{"pageNumber":"1616","pageRowStart":"40375","pageSize":"25","recordCount":40778,"records":[{"id":70221183,"text":"70221183 - 1964 - Relation of temperature distribution to ground-water movement in carbonate rocks of central Israel","interactions":[],"lastModifiedDate":"2021-06-04T17:34:58.608687","indexId":"70221183","displayToPublicDate":"1964-03-01T12:31:10","publicationYear":"1964","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":"Relation of temperature distribution to ground-water movement in carbonate rocks of central Israel","docAbstract":"

The Cenomanian-Turonian formations of central Israel constitute a highly permeable dolomite and limestone aquifer. In this area it is on the west limb of an anticlinorium that trends north-northeast, and it contains water under artesian pressure. A graph of water temperatures and well depths suggests that there is a very small vertical temperature gradient in local segments of the aquifer. The small gradient is believed to result from a large vertical component of flow that tends to equalize the vertical temperature distribution. On a regional scale the apparent horizontal temperature distribution indicates a westward increase with increasing depth of the aquifer, suggesting a manifestation of the regional geothermal gradient. The westward increase in temperature also implies that the lateral component of flow may be in the normal range for artesian carbonate-rock aquifers whose pores consist mainly of solution cavities. Locally, pumping appears to have affected the temperature distribution by modifying the natural flow pattern. In parts of the most intensively developed area, the aquifer is hydraulically connected with overlying coastal-plain deposits, and some cooler water has been induced to move into the aquifer from this source. At three other areas, pumping has resulted in an apparent horizontal shift of the isotherms on a temperature-distribution map. The data suggest that the spatial distribution of temperature may be used to determine some of the flow characteristics of carbonate-rock aquifers.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1964)75[209:ROTDTG]2.0.CO;2","usgsCitation":"Schneider, R., 1964, Relation of temperature distribution to ground-water movement in carbonate rocks of central Israel: Geological Society of America Bulletin, v. 75, no. 3, p. 209-216, https://doi.org/10.1130/0016-7606(1964)75[209:ROTDTG]2.0.CO;2.","productDescription":"8 p.","startPage":"209","endPage":"216","costCenters":[],"links":[{"id":386224,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Israel","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n 35.57373046875,\n 33.284619968887675\n ],\n [\n 35.430908203125,\n 33.100745405144245\n ],\n [\n 35.13427734375,\n 33.100745405144245\n ],\n [\n 34.1455078125,\n 31.372399104880525\n ],\n [\n 34.9365234375,\n 29.458731185355344\n ],\n [\n 35.595703125,\n 32.13840869677249\n ],\n [\n 35.57373046875,\n 33.284619968887675\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"75","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Schneider, Robert","contributorId":102460,"corporation":false,"usgs":true,"family":"Schneider","given":"Robert","email":"","affiliations":[],"preferred":false,"id":817001,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2404,"text":"wsp1749 - 1964 - Geology and ground-water resources of Nobles County, and part of Jackson County, Minnesota","interactions":[],"lastModifiedDate":"2023-04-11T18:27:13.54031","indexId":"wsp1749","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1749","title":"Geology and ground-water resources of Nobles County, and part of Jackson County, Minnesota","docAbstract":"

The area described in this report is in southwestern Minnesota, about 130 miles southwest of Minneapolis and St. Paul. It includes; Nobles County and the western tier of townships in Jackson County, a total of 864 square miles. Worthington, the Nobles County seat, is the largest city in the area, having a population of 9,015 persons (1960 census). Farming is the leading occupation, and food processing is the major industry. Critical water shortages have occurred in several parts of the area.

\n

The climate is characterized by mild, subhumid summers and relatively long, severe winters. Mean monthly temperatures range from 15.1 °F in January to 73.3 °F in July. The mean annual precipitation is 26.75 inches.

