{"pageNumber":"1617","pageRowStart":"40400","pageSize":"25","recordCount":40778,"records":[{"id":2145,"text":"wsp1619J - 1963 - Ground-water geology of Edwards County, Texas","interactions":[],"lastModifiedDate":"2024-09-23T22:02:33.617404","indexId":"wsp1619J","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":"1619","chapter":"J","title":"Ground-water geology of Edwards County, Texas","docAbstract":"

Edwards County occupies 2,075 square miles of the southern part of the Edwards Plateau in southwest Texas. In 1950 it had a population of 2,908. Its thin limestone soil supports the characteristic flora of a semiarid region. The county is underlain by nearly flat-lying beds of limestone and a few beds of shale and marl.

\n

The Glen Rose limestone of Cretaceous age, the oldest formation tapped by water wells in the county, yields small quantities of rather highly mineralized water. Springs in the Glen Rose discharge water that is generally less mineralized than that from wells. Nearly all the wells and springs tapping the Glen Rose are in the southeastern part of the county, where the Edwards and associated limestones have been removed by erosion or are very thin.

\n

The Comanche Peak, Edwards, and Georgetown limestones, collectively called the Edwards and associated limestones, underlie most of the county and form the principal aquifer. Generally, the water in the Edwards is under water-table conditions, but locally it may be artesian. The Edwards and associated limestones yield small to moderate quantities of water that is hard but otherwise of good chemical quality.

\n

The alluvium in the major stream valleys yields small to moderate quantities of hard water similar in quality to that of the Edwards and associated limestones.

\n

The main ground-water divides in the Edwards and associated limestones follow the topographic divides. Most of the ground water flows southward and either appears as springflow in the Nueces River drainage or flows underground into Kinney or Val Verde County. The remainder flows northward and ultimately appears as springflow in the South Llano River drainage.

\n

About 150,000 acre-feet of water is recharged annually to and discharged from the Edwards and associated limestones in Edwards County. Most of this water is available for additional development inasmuch as only about 900 acre-feet per year is currently being used; however, additional development of ground water will result in a reduction in streamflow.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1619J","isbn":"pbk","usgsCitation":"Long, A.T., 1963, Ground-water geology of Edwards County, Texas: U.S. Geological Survey Water Supply Paper 1619, Report: iv, 29 p.; 5 Plates: 32.00 x 28.25 inches or smaller, https://doi.org/10.3133/wsp1619J.","productDescription":"Report: iv, 29 p.; 5 Plates: 32.00 x 28.25 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":109997,"rank":8,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24826.htm","linkFileType":{"id":5,"text":"html"},"description":"24826"},{"id":27750,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619j/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27749,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619j/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27748,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619j/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27747,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619j/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27752,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1619j/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27751,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619j/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137816,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1619j/report-thumb.jpg"}],"country":"United States","state":"Texas","county":"Edwards County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-100.6999,30.2899],[-100.1183,30.2897],[-100.0347,30.287],[-99.7576,30.2882],[-99.7577,30.0772],[-99.9235,30.0772],[-99.9235,30.0809],[-99.9726,30.0796],[-99.9742,30.0425],[-99.9789,30.0214],[-99.9916,30.0205],[-99.9989,29.9166],[-100.0016,29.9093],[-100.0042,29.9019],[-100.0063,29.8983],[-100.011,29.8941],[-100.0169,29.89],[-100.021,29.8868],[-100.0226,29.8836],[-100.0237,29.8795],[-100.0232,29.874],[-100.021,29.868],[-100.0205,29.8639],[-100.0226,29.8589],[-100.0242,29.8534],[-100.0263,29.8493],[-100.0295,29.8479],[-100.0331,29.847],[-100.0347,29.8438],[-100.0326,29.8396],[-100.0295,29.8369],[-100.0279,29.8337],[-100.0274,29.8305],[-100.0279,29.8277],[-100.0274,29.8232],[-100.0268,29.82],[-100.0226,29.8163],[-100.0205,29.8131],[-100.0216,29.8103],[-100.0205,29.8062],[-100.0173,29.8007],[-100.0147,29.7984],[-100.0137,29.7957],[-100.0152,29.7938],[-100.0237,29.7902],[-100.0279,29.7879],[-100.0289,29.7851],[-100.0289,29.7824],[-100.03,29.7801],[-100.0331,29.7787],[-100.0352,29.7764],[-100.0336,29.7709],[-100.0268,29.7535],[-100.0226,29.7439],[-100.0231,29.7421],[-100.0252,29.7407],[-100.0289,29.7393],[-100.0305,29.7348],[-100.0284,29.7325],[-100.0263,29.7283],[-100.0252,29.7251],[-100.0257,29.7233],[-100.0624,29.7113],[-100.0521,29.7096],[-100.0462,29.7079],[-100.0443,29.6944],[-100.0408,29.6931],[-100.0384,29.6896],[-100.0315,29.6883],[-100.0275,29.6835],[-100.0172,29.6788],[-100.0192,29.6722],[-100.0261,29.667],[-100.0285,29.6657],[-100.0197,29.6492],[-100.0123,29.6396],[-100.0084,29.6375],[-100.0079,29.6318],[-100.0145,29.6237],[-100.111,29.6236],[-100.6992,29.6236],[-100.6999,30.2899]]]},\"properties\":{\"name\":\"Edwards\",\"state\":\"TX\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66db81","contributors":{"authors":[{"text":"Long, Archie T.","contributorId":65059,"corporation":false,"usgs":true,"family":"Long","given":"Archie","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":144736,"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":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":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

