern Appalachian Mountains","interactions":[],"lastModifiedDate":"2021-06-02T16:06:25.298065","indexId":"70221119","displayToPublicDate":"1963-08-01T11:00:12","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Early pennsylvanian currents in the southern Appalachian Mountains","docAbstract":"

Measurement of more than 1200 cross-beds in lower Pennsylvanian sandstones of the southern Appalachian Mountains reveals a broad pattern of sediment transport to the southwest and west. Most of the sand appears to have been derived from the east and to have moved south-westward parallel to the axis of the Appalachian geosyncline. The pattern has a similar alignment to that in the Illinois basin, but it is at right angles to earlier Paleozoic dispersal directions in the Appalachian geosyncline. Little or no sand has been contributed from the Cincinnati arch. The cross-beds are in sheetlike sandstone formations; the sandstone is conglomeratic, contains plant impressions, and is composed of lenticular, channeling, quartzose sedimentation units. The variation in thickness and lateral persistence of sedimentation units is also reflected in a moderate variability of mean cross-bedding directions between adjacent formations, and even within the same formation. Cross-bedding variability between adjacent units is thought to be due to regional changes in the position and orientation of channel-way systems from deposition of one sandstone formation to the next. Changes of cross-bedding azimuths within the same formation may result from channel curvature of local meanderlike deposits or from channel migration as the sands coalesced into a blanket deposit. 

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[1439:EPCITS]2.0.CO;2","usgsCitation":"Schlee, J., 1963, Early pennsylvanian currents in the southern Appalachian Mountains: Geological Society of America Bulletin, v. 74, no. 12, p. 1439-1451, https://doi.org/10.1130/0016-7606(1963)74[1439:EPCITS]2.0.CO;2.","productDescription":"13 p.","startPage":"1439","endPage":"1451","costCenters":[],"links":[{"id":386132,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Kentucky, Tennessee, Alabama, Georgia","otherGeospatial":"southern Appalachian Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.58447265624999,\n 37.16031654673677\n ],\n [\n -84.561767578125,\n 35.71975793933433\n ],\n [\n -86.59423828125,\n 34.66935854524543\n ],\n [\n -85.902099609375,\n 34.161818161230386\n ],\n [\n -81.090087890625,\n 36.54494944148322\n ],\n [\n -80.595703125,\n 37.06394430056685\n ],\n [\n -81.58447265624999,\n 37.16031654673677\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"74","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Schlee, John","contributorId":16078,"corporation":false,"usgs":true,"family":"Schlee","given":"John","affiliations":[],"preferred":false,"id":816796,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221087,"text":"70221087 - 1963 - Gibson peak pluton: A discordant composite intrusion in the southeastern Trinity Alps, northern California","interactions":[],"lastModifiedDate":"2021-06-01T19:12:37.423082","indexId":"70221087","displayToPublicDate":"1963-07-01T14:08:26","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Gibson peak pluton: A discordant composite intrusion in the southeastern Trinity Alps, northern California","docAbstract":"