\n

The crest of the Coteau des Prairies, a broad highland belt, traverses Nobles County from northwest to southeast. Three glacial end moraines and their associated ground moraines trend south to southeast across the area. Altitudes range from about 1,820 feet on the crest of the coteau in the northwestern part of the area to about 1,390 feet above mean sea level in the Jack and Okabena Creek valleys in the northeast.

\n

The Mississippi-Missouri River drainage divide crosses the area from north to east. The Gary outer end moraine trends southeast through central Nobles County. East of this moraine the land is poorly drained and contains numerous lakes and swamps; west of this moraine the land is well drained and contains few, if any, undrained depressions.

\n

Within the area, granite and Sioux Quartzite of Precambrian age are overlain by Cretaceous strata, except locally in the northeast and northwest parts of the area where the quartzite is directly overlain by glacial drift. The Cretaceous strata are composed of interbedded shale, siltstone, and sandstone. The surface of the area is composed of Pleistocene deposits of glacial drift and some thin, patchy deposits of Recent age. Bedrock is not known to crop out in the area. The drift ranges in thickness from about 150 feet in the southwest and northeast corners to about 500 feet on the highest part of the Coteau des Prairies.

\n

The Precambrian granite is not a source of ground water in this area. The Sioux Quartzite yields moderate supplies in adjacent counties to the north and west, but because of its sporadic occurrence it does not constitute an important water source in this area. The Cretaceous sandstone units are a secondary source of ground water and yield adequate supplies 'to at least 24 farm wells, which range in depth from 283 to 586 feet below land surface.

\n

The primary source of ground water in the Nobles-Jackson County area is the glacial drift. Buried outwash deposits supply water to 7 of the 10 municipalities and to most of the farms in the area. Two Worthington city wells, completed in a buried outwash deposit underlying East Okabena dry lake bed, were tested for short periods at 500 gallons per minute. The estimated coefficient of transmissibility for the aquifer at one of the wells was 70,000 gpd (gallons per day) per ft.

\n

The buried outwash deposits may occur anywhere within the drift from about 15 feet below land surface to bedrock which is as much as 500 feet below land surface. The outwash ranges from a fraction of a foot to more than 25 feet in thickness where permeable; below the water table it generally will supply ample quantities of water to properly constructed wells.

\n

Surflcial outwash deposits fill the valley bottoms and form the terrace deposits associated with the present-day drainage channels. The thicker, more extensive, and continuous deposits occur in the proglacial stream channels that drained the fronts of the ice sheets rather than in those channels that now drain the backs of the moraines. The surflcial outwash deposits generally are made up of sand, gravel and some silt and clay, and range in thickness from 0 to more than 60 feet; they range in width from a few feet in the narrow tributaries to about one mile in the larger stream valleys.

\n

Four municipalities and many farms obtain part or all of their water supplies from surficial outwash. An Adrian municipal well, completed in this source, was pumped at a rate of 400 gpm. At the confluence of two streams which drain Ocheda Lake in southeastern Nobles County, the sand and gravel section is more than 60 feet thick in places. Results of a pumping test here showed an average coefficient of transmissibility of 150,000 gpd per ft. Coefficients of transmissibility may be as much as 500,000 gdp per ft in the thickest part of the deposit if the permeability of the sand and gravel is uniform.

\n

Recharge to the surflcial outwash deposits is relatively rapid; it is slower to the buried outwash deposits where the descending water must percolate through till of low permeability before entering the aquifers.