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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.

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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":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":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":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":61965,"text":"mr23 - 1962 - Manganese in the United States, exclusive of Alaska and Hawaii","interactions":[{"subject":{"id":46031,"text":"ofr6139 - 1961 - Manganese in the United States","indexId":"ofr6139","publicationYear":"1961","noYear":false,"title":"Manganese in the United States"},"predicate":"SUPERSEDED_BY","object":{"id":61965,"text":"mr23 - 1962 - Manganese in the United States, exclusive of Alaska and Hawaii","indexId":"mr23","publicationYear":"1962","noYear":false,"title":"Manganese in the United States, exclusive of Alaska and Hawaii"},"id":1}],"lastModifiedDate":"2025-05-22T17:03:19.184597","indexId":"mr23","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":324,"text":"Mineral Investigations Resource Map","code":"MR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"23","title":"Manganese in the United States, exclusive of Alaska and Hawaii","docAbstract":"

The manganese deposits in the United States (exclusive of Alaska and Hawaii) are shown on the accompanying map. The deposits have been divided into several genetic types distinguished on the map by symbols. The principal distinction is between syngenetic deposits, in which the manganese was deposited contemporaneously with the enclosing rocks, and epigenetic, in which manganese was introduced into sedimentary rocks after their deposition or into igneous rocks after solidification. Because hydrothermal, metamorphic, and particularly supergene processes modify and in places concentrate manganese minerals after deposition of the element, classification of many deposits is subject to uncertainties. A third category, deposits of unknown or uncertain origin, is therefore included also. Subdivisions of these principal categories are based on the geologic history subsequent to original accumulation of the syngenetic deposits, and on gross mineralogic nature of the epigenetic ones.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mr23","usgsCitation":"Crittenden, M., and Pavlides, L., 1962, Manganese in the United States, exclusive of Alaska and Hawaii: U.S. Geological Survey Mineral Investigations Resource Map 23, Report: 8 p.; 1 Plate: 64.13 x 40.59 inches, https://doi.org/10.3133/mr23.","productDescription":"Report: 8 p.; 1 Plate: 64.13 x 40.59 inches","costCenters":[],"links":[{"id":179867,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mr/23/report-thumb.jpg"},{"id":260419,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mr/23/plate-1.pdf"},{"id":486401,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/mr/23/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"3168000","country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -127.25,24.25 ], [ -127.25,49.25 ], [ -66.5,49.25 ], [ -66.5,24.25 ], [ -127.25,24.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a82e4b07f02db64ae18","contributors":{"authors":[{"text":"Crittenden, Max D.","contributorId":43404,"corporation":false,"usgs":true,"family":"Crittenden","given":"Max D.","affiliations":[],"preferred":false,"id":266620,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pavlides, Louis","contributorId":79444,"corporation":false,"usgs":true,"family":"Pavlides","given":"Louis","email":"","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":266621,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":52276,"text":"ofr62115 - 1962 - Geology of the Williston basin, North Dakota, Montana, and South Dakota, with reference to subsurface disposal of radioactive wastes","interactions":[],"lastModifiedDate":"2012-02-02T00:11:20","indexId":"ofr62115","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"62-115","title":"Geology of the Williston basin, North Dakota, Montana, and South Dakota, with reference to subsurface disposal of radioactive wastes","docAbstract":"The southern Williston basin, which underlies about 110,000 square miles #n North Dakota, South Dakota, and eastern Montana, is part of a large structural and sedimentary basin. Its surface is a flat to gently rolling plain, standing about 1,500 to 3,500 feet above sea