Gibson Peak pluton is the most discordant of several dominantly granitic intrusions in the Trinity Alps of northern California. It formed during Nevadan (Late Jurassic) deformation by emplacement of at least five discrete rock units that define a successively more silicic series, ranging from hypersthene gabbro to trondhjemitic tonalite. Contact features suggest that several units were incompletely crystalline when intruded by succeeding phases. Deformation of wall rocks, mainly partly serpentinized peridotite, indicates forceful intrusion, despite remarkable discordance of the pluton to regional structures. The discordance probably was controlled by regional extension fracturing during late stages of Nevadan deformation. Chemical compositions, computed from average modes of the intrusive units, are characterized by high Fe2O3-FeO and Na2O-K2O ratios. Plots of normative feldspar define a trend of trondhjemitic differentiation that diverges markedly from typical calc-alkaline trends. Contact metamorphism to mineral assemblages of pyroxene hornfels facies has been largely obscured by later low-grade hydration reactions, resulting in a net increase in serpentinization of most country-rock peridotite within the contact aureole.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[1259:GPPADC]2.0.CO;2","usgsCitation":"Lipman, P.W., 1963, Gibson peak pluton: A discordant composite intrusion in the southeastern Trinity Alps, northern California: Geological Society of America Bulletin, v. 74, no. 10, p. 1259-1280, https://doi.org/10.1130/0016-7606(1963)74[1259:GPPADC]2.0.CO;2.","productDescription":"22 p.","startPage":"1259","endPage":"1280","costCenters":[],"links":[{"id":386061,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"northern California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124.98046874999999,\n 38.73694606567598\n ],\n [\n -119.79492187499997,\n 38.73694606567598\n ],\n [\n -119.79492187499997,\n 42.00032514831618\n ],\n [\n -124.98046874999999,\n 42.00032514831618\n ],\n [\n -124.98046874999999,\n 38.73694606567598\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"74","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Lipman, Peter W. 0000-0001-9175-6118","orcid":"https://orcid.org/0000-0001-9175-6118","contributorId":203612,"corporation":false,"usgs":true,"family":"Lipman","given":"Peter","email":"","middleInitial":"W.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true},{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"preferred":true,"id":816719,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1686,"text":"1686 - 1963 - Dispersion in natural streams","interactions":[],"lastModifiedDate":"2022-08-17T19:54:23.991124","indexId":"1686","displayToPublicDate":"1963-01-01T10:28:08","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":375,"text":"Open-File Report","active":false,"publicationSubtype":{"id":6}},"title":"Dispersion in natural streams","docAbstract":"

Eleven tests were conducted to study the dispersion patterns of a radiotracer in five natural stream channels and in one canal. The radiotracer was injected as a line source. The patterns of dispersion that were observed in these channels were compared with patterns predicted by the theoretical models for one-dimensional flow developed by Taylor and other investigators. Analysis of the relation between time and concentration of the tracer at several sections in each of the six reaches shows that the available theoretical models are not adequate to describe the dispersion patterns actually observed. Dispersion coefficients determined from the test data are from 2 to 30 times greater than those predicted by the theoretical models. It is apparent that a better understanding of the dispersal phenomenon is needed in order to predict dispersion patterns in natural streams.

","language":"English","publisher":"U.S. Geological Survey,","publisherLocation":"Washington, D.C.","doi":"10.3133/1686","collaboration":"Prepared in cooperation with the United States Atomic Energy Commission","usgsCitation":"Godfrey, R.G., and Frederick, B.J., 1963, Dispersion in natural streams: Open-File Report, viii, 75 p., https://doi.org/10.3133/1686.","productDescription":"viii, 75 p.","numberOfPages":"83","costCenters":[],"links":[{"id":405280,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/1686/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":289868,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/1686/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53c4fc0ce4b0b58d96eeb581","contributors":{"authors":[{"text":"Godfrey, Richard G.","contributorId":100046,"corporation":false,"usgs":true,"family":"Godfrey","given":"Richard","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":143970,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Frederick, Bernard J.","contributorId":106808,"corporation":false,"usgs":true,"family":"Frederick","given":"Bernard","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":143971,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010770,"text":"70010770 - 1963 - Indirect spectrophotometric determination of traces of bromide in water","interactions":[],"lastModifiedDate":"2020-11-19T18:18:17.78877","indexId":"70010770","displayToPublicDate":"1963-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":761,"text":"Analytical Chemistry","active":true,"publicationSubtype":{"id":10}},"title":"Indirect spectrophotometric determination of traces of bromide in water","docAbstract":"

A rapid, accurate, and sensitive indirect spectrophotometric method for the determination of bromide in natural waters is based on the catalytic effect of bromide on the oxidation of iodine to iodate by potassium permanganate in sulfuric acid solution. The method is applicable to concentrations ranging from 1 to 100 μg. of bromide per liter, but may be modified to extend the concentration range. Most ions commonly occurring in water do not interfere. The standard deviation is 2.9 at bromide concentrations of 100 μg. per liter and less at lower concentrations. The determination of bromide in samples containing known added amounts gave values ranging from 99 to 105% of the concentration calculated to be present.