\n

The quality of water in the Precambrian crystalline rocks, the Cretaceous strata, and the buried Pleistocene aquifers is poor. Chemical analyses of 22 water samples showed that dissolved solids ranged from 1,100 ppm (parts per million) to 3,050 ppm. Water from the surficial outwash deposits is good by comparison; dissolved solids in water from these aquifers ranged from 425 to 870 ppm.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1749","collaboration":"Prepared in cooperation with the Division of Waters, Minnesota Department of Conservation, and the city of Worthington","usgsCitation":"Norvitch, R.F., 1964, Geology and ground-water resources of Nobles County, and part of Jackson County, Minnesota: U.S. Geological Survey Water Supply Paper 1749, Document: iv, 70 p.; 5 Plates: 23.0 x 23.5 inches or smaller, https://doi.org/10.3133/wsp1749.","productDescription":"Document: iv, 70 p.; 5 Plates: 23.0 x 23.5 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":28402,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1749/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28399,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1749/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28404,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1749/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":415582,"rank":8,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24926.htm","linkFileType":{"id":5,"text":"html"}},{"id":28403,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1749/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28400,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1749/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139050,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1749/report-thumb.jpg"},{"id":28401,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1749/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Minnesota","county":"Jackson County, Nobles County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -96.051,\n 43.847\n ],\n [\n -96.051,\n 43.5\n ],\n [\n -95.336,\n 43.5\n ],\n [\n -95.336,\n 43.847\n ],\n [\n -96.051,\n 43.847\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685a7f","contributors":{"authors":[{"text":"Norvitch, Ralph F.","contributorId":65456,"corporation":false,"usgs":true,"family":"Norvitch","given":"Ralph","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":145148,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":52426,"text":"ofr64128 - 1964 - Ground-water reconnaissance in the Burnt River valley, Baker County, Oregon","interactions":[],"lastModifiedDate":"2025-12-04T19:36:52.263227","indexId":"ofr64128","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","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":"64-128","title":"Ground-water reconnaissance in the Burnt River valley, Baker County, Oregon","docAbstract":"

The Burnt River valley in southern Baker County, Oreg., is underlain by rocks that range in age from pre-Tertiary to Quaternary. The pre-Tertiary rocks consist mainly of argillites, schists, limestones, and intrusive igneous rocks, while the Tertiary rocks consist mainly of felsic and mafic volcanic tuffs, lava flows and breccias, and fluviolacustrine deposits. Quaternary rocks include terrace gravels of Pleistocene and Recent age, and stream-valley alluvium of Recent age. The rock units most widely exposed along the valley are the fluviolacustrine deposits of Miocene and Pliocene(?) age, which extend to depths of as much as a thousand feet below the valley floor, and the pre-Tertiary rocks.

Most of the rocks that underlie the valley are of relatively low permeability and yield only small to moderate quantities of water (generally less than 50 gpm) to wells. The fluviolacustrine deposits contain scattered lenses of relatively permeable sand and gravel, hut the unit as a whole is mainly silt and clay of low permeability. Two prospective irrigation wells in the area penetrated these deposits but were abandoned because of insufficient yield.

Perhaps the most permeable rock unit in the area is the Columbia River Basalt of Miocene and Pliocene(?) age. It is exposed extensively west of the main valley, but apparently occurs only' as discontinuous lenses beneath the valley floor.

Chemical analyses of water from seven wells in the area indicate that the ground waters have relatively large concentrations of dis-. solved mineral constituents. Water from two of the wells had excessive concentrations of boron and high sodium and salinity hazards with respect to use for irrigation.

Perhaps the most favorable site for a test irrigation well is about 8 to 10 miles east of Hereford, where the Columbia River Basalt apparently extends beneath, and is intercalated with, the fluviolacustrine deposits.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr64128","collaboration":"Prepared in cooperation with the U.S. Bureau of Reclamation","usgsCitation":"Price, D., 1964, Ground-water reconnaissance in the Burnt River valley, Baker County, Oregon: U.S. Geological Survey Open-File Report 64-128, Report: 31 p.; 2 Figures: 29.69 x 29.91 inches and 36.75 x 20.21 inches, https://doi.org/10.3133/ofr64128.","productDescription":"Report: 31 p.; 2 Figures: 29.69 x 29.91 inches and 36.75 x 20.21 inches","costCenters":[],"links":[{"id":497027,"rank":4,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1964/0128/figure-2B.pdf","text":"Figure 2B","linkFileType":{"id":1,"text":"pdf"}},{"id":497026,"rank":3,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1964/0128/figure-2A.pdf","text":"Figure 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa7e4b07f02db66710a","contributors":{"authors":[{"text":"Price, Don","contributorId":30608,"corporation":false,"usgs":true,"family":"Price","given":"Don","email":"","affiliations":[],"preferred":false,"id":245325,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010550,"text":"70010550 - 1964 - Fused rock from Köfels, Tyrol","interactions":[],"lastModifiedDate":"2015-06-19T14:44:24","indexId":"70010550","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3659,"text":"Tschermaks Mineralogische und Petrographische Mitteilungen","active":true,"publicationSubtype":{"id":10}},"title":"Fused rock from Köfels, Tyrol","docAbstract":"