level and locally studded by a few high buttes. The sedimentary sequence that fills the basin has a maximum thickness of about 16,700 feet and rests on Precambrian metamorphic rocks at depths of 500 to 13,900 feet below sea level. It contains rocks of every geologic system, from Cambrian to Quaternary. Rocks of Middle Cambrian through Middle Ordovician age are largely shale and sandstone, as much as 1,200 feet thick; rocks of Late Ordovician through Pennsylvanian age are largely limestone and dolomite, as much as 7,500 feet thick; and rocks of Permian through Tertiary age are predominantly shale and siltstone, as much as 8,000 feet thick. Pleistocene glacial drift mantles the northern and eastern parts of the area. Rocks of the Williston basin are gently folded and regional dips are 1? or less from the margins to the basin center. Dips on the flanks of the major anticlinal folds, the Nesson and cedar Creek anticlines and the Poplar and Bowdoin domes, generally are about 1? to 3? except on the steep west limb of the Cedar Creek anticline. The basin was shaped by Laramide orogeny during latest Cretaceous and early Tertiary time. Most of the present structural features, however, were initiated during the Precambrian and reactivated by several subsequent orogenies, of which the latest was the Laramide. The most important mineral resource of the area is oil, which is produced predominantly from the Paleozoic carbonate sequence and largely on three of the major anticlinal folds, and lignite, which is present near the surface in Paleocene rocks. \r\n\r\nThe subsurface disposal of radioactive wastes at some places in the Williston basin appears to be geographically and geologically feasible. Many sites, at which large quantities of wastes might be injected with minimal danger of contamination of fresh-water aquifers and-oil-producing strata, are available.. The strata and types of reservoirs that deserve primary consideration for waste disposal are the Winnipeg Formation of Middle Ordovician age as a deep salaquifer, the Permian to Jurassic salt beds as moderately deep-units in which solution cavities might be created for storage, the thick Upper Cretaceous shale beds as shallow hydraulically fractured shale reservoirs, and the Newcastle Sandstone of Early Cretaceous age as a shallow shale-enclosed sandstone reservoir.","language":"ENGLISH","doi":"10.3133/ofr62115","usgsCitation":"Sandberg, C.A., 1962, Geology of the Williston basin, North Dakota, Montana, and South Dakota, with reference to subsurface disposal of radioactive wastes: U.S. Geological Survey Open-File Report 62-115, 148 p., https://doi.org/10.3133/ofr62115.","productDescription":"148 p.","costCenters":[],"links":[{"id":179401,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0115/report-thumb.jpg"},{"id":86779,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0115/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86780,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0115/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86781,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0115/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86782,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0115/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c950","contributors":{"authors":[{"text":"Sandberg, C. A.","contributorId":86016,"corporation":false,"usgs":true,"family":"Sandberg","given":"C.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":245071,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":62042,"text":"mr29 - 1962 - Titanium in the United States, exclusive of Alaska and Hawaii","interactions":[{"subject":{"id":43993,"text":"ofr61130 - 1961 - Titanium in the United States","indexId":"ofr61130","publicationYear":"1961","noYear":false,"title":"Titanium in the United States"},"predicate":"SUPERSEDED_BY","object":{"id":62042,"text":"mr29 - 1962 - Titanium in the United States, exclusive of Alaska and Hawaii","indexId":"mr29","publicationYear":"1962","noYear":false,"title":"Titanium in the United States, exclusive of Alaska and Hawaii"},"id":1}],"lastModifiedDate":"2025-05-23T13:33:48.606875","indexId":"mr29","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":324,"text":"Mineral Investigations Resource Map","code":"MR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"29","title":"Titanium in the United States, exclusive of Alaska and Hawaii","docAbstract":"