","language":"English","publisher":"ACS Publications","doi":"10.1021/ac60195a012","usgsCitation":"Fishman, M.J., and Skougstad, M., 1963, Indirect spectrophotometric determination of traces of bromide in water: Analytical Chemistry, v. 35, no. 2, p. 146-149, https://doi.org/10.1021/ac60195a012.","productDescription":"4 p.","startPage":"146","endPage":"149","numberOfPages":"4","costCenters":[],"links":[{"id":218658,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"35","issue":"2","noUsgsAuthors":false,"publicationDate":"2002-05-01","publicationStatus":"PW","scienceBaseUri":"505a3a99e4b0c8380cd61de4","contributors":{"authors":[{"text":"Fishman, M. J.","contributorId":65069,"corporation":false,"usgs":true,"family":"Fishman","given":"M.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":359610,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Skougstad, M. W.","contributorId":59418,"corporation":false,"usgs":true,"family":"Skougstad","given":"M. W.","affiliations":[],"preferred":false,"id":359609,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1000140,"text":"1000140 - 1963 - Age and growth of the whitefish in Lake Superior","interactions":[],"lastModifiedDate":"2013-02-04T11:54:57","indexId":"1000140","displayToPublicDate":"1963-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1663,"text":"Fishery Bulletin","printIssn":"0090-0656","active":true,"publicationSubtype":{"id":10}},"title":"Age and growth of the whitefish in Lake Superior","docAbstract":"The average annual commercial production of whitefish in the U.S. waters of Lake Superior dropped from 2,194,000 pounds in 1879-1908 to 504,000 pounds in 1911-59. The modern production, though far below the earlier, has accounted for more than 10 percent of the total value of the fishery in all but one of the last 20 years. Data are given on growth rate, age and year-class composition, size distribution, and length-weight relation of 1,800 fish collected in 1957-59 at Bayfield, Wis., and Marquette, Whitefish Point, and Dollar Settlement, Mich. Studies of the body-scale relation, sex ratio, and age and size at maturity were limited to fish collected at Bayfield. The age composition and mean age varied widely by port and year of capture. Oldest fish were those of the 1957 Bayfield samples which were dominated by age group VII and averaged 5.5 years old. The youngest were from Whitefish Point in 1959; age-group III was dominant, and the mean age was 3.2 years. The evidence on the strength of year classes was not clear-cut, but it was obvious that fluctuations in stocks of different areas were largely independent. The percentage of legal-size fish (17 inches or longer) in age groups ranged widely; only 8.6 percent of the V group were legal in the 1957 Bayfield collections, whereas 100 percent of fish of the same age were legal in the 1957-59 collections from Whitefish Point. The weight of whitefish in the combined samples increased as the 3.2408 power of the length. The growth rate from the fastest to the slowest growing stocks ranked as follows: Whitefish Point; Dollar Settlement and Marquette (fish from the two ports reversed ranks after 3 years); Bayfield. The major differences in growth in length among the various stocks occurred during the first years of life. Beyond the fifth year the annual increments were nearly the same in all stocks. The whitefish from Whitefish Point, Dollar Settlement, and Marquette are among the fastest growing in the Great Lakes. The differences among the Lake Superior stocks in age and year-class composition, and in growth rate offer convincing evidence that populations of different areas are entirely independent. The sexes were almost equally represented (51.5 percent males) in the combined Bayfield samples, but males were scarce in age groups older than VIII. Whitefish from Bayfield shorter than 14.5 inches were immature and those larger than 17.4 inches were mature. The youngest mature fish belonged to age-group V,and all older than the VII group were mature.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Fishery Bulletin","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"U.S. Fish and Wildlife Service","usgsCitation":"Dryer, W.R., 1963, Age and growth of the whitefish in Lake Superior: Fishery Bulletin, v. 63, no. 1, p. 77-95.","productDescription":"19 p.","startPage":"77","endPage":"95","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":128720,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":266925,"type":{"id":11,"text":"Document"},"url":"https://fishbull.noaa.gov/63-1/dryer.pdf"}],"volume":"63","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae3e4b07f02db6896d5","contributors":{"authors":[{"text":"Dryer, William R.","contributorId":71921,"corporation":false,"usgs":true,"family":"Dryer","given":"William","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":308130,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70161319,"text":"70161319 - 1962 - Studies of transmission of mycobacterial infections in Chinook salmon","interactions":[],"lastModifiedDate":"2016-01-05T11:49:33","indexId":"70161319","displayToPublicDate":"2015-09-07T05:15:00","publicationYear":"1962","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3196,"text":"Progressive Fish-Culturist","active":true,"publicationSubtype":{"id":10}},"title":"Studies of transmission of mycobacterial infections in Chinook salmon","docAbstract":"