The vesicular glass from Köfels, Tyrol, contains grains of quartz that have been partially melted but not dissolved in the matrix glass. This phenomenon has been observed in similar glasses formed by friction along a thrust fault and by meteorite impact, but not in volcanic glasses. The explosion of a small nuclear device buried behind a steep slope produced a geologic structure that is a good small-scale model of that at Köfels. Impact of a large meteorite would have an effect analogous to that of a subsurface nuclear explosion and is the probable cause of the Köfels feature.

","language":"English","publisher":"Springer","doi":"10.1007/BF01127777","issn":"00413763","usgsCitation":"Milton, D.J., 1964, Fused rock from Köfels, Tyrol: Tschermaks Mineralogische und Petrographische Mitteilungen, v. 9, no. 1-2, p. 86-94, https://doi.org/10.1007/BF01127777.","productDescription":"9 p.","startPage":"86","endPage":"94","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":218903,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":204895,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF01127777"}],"volume":"9","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a142de4b0c8380cd5493d","contributors":{"authors":[{"text":"Milton, Daniel J.","contributorId":54963,"corporation":false,"usgs":true,"family":"Milton","given":"Daniel","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":359155,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1007574,"text":"1007574 - 1964 - 1,1' diacetyl-1,1'-dihydro-4,4' bipyridine and the yellow and colorless modifications of 1,1'-diacetyl-1,1',4,4'-tetrahydro-4,4' bipyridine","interactions":[],"lastModifiedDate":"2013-02-23T21:58:33","indexId":"1007574","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2408,"text":"Journal of Organic Chemistry","active":true,"publicationSubtype":{"id":10}},"title":"1,1' diacetyl-1,1'-dihydro-4,4' bipyridine and the yellow and colorless modifications of 1,1'-diacetyl-1,1',4,4'-tetrahydro-4,4' bipyridine","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Journal of Organic Chemistry","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"American Chemical Society","doi":"10.1021/jo01031a016","usgsCitation":"Nielsen, A., Moore, D.W., Muha, G., and Highberg, K., 1964, 1,1' diacetyl-1,1'-dihydro-4,4' bipyridine and the yellow and colorless modifications of 1,1'-diacetyl-1,1',4,4'-tetrahydro-4,4' bipyridine: Journal of Organic Chemistry, v. 29, no. 8, p. 2175-2179, https://doi.org/10.1021/jo01031a016.","startPage":"2175","endPage":"2179","numberOfPages":"5","costCenters":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"links":[{"id":268064,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1021/jo01031a016"},{"id":130194,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"29","issue":"8","noUsgsAuthors":false,"publicationDate":"2002-05-01","publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e55e","contributors":{"authors":[{"text":"Nielsen, A.T.","contributorId":62551,"corporation":false,"usgs":true,"family":"Nielsen","given":"A.T.","email":"","affiliations":[],"preferred":false,"id":315650,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Moore, D. W.","contributorId":93431,"corporation":false,"usgs":true,"family":"Moore","given":"D.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":315653,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Muha, G.M.","contributorId":78687,"corporation":false,"usgs":true,"family":"Muha","given":"G.M.","email":"","affiliations":[],"preferred":false,"id":315651,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Highberg, K.","contributorId":90673,"corporation":false,"usgs":true,"family":"Highberg","given":"K.","email":"","affiliations":[],"preferred":false,"id":315652,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1000379,"text":"1000379 - 1964 - Status of the deepwater cisco population of Lake Michigan","interactions":[],"lastModifiedDate":"2016-02-25T11:51:54","indexId":"1000379","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3624,"text":"Transactions of the American Fisheries Society","active":true,"publicationSubtype":{"id":10}},"title":"Status of the deepwater cisco population of Lake Michigan","docAbstract":"