The accompanying map shows the location of the principal deposits of titanium minerals in the United States (excluding Alaska and Hawaii). Four broad geologic categories of deposits have been distinguished on the map by the shapes of the symbols, and relative importance is indicated by their size. The smaller deposits and the deposits for which adequate data are lacking can only be rated as \"potential, unevaluated, or small\". The deposits placed in the next category have been characterized by modest production or can be described as having \"significant potential\". The larger deposits, for which, more information is available, arc divided into two categories, based on estimated production plus reserves: those containing 1,000,000 to 10,000,000 tons of TiO2, and those having more than 10,000,000 tons of TiO2.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mr29","usgsCitation":"Rogers, C.L., and Jaster, M.C., 1962, Titanium in the United States, exclusive of Alaska and Hawaii: U.S. Geological Survey Mineral Investigations Resource Map 29, Report: 18 p.; 1 Plate: 63.97 x 40.50 inches, https://doi.org/10.3133/mr29.","productDescription":"Report: 18 p.; 1 Plate: 63.97 x 40.50 inches","costCenters":[],"links":[{"id":180500,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mr/29/report-thumb.jpg"},{"id":486413,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/mr/29/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":260488,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mr/29/plate-1.pdf"}],"scale":"3168000","country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -127.25,24.25 ], [ -127.25,49.25 ], [ -66.5,49.25 ], [ -66.5,24.25 ], [ -127.25,24.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699a4c","contributors":{"authors":[{"text":"Rogers, Cleaves Lincoln","contributorId":12858,"corporation":false,"usgs":true,"family":"Rogers","given":"Cleaves","email":"","middleInitial":"Lincoln","affiliations":[],"preferred":false,"id":266767,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jaster, Marion Charlotte","contributorId":27117,"corporation":false,"usgs":true,"family":"Jaster","given":"Marion","email":"","middleInitial":"Charlotte","affiliations":[],"preferred":false,"id":266768,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":52271,"text":"ofr62107 - 1962 - Hydraulic model studies--stream gaging control structure for Carrizo-Corduroy Project, Arizona","interactions":[],"lastModifiedDate":"2013-08-01T15:16:00","indexId":"ofr62107","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"62-107","title":"Hydraulic model studies--stream gaging control structure for Carrizo-Corduroy Project, Arizona","language":"ENGLISH","doi":"10.3133/ofr62107","usgsCitation":"Richardson, E., 1962, Hydraulic model studies--stream gaging control structure for Carrizo-Corduroy Project, Arizona: U.S. Geological Survey Open-File Report 62-107, 42 p., https://doi.org/10.3133/ofr62107.","productDescription":"42 p.","costCenters":[],"links":[{"id":179396,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0107/report-thumb.jpg"},{"id":275860,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0107/report.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db62a1f4","contributors":{"authors":[{"text":"Richardson, E.V.","contributorId":105697,"corporation":false,"usgs":true,"family":"Richardson","given":"E.V.","email":"","affiliations":[],"preferred":false,"id":245066,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1333,"text":"wsp1536E - 1962 - Theory of aquifer tests","interactions":[],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1536E","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":"1536","chapter":"E","title":"Theory of aquifer tests","docAbstract":"The development of water supplies from wells was placed on a rational basis with Darcy's development of the law governing the movement of fluids through sands and with Dupuit's application of that law to the problem of radial flow toward a pumped well. As field experience increased, confidence in the applicability of quantitative methods was gained and interest in developing solutions for more complex hydrologic problems was stimulated. An important milestone was Theis' development in 1935 of a solution for the nonsteady flow of ground water, which enabled hydrologists for the first time to predict future changes in ground-water levels resulting from pumping or recharging of wells. In the quarter century since, quantitative ground-water hydrology has been enlarging so rapidly as to discourage the preparation of comprehensive