THE INCLUSION OF VISCERA AND CARCASSES OF TUBERCULOUS ADULT SALMON IN THE DIET OF JUVENILE SALMONIDS is considered to be the major source of mycobacterial infections in hatchery-reared fish (Wood and Ordal, 1958; Ross, Earp, and Wood, 1959). In considering additional modes of infection, we speculated about transovarian transmission or a mechanical process arising from contamination of the ova at the egg-taking stage with subsequent entry of the bacteria into the egg at the time of fertilization. This paper is a report on observations made during an experiment designed to test the latter theories.

","language":"English","publisher":"Bureau of Fisheries, U.S. Department of Commerce","doi":"10.1577/1548-8659(1962)24[147:SOTOMI]2.0.CO;2","usgsCitation":"Ross, A.J., and Johnson, H., 1962, Studies of transmission of mycobacterial infections in Chinook salmon: Progressive Fish-Culturist, v. 24, no. 4, p. 147-149, https://doi.org/10.1577/1548-8659(1962)24[147:SOTOMI]2.0.CO;2.","productDescription":"3 p.","startPage":"147","endPage":"149","numberOfPages":"3","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":654,"text":"Western Fisheries Research Center","active":true,"usgs":true}],"links":[{"id":313500,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"24","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"568cf74ae4b0e7a44bc0f18e","contributors":{"authors":[{"text":"Ross, A. J.","contributorId":105267,"corporation":false,"usgs":true,"family":"Ross","given":"A.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":585730,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, H.E.","contributorId":56757,"corporation":false,"usgs":true,"family":"Johnson","given":"H.E.","email":"","affiliations":[],"preferred":false,"id":585731,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2535,"text":"wsp1607 - 1962 - Reconnaissance of ground-water resources in the Eastern Coal Field Region, Kentucky","interactions":[],"lastModifiedDate":"2012-02-02T00:05:29","indexId":"wsp1607","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"1607","title":"Reconnaissance of ground-water resources in the Eastern Coal Field Region, Kentucky","docAbstract":"In the Eastern Coal Field region of Kentucky, water is obtained from consolidated sedimentary rocks ranging in age from Devonian to Pennsylvanian and from unconsolidated sediments of Quaternary age. About 95 percent of the area is underlain by shale, sandstone, and coal of Pennsylvanian age. Principal factors governing the availability of water in the region are depth, topographic location, and the lithology of the aquifer penetrated. In general, the yield of the well increases as the depth increases. Wells drilled in topographic lows, such as valleys, are likely to yield more water than wells drilled on topographic highs, such as hills. Sand and gravel, present in thick beds in the alluvium along the Ohio River, form the most productive aquifer in the Eastern Coal Field. Of the consolidated rocks in the region sandstone strata are the best aquifers chiefly because joints, openings along bedding planes, and intergranular pore spaces are best developed in them. Shale also supplies water to many wells in the region, chiefly from joints and openings along bedding planes. Coal constitutes a very small part of the sedimentary section, but it yields water from fractures to many wells. Limestone yields water readily from solution cavities developed along joint and bedding-plane openings. \r\n\r\nThe availability of water in different parts of the region was determined chiefly by analyzing well data collected during the reconnaissance. The resulting water-availability maps, published as hydrologic investigations atlases (Price and others, 1961 a, b; Kilburn and others, 1961) were designed to be used in conjunction with this report. The maps were constructed by dividing the region into 5 physiographic areas, into 10 subareas based chiefly on lithologic facies, and, in the case of the Kanawha section, into 2 quality-of-water areas. The 5 physiographic areas are the Knobs, Mississippian