The species and size composition and the abundance of the cisco (Leucichthys spp.) population of Lake Michigan have undergone drastic changes since the sea lamprey became established in the 1940's. The changes were measured by the catches of gill nets of identical specifications fished at the same seasons, depths, and locations in 1930-32, 1954-55, and 1960-61. The two largest ciscoes (johannae and nigripinnis), exploited heavily in a highly selective fishery from the midnineteenth century to the early 1900's, were only sparsely represented in the catch in the 1930's and were absent from catches of the comparison surveys in 1954-55 and 1960-61. The species of intermediate size (alpenae, artedi, kiyi, reighardi, and zenithicus) constituted about two-thirds of the cisco stocks of the deepwater zone in the 1930's but declined to 23.9 and 6.4 percent in the 1950's and 1960's, respectively. Major causes of change were the increased fishing pressure and sea lamprey predation that accompanied the disappearance of the lake trout. The small, slow-growing cisco (hoyi) - the primary food of lake trout - which was not fished intensively, and was too small to suffer greatly from sea lamprey predation, increased from 31.0 percent of the catch in the 1930's to 76.1 percent in the 1950's and 93.6 percent in the 1960's. Consequences of the extreme imbalance of the cisco population have been a reduction in mean size of all species, extension of the range of the very abundant hoyi (formerly most abundant in moderately shallow areas) to almost all depths and sections of the lake, and possibly introgressive hybridization among the various species. The primary change in the fishery has been a shift from gill nets to more extensive use of trawls which can take the now abundant smaller fish.

","language":"English","publisher":"Taylor & Francis","doi":"10.1577/1548-8659(1964)93[155:SOTDCP]2.0.CO;2","usgsCitation":"Smith, S.H., 1964, Status of the deepwater cisco population of Lake Michigan: Transactions of the American Fisheries Society, v. 93, no. 2, p. 155-163, https://doi.org/10.1577/1548-8659(1964)93[155:SOTDCP]2.0.CO;2.","productDescription":"9 p.","startPage":"155","endPage":"163","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":133096,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"93","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48d5e4b07f02db549082","contributors":{"authors":[{"text":"Smith, Stanford H.","contributorId":86711,"corporation":false,"usgs":true,"family":"Smith","given":"Stanford","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":308483,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2353,"text":"wsp1600 - 1964 - Geology and ground-water conditions of Clark County, Washington, with a description of a major alluvial aquifer along the Columbia River","interactions":[],"lastModifiedDate":"2023-03-23T21:07:44.77317","indexId":"wsp1600","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1600","title":"Geology and ground-water conditions of Clark County, Washington, with a description of a major alluvial aquifer along the Columbia River","docAbstract":"