textbooks. \r\n\r\nThis report surveys developments in fluid mechanics that apply to groundwater hydrology. It emphasizes concepts and principles, and the delineation of limits of applicability of mathematical models for analysis of flow systems in the field. It stresses the importance of the geologic variable and its role in governing the flow regimen. \r\n\r\nThe report discusses the origin, occurrence, and motion of underground water in relation to the development of terminology and analytic expressions for selected flow systems. It describes the underlying assumptions necessary for mathematical treatment of these flow systems, with particular reference to the way in which the assumptions limit the validity of the treatment.","language":"ENGLISH","publisher":"U.S. Government Print. Office,","doi":"10.3133/wsp1536E","usgsCitation":"Ferris, J., Knowles, D., Brown, R.H., and Stallman, R., 1962, Theory of aquifer tests: U.S. Geological Survey Water Supply Paper 1536, vii, 105 p. :ill. ;24 cm., https://doi.org/10.3133/wsp1536E.","productDescription":"vii, 105 p. :ill. ;24 cm.","costCenters":[],"links":[{"id":12,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wsp1536-E","linkFileType":{"id":5,"text":"html"}},{"id":137382,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0de4b07f02db5fd475","contributors":{"authors":[{"text":"Ferris, J.G.","contributorId":12453,"corporation":false,"usgs":true,"family":"Ferris","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":143577,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Knowles, D.B.","contributorId":83898,"corporation":false,"usgs":true,"family":"Knowles","given":"D.B.","email":"","affiliations":[],"preferred":false,"id":143580,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brown, R. H.","contributorId":19931,"corporation":false,"usgs":false,"family":"Brown","given":"R.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143578,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Stallman, R.H.","contributorId":55800,"corporation":false,"usgs":true,"family":"Stallman","given":"R.H.","email":"","affiliations":[],"preferred":false,"id":143579,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1767,"text":"wsp1499C - 1962 - Water resources of the Utica-Rome area, New York","interactions":[],"lastModifiedDate":"2021-12-13T21:17:31.346876","indexId":"wsp1499C","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":"1499","chapter":"C","title":"Water resources of the Utica-Rome area, New York","docAbstract":"The Utica-Rome area is along the Mohawk River and New York State Erie (Barge) Canal about midway between Lake Ontario and Albany. It encompasses about 390 square miles centered around the industrial cities of Utica and Rome. The Mohawk River, its tributary West Canada Creek, and a system of reservoirs and diversions to maintain the flow in the barge-canal system, assure an ample water supply for the foreseeable needs of the area. The water from these sources is generally of good chemical quality requiring little treatment, although that from the Mohawk River is only fair and may require some treatment for sensitive industrial processes. Additional surface water is available from smaller streams in the area, particularly Oriskany and Sauquoit Creeks, but the water from these sources is hard, and has a dissolved-solids content of more than 250 ppm (parts per million). Ground water is available in moderate quantities from unconsolidated sand and gravel deposits in the river valleys and buried bedrock channels, and in small quantities from bedrock formations and less permeable unconsolidated deposits. The quality of water from sand and gravel, and bedrock ranges from good to poor. However, where necessary, the quality can be improved with treatment. \r\n\r\nThe Mohawk River is the source of the largest quantity of water in the area. The flow of the stream below Delta Dam equals or exceeds 108 mgd (million gallons per day) 90 percent of the time, and at Little Falls it equals or exceeds 560 mgd 90 percent of the time. The flow between these two points is increased by additions from Oriskany, Sauquoit, and West Canada Creeks and from many smaller tributary streams. The flow is also increased by diversions from outside the area, from the Black and Chenango Rivers and West Canada Creek for improvement of navigation in the Erie (Barge) Canal, and from West Canada and East Branch Fish Creeks for the public supplies of Utica and Rome. Much of the public-supply water eventually reaches the river by way of sewerage and industrial waste-disposal systems. The