Plateau, Cumberland Plateau section, Kanawha section, and Cumberland Mountain section. \r\n\r\nThe 10 subareas are as follows: \r\n\r\n1. The Chattanooga shale. This black shale yields only enough water for a minimum domestic supply-100 to 500 gpd (gallons per day). \r\n\r\n2. Mississippian-Devonian rocks exposed along Pine Mountain. These rocks consist of shale, limestone, and sandstone. The limestone yields water to springs, and faulted limestone and sandstone lying below drainage may yield several hundred gallons per minute to wells. \r\n\r\n3. Mississippian rocks exposed along the western margin of the region. These rocks consist of thick limestone underlain by shale. The limestone yields enough water for a modern domestic supply (more than 500 gpd) , and discharges as much as 100 gpm (gallons per minute) to springs. The shale yields only enough water for a minimum domestic supply. \r\n\r\n4. Subarea 1 of the Lee formation of Pennsylvanian age. The thin shaly rocks of this subarea generally yield only enough water for a minimum domestic supply. \r\n\r\n5. Subarea 2 of the Lee formation of Pennsylvanian age. This subarea is predominantly underlain by massive sandstones; it generally yields enough water for a modern domestic supply, and in some places, enough water for small public and industrial supplies. \r\n\r\n6. Subarea 1 of the Breathitt and Conemaugh formations of Pennsylvanian age. Rocks in this subarea contain more shale than sandstone. Wells in this subarea range from adequate for a minimum domestic supply to adequate for a modern domestic supply. \r\n\r\n7. Subarea 2 of the Breathitt formation of Pennsylvanian age and undifferentiated post-Lee Pennsylvanian rocks. Wells in this subarea yield enough water for a modern domestic supply, and in many places, enough water for small public and industrial supplies. \r\n\r\n8. Alluvium along the Ohio River. Mostly composed of glacial outwash sand and gravel, the alluvium is reported to yield as much as 360 gpm to wells. \r\n\r\n9. Alluvium along the Big Sandy River and lower reaches of its Tug and Levisa Forks. Where consisting mostly of sand, ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1607","usgsCitation":"Price, W.E., Mull, D.S., and Kilburn, C., 1962, Reconnaissance of ground-water resources in the Eastern Coal Field Region, Kentucky: U.S. Geological Survey Water Supply Paper 1607, iv, 56 p. :ill., maps ;24 cm. + plates folded in pocket., https://doi.org/10.3133/wsp1607.","productDescription":"iv, 56 p. :ill., maps ;24 cm. + plates folded in pocket.","costCenters":[],"links":[{"id":138579,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1607/report-thumb.jpg"},{"id":28766,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28767,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28768,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28769,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28770,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28771,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28772,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28773,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28774,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28775,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28776,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1607/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a69e4b07f02db63c1ba","contributors":{"authors":[{"text":"Price, William E.","contributorId":84740,"corporation":false,"usgs":true,"family":"Price","given":"William","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":145361,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mull, D. S.","contributorId":43331,"corporation":false,"usgs":true,"family":"Mull","given":"D.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":145359,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kilburn, Chabot","contributorId":83499,"corporation":false,"usgs":true,"family":"Kilburn","given":"Chabot","email":"","affiliations":[],"preferred":false,"id":145360,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}