This report presents the results of an investigation of the ground-water resources of the populated parts of Clark County. Yields adequate for irrigation can be obtained from wells inmost farmed areas in Clark County, Wash. The total available supply is sufficient for all foreseeable irrigation developments. In a few local areas aquifers are fine-grained, and yields of individual wells are low. An enormous ground-water supply is available from a major alluvial aquifer underlying the flood plain of the Columbia River in the vicinity of Vancouver, Camas, and Washougal, where the aquifer is recharged, in part, by infiltration from the river. Yields of individual wells are large, ranging to as much as 4,000 gpm (gallons per minute). Clark County lies along the western flank of the Cascade Range. in the structural lowland (Willamette-Puget trough) between those mountains and the Coast Ranges to the west. The area covered by the report includes the urban, the suburban, and most of the agricultural lands in the county. These lands lie on a Series of nearly fiat plains and benches which rise steplike from the level of the Columbia River (a few feet above sea level) to about 800 feet above sea level. Clark County is-drained by the Columbia River (the trunk stream of the Pacific Northwest) and its tributaries. The Columbia River forms the southern and western boundaries of the county. Although the climate of the county is considered to be humid, the precipitation ranging from about 37 to more than 110 inches annually in various parts of the county, the unequal seasonal distribution (about 1.5 inches total for ;July and August in the agricultural area) makes irrigation highly desirable for most .crops and essential for some specialized crops. Consolidated rocks of Eocene to Miocene age, chiefly volcanic lava flows and pyroclastics but including some sedimentary strata, crop out in the foothills of the Cascades in the eastern part of the county and underlie the younger, unconsolidated rocks in the lowlands to the west At most places small to moderate quantities of water can be obtained from fractures in the older consolidated rocks. However, in the populated parts of the county, these rocks generally are overlain by considerable thicknesses of more permeable materials, and few wells have been drilled in them. Springs and dug wells yield an ample domestic supply at a number of outlying farms in the foothills. The younger (Pliocene to Recent) unconsolidated materials were deposited chiefly by streams in the basin formed by downwarping of the older rocks. However, some lake deposits and glacial drift also are included. The oldest unit of this group, the lower member of the Troutdale formation of Pliocene age, consists chiefly of clay, silt, and fine sand but includes lenses of coarser sand and, rarely, gravel. The maximum known thickness of the lower member of the Troutdale formation is about 660 feet. This unit is not a good aquifer because most of the strata are fine grained. However, at a few places drilled wells have penetrated lenses of coarser grained materials in these deposits and have obtained small to moderate amounts of water from them. The upper member of the Troutdale formation consists almost entirely of lightly to moderately cemented gravel, of which the most striking feature is the presence of a considerable percentage of quartzite pebbles. The average thickness of the upper member of the Troutdale may originally have been 300 to 400 feet. The member crops out over considerable areas in the county and, where conditions of topography and exposure are optimum, has beer very deeply weathered. It is suggested that the upper member of the Troutdale formation may prove to be of early Pleistocene age. 

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1600","usgsCitation":"Mundorff, M.J., 1964, Geology and ground-water conditions of Clark County, Washington, with a description of a major alluvial aquifer along the Columbia River: U.S. Geological Survey Water Supply Paper 1600, Report: vi, 268 p.; 3 Plates: 35.00 x 50.19 inches or smaller, https://doi.org/10.3133/wsp1600.","productDescription":"Report: vi, 268 p.; 3 Plates: 35.00 x 50.19 inches or smaller","costCenters":[],"links":[{"id":28281,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1600/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28280,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1600/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28279,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1600/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":414663,"rank":6,"type":{"id":36,"text":"NGMDB Index 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Maurice John","contributorId":41404,"corporation":false,"usgs":true,"family":"Mundorff","given":"Maurice","email":"","middleInitial":"John","affiliations":[],"preferred":false,"id":145066,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221125,"text":"70221125 - 1964 - Origin of precambrian iron formations","interactions":[],"lastModifiedDate":"2021-06-02T17:51:31.990895","indexId":"70221125","displayToPublicDate":"1963-09-01T12:48:10","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Origin of precambrian iron formations","docAbstract":"