total diversion from these sources averages more than 92 mgd. An estimated 18.5 mgd is withdrawn from the Mohawk River by industry, mostly for nonconsumptive uses. \r\n\r\nFloods in the Utica-Rome area are not a frequent problem owing to the use of regulatory measures. The major streams fluctuate through a narrow range in stage and generally only a narrow strip along the streams is subject to flooding. Water-bearing sand and gravel deposits in the major river valleys are the principal sources of ground water, especially where they are recharged by infiltration from streams. The most important potential source is the deposit of sand and gravel underlying the extensive plain adjacent to the Mohawk River between Delta Reservoir and Rome. Maximum sustained yields from these deposits are not known; but moderate quantities of water, 300 gpm (gallons per minute) or less from a single well, can probably be obtained from some parts of the sand plain area, particularly in the vicinity of a buried bedrock channel that extends southwestward from Delta Reservoir. Similar quantities of ground water probably can be withdrawn from some parts of the flood plain of the Mohawk River between Rome and Frankfort and from the sand and gravel deposits filling the valley of Ninemile Creek below Holland Patent. The deposits underlying the flood plain of the Mohawk River generally are fine grained but in places contain interstratified beds of coarser sand and gravel. The most productive part of the flood plain is at the east end near Frankfort. The deposits in Ninemile Creek valley also are generally fine grained; but where they are sufficiently thick, as over a buried bedrock valley southwest of Floyd, moderate quantities of water may be obtained. \r\n\r\nSmall to moderate quantities of water (150 gpm or less from a single well) can be obtained from sand and gravel deposits in the bottoms of Oriskany and Sauquoit Creek vall","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1499C","usgsCitation":"Halberg, H., Hunt, O.P., and Pauszek, F.H., 1962, Water resources of the Utica-Rome area, New York: U.S. Geological Survey Water Supply Paper 1499, Report: iv, 46 p.; 3 Plates: 21.00 × 17.15 inches or smaller, https://doi.org/10.3133/wsp1499C.","productDescription":"Report: iv, 46 p.; 3 Plates: 21.00 × 17.15 inches or smaller","costCenters":[],"links":[{"id":26891,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499c/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26890,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499c/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26889,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137141,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499c/report-thumb.jpg"},{"id":26892,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":392829,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24439.htm"}],"country":"United States","state":"New York","city":"Rome, Utica","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.59417724609375,\n 43.018705515824635\n ],\n [\n -75.10528564453125,\n 43.018705515824635\n ],\n [\n -75.10528564453125,\n 43.29120116988416\n ],\n [\n -75.59417724609375,\n 43.29120116988416\n ],\n [\n -75.59417724609375,\n 43.018705515824635\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dfe4b07f02db5e3376","contributors":{"authors":[{"text":"Halberg, Henry N.","contributorId":19929,"corporation":false,"usgs":true,"family":"Halberg","given":"Henry N.","affiliations":[],"preferred":false,"id":144113,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hunt, O. P.","contributorId":69116,"corporation":false,"usgs":true,"family":"Hunt","given":"O.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":144115,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pauszek, F. H.","contributorId":61399,"corporation":false,"usgs":true,"family":"Pauszek","given":"F.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144114,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":3506,"text":"cir468 - 1962 - Ground-water studies and analog models","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"cir468","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"468","title":"Ground-water studies and analog models","docAbstract":"Hydrologists make ground-water studies to aid managers and users of water resources in solving their problems in the development and management of ground water. Geologic and hydrologic information provides the basic knowledge for construction of electric analog models that portray the ground-water system in miniature. Analog models can be analyzed electrically, and the results of the analysis are presented in terms of the ground-water system so that the effects of alternative methods of water development can be assessed.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/cir468","usgsCitation":"Robinove, C.J., 1962, Ground-water studies and analog models: U.S. Geological Survey Circular 468, 12 p. :ill. ;27 cm., https://doi.org/10.3133/cir468.","productDescription":"12 p. :ill. ;27 cm.","costCenters":[],"links":[{"id":123185,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1962/0468/report-thumb.jpg"},{"id":30520,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1962/0468/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db696865","contributors":{"authors":[{"text":"Robinove, Charles Joseph","contributorId":71153,"corporation":false,"usgs":true,"family":"Robinove","given":"Charles","email":"","middleInitial":"Joseph","affiliations":[],"preferred":false,"id":147055,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2231,"text":"wsp1599 - 1962 - Reconnaissance of ground-water resources in the Western Coal Field Region, Kentucky","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1599","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":"1599","title":"Reconnaissance of ground-water resources in the Western Coal Field Region, Kentucky","docAbstract":"In the Western Coal Field region of Kentucky, water is obtained from consolidated sedimentary rocks of Mississippian and Pennsylvanian ages and from unconsolidated sediments of Cenozoic age. Pennsylvanian rocks crop out in more than 95 percent of the area and consist of shale and sandstone interbedded with some limestone and coal. The Pennsylvanian strata are divided into five formations. They are, in ascending order: the Caseyville sandstone and the Tradewater, Carbondale, Lisman, and Henshaw formations. The Anvil Rock sandstone member of the Lisman formation and the Caseyville sandstone are the only bedrock aquifers in the region that are known to yield more than 100 gpm (gallons per minute) to wells. Most bedrock wells produce enough water for a modern domestic supply, more than 500 gpd (gallons per day), and few yield so little water as to be inadequate for hand pumps and bailers, less than 100 gpd. \r\n\r\nUnconsolidated Cenozoic deposits range from latest Pliocene(?) to Recent in age and consist of clay, silt, sand, and gravel. High gravels, tentatively considered to be late Pliocene and early Pleistacene in age by McFarlan (1950, p. 125), and loess of Pleistocene age are locally exposed, but nearly all of the alluvium is of late Pleistocene and Recent ages. The alluvium along the Ohio River generally yields from a few hundred to as much as 1,000 gpm to single vertical wells and as much as several thousand gallons per minute to wells that have multiple horizontal screens. Alluvium in the tributaries of the Ohio River generally is finer grained than that of the Ohio Valley. The highest known yield from a well in the alluvium of the tributaries is 56 gpm; other wells yield enough for domestic supplies. \r\n\r\nAvailability of ground water in the region depends on the character and thickness of the aquifer penetrated, and, where the aquifer is bedrock on the depth of the water-bearing bed, and to a certain extent on the topographic situation. Most bedrock aquifers in the Western Coal Field region are sandstone and may vary greatly in thickness and composition within short distances. The region is divided into five areas of ground-water availability. Area 1 is confined to the Ohio Valley, most of which is underlain by relatively thick sections of sand and gravel that yield at least 50 gpm to most wells at depths of less than 150 feet. In area 2 most wells yield enough water for a modern domestic supply from depths of less than 300 feet. This area includes the largest part of the bedrock outcrop in the region, some of the alluvial area along the Ohio River, and much of the alluvial areas along the larger tributaries. In area 3 most wells yield enough water from depths of less than 300 feet to supply domestic needs when a hand pump is used. This area covers the bedrock parts of the region that are underlain by shale, sandy shale, and limestone, and the section where few wells are known to yield large supplies of water. In area 4 most wells fail to supply enough water for domestic use from depths of less than 300 feet, probably because they penetrate thick sections of unfractured shale or well-cemented sandstone. In area 5 the yield of wells is unpredictable, commonly because of faulting. \r\n\r\nThe water in the shallow bedrock aquifers of the region is mostly of the sodium bicarbonate or the calcium bicarbonate type. Saline water has been encountered at depths as shallow as 100 feet, but fresh water has been obtained at depths approaching 1,000 feet. Water from the bedrock is soft to moderately hard, but it may contain undesirable amounts of iron. Most water from the alluvium is of the calcium bicarbonate type and is generally harder and contains more iron than water from the bedrock.