A statistical study of the chemical composition of the Precambrian iron formations of the Canadian Shield affords a new approach to the origin of these unusual formations. The average total iron content of 2,200 samples from the literature and from unpublished mining company analyses is 26.7 percent Fe. The average Fe content for 16 iron formations in the United States and Canada ranges from 24.5 to 34.1 percent. Low contents of A1203, Ti02, P2O5, and CaO characterize the Precambrian iron formations compared to the relatively large amounts of these constituents in the post-Precambrian iron-bearing sediments. The chemical data emphasize that whereas iron, manganese, and silica were transported and deposited together in the cherty iron formations of the Precambrian, these same elements were chemically differentiated in younger geological time in large but separate deposits of iron and silica. Isotopic age determinations indicate that cherty iron formations were deposited during a long interval of geologic time from approximately 1,700 to 3,000 million years ago. A model is proposed to explain the origin of the iron formations of the Lake Superior type based on the absence or marked deficiency of free oxygen in the atmosphere prior to the Late Precambrian. Lateritic weathering under these conditions permitted the transport of iron and manganese together with silica. The weathered mantle effectively retained aluminum, titanium, phosphorus, and colloidal clay. Graphitic material of biogenic origin is closely associated with the Precambrian iron formations. Although it is uncertain whether iron was precipitated directly through biologic processes, the removal of C02 and the liberation of oxygen to the sea water through photosynthesis of primitive plants undoubtedly influenced the energy relationships among the iron minerals. As a result of the variable conditions the iron formations commonly are characterized by nonequilibrium mineral assemblages. In Late Precambrian time a critical level of free oxygen in the atmosphere was attained permitting a marked acceleration in plant growth and in accretion of oxygen. This stage in the development of an oxygenated atmosphere was reached at least 1,200 million years ago and effectively curtailed the development of cherty iron formations of the Lake Superior type.

","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.59.6.1025","usgsCitation":"Lepp, H., and Goldich, S., 1964, Origin of precambrian iron formations: Economic Geology, v. 59, no. 6, p. 1025-1060, https://doi.org/10.2113/gsecongeo.59.6.1025.","productDescription":"36 p.","startPage":"1025","endPage":"1060","costCenters":[],"links":[{"id":386141,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"59","issue":"6","noUsgsAuthors":false,"publicationDate":"1964-09-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Lepp, H.","contributorId":259204,"corporation":false,"usgs":false,"family":"Lepp","given":"H.","email":"","affiliations":[],"preferred":false,"id":816811,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Goldich, S. S.","contributorId":65536,"corporation":false,"usgs":true,"family":"Goldich","given":"S. S.","affiliations":[],"preferred":false,"id":816812,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70161192,"text":"70161192 - 1963 - Co-oxidation of the sulfur-containing amino acids in an autoxidizing lipid system","interactions":[],"lastModifiedDate":"2016-01-05T10:57:40","indexId":"70161192","displayToPublicDate":"2015-09-08T05:15:00","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2293,"text":"Journal of Food Science","active":true,"publicationSubtype":{"id":10}},"title":"Co-oxidation of the sulfur-containing amino acids in an autoxidizing lipid system","docAbstract":"

Oxidation of the sulfur amino acids by autoxidizing lipids was studied in a model system consisting of an amino acid dispersed in cold-pressed, molecularly distilled menhaden oil (20–80% w/w). Under all conditions investigated, cysteine was oxidized completely to cystine. Preliminary results suggest that at 110°C the oxidation follows first-order kinetics for at least the first 8 hr. A specific reaction rate constant of 0.25 per hour was calculated. When fatty acids were added to the system, cystine was oxidized to its thiosulfinate ester. When the fatty acid-cystine ratio was 1:2, oxidation of cystine was a maximum. No oxidation of cystine occurred unless either a fatty acid, volatile organic acid, or ethanol was added. Under the conditions investigated, methionine was not oxidized to either its sulfoxide or its sulfone.