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1599","usgsCitation":"Maxwell, B.W., and Devaul, R.W., 1962, Reconnaissance of ground-water resources in the Western Coal Field Region, Kentucky: U.S. Geological Survey Water Supply Paper 1599, vi, 34 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1599.","productDescription":"vi, 34 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":137734,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1599/report-thumb.jpg"},{"id":247195,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1599/plate-table_4.pdf","size":"791","linkFileType":{"id":1,"text":"pdf"}},{"id":27985,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1599/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27986,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1599/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27987,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1599/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27988,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1599/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a64e4b07f02db637b34","contributors":{"authors":[{"text":"Maxwell, Bruce William","contributorId":67489,"corporation":false,"usgs":true,"family":"Maxwell","given":"Bruce","email":"","middleInitial":"William","affiliations":[],"preferred":false,"id":144860,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Devaul, Robert Washburn","contributorId":84338,"corporation":false,"usgs":true,"family":"Devaul","given":"Robert","email":"","middleInitial":"Washburn","affiliations":[],"preferred":false,"id":144861,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1115,"text":"wsp1535G - 1962 - Rainwater as a chemical agent of geologic processes; a review","interactions":[],"lastModifiedDate":"2013-08-12T12:37:51","indexId":"wsp1535G","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":"1535","chapter":"G","title":"Rainwater as a chemical agent of geologic processes; a review","docAbstract":"Chemical analyses of the rainwater collected at several localities are given to show the variations of the principal constitutents. In rock weathering and soil-forming processes, the chemical composition of rainwater has an important effect which has been evaluated for only a few arid areas. In humid regions the important amounts of calcium, magnesium, sodium, and potassium added yearly by rain may be expected to influence the composition of the soil water and thereby the cations in the exchange positions of soil clay minerals. The acquisition of cations by clay minerals may slow down chemical weathering. The stability of soil clay minerals is influenced by the constant accession of cations from rainwater. Conversely, the clay minerals modify the amounts and kinds of cations that are leached out by drainage waters. The stability of micaceous minerals in soils may be partly due to accessions of K +1 ions from rainwater. \n\nThe pH of rainwater in any area varies considerably and seems to form a seasonal and regional pattern. The recorded pH values range from 3.0 to 9.8.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1535G","usgsCitation":"Carroll, D., 1962, Rainwater as a chemical agent of geologic processes; a review: U.S. Geological Survey Water Supply Paper 1535, 18 p., 1 leaf of plates ;23 cm. Reprinted 1965, https://doi.org/10.3133/wsp1535G.","productDescription":"18 p., 1 leaf of plates ;23 cm. Reprinted 1965","costCenters":[],"links":[{"id":138099,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1535g/report-thumb.jpg"},{"id":25877,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1535g/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":276517,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1535g/plate-1.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649593","contributors":{"authors":[{"text":"Carroll, Dorothy","contributorId":38534,"corporation":false,"usgs":true,"family":"Carroll","given":"Dorothy","email":"","affiliations":[],"preferred":false,"id":143201,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}