","language":"English","publisher":"Wiley","doi":"10.1111/j.1365-2621.1963.tb00239.x","usgsCitation":"Wedemeyer, G., and Dollar, A., 1963, Co-oxidation of the sulfur-containing amino acids in an autoxidizing lipid system: Journal of Food Science, v. 28, no. 5, p. 537-540, https://doi.org/10.1111/j.1365-2621.1963.tb00239.x.","productDescription":"4 p.","startPage":"537","endPage":"540","numberOfPages":"4","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":654,"text":"Western Fisheries Research Center","active":true,"usgs":true}],"links":[{"id":313399,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"28","issue":"5","noUsgsAuthors":false,"publicationDate":"2006-08-25","publicationStatus":"PW","scienceBaseUri":"568cf73ee4b0e7a44bc0f13f","contributors":{"authors":[{"text":"Wedemeyer, Gary","contributorId":94244,"corporation":false,"usgs":true,"family":"Wedemeyer","given":"Gary","affiliations":[],"preferred":false,"id":585143,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dollar, A.M.","contributorId":150882,"corporation":false,"usgs":false,"family":"Dollar","given":"A.M.","email":"","affiliations":[],"preferred":false,"id":585144,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70039573,"text":"70039573 - 1963 - Use of hydrologic models in the analysis of flood runoff","interactions":[],"lastModifiedDate":"2012-08-14T01:01:44","indexId":"70039573","displayToPublicDate":"2012-01-01T16:11:06","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":371,"text":"Monograph","active":false,"publicationSubtype":{"id":6}},"title":"Use of hydrologic models in the analysis of flood runoff","docAbstract":"The analog technique is applied to the analysis of flood runoff. A quasi-linear analog model has been developed for simulating the runoff-producing characteristics of a drainage system. Where storage is linear a unique relationship correlating the inflow and outflow peaks is derived. The technique for synthesizing flood-frequency distribution is also discussed. It is found that a linear-basin system would not modify the type of probability distribution of its inflow, whereas a nonlinear-basin system would.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/70039573","usgsCitation":"Shen, J., 1963, Use of hydrologic models in the analysis of flood runoff: Monograph, vii, 52 p.; ill., https://doi.org/10.3133/70039573.","productDescription":"vii, 52 p.; ill.","numberOfPages":"87","costCenters":[{"id":629,"text":"Water Resources Division","active":false,"usgs":true}],"links":[{"id":261089,"rank":800,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70039573/report.pdf"},{"id":261090,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70039573/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bbf28e4b08c986b3299b9","contributors":{"authors":[{"text":"Shen, John","contributorId":34109,"corporation":false,"usgs":true,"family":"Shen","given":"John","email":"","affiliations":[],"preferred":false,"id":466498,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70039538,"text":"70039538 - 1963 - A progress report on seismic model studies","interactions":[],"lastModifiedDate":"2013-01-15T11:22:54","indexId":"70039538","displayToPublicDate":"2012-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":355,"text":"Crustal Studies Technical Letter","active":false,"publicationSubtype":{"id":6}},"seriesNumber":"15","title":"A progress report on seismic model studies","docAbstract":"The value of seismic-model studies as an aid to understanding wave propagation in the Earth's crust was recognized by early investigators (Tatel and Tuve, 1955). Preliminary model results were very promising, but progress in model seismology has been restricted by two problems: (1) difficulties in the development of models with continuously variable velocity-depth functions, and (2) difficulties in the construction of models of adequate size to provide a meaningful wave-length to layer-thickness ratio. The problem of a continuously variable velocity-depth function has been partly solved by a technique using two-dimensional plate models constructed by laminating plastic to aluminum, so that the ratio of plastic to aluminum controls the velocity-depth function (Healy and Press, 1960). These techniques provide a continuously variable velocity-depth function, but it is not possible to construct such models large enough to study short-period wave propagation in the crust. This report describes improvements in our ability to machine large models. Two types of models are being used: one is a cylindrical aluminum tube machined on a lathe, and the other is a large plate machined on a precision planer. Both of these modeling techniques give promising results and are a significant improvement over earlier efforts.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Denver, CO","doi":"10.3133/70039538","collaboration":"In cooperation with the Defense Advanced Research Projects Agency","usgsCitation":"Healy, J.H., and Mangan, G.B., 1963, A progress report on seismic model studies: Crustal Studies Technical Letter 15, iv, 8 p., https://doi.org/10.3133/70039538.","productDescription":"iv, 8 p.","numberOfPages":"12","onlineOnly":"Y","costCenters":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"links":[{"id":259557,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/misc/tl/0015/tl0015.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":259554,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/misc/tl/0015/","linkFileType":{"id":5,"text":"html"}},{"id":259569,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e511e4b0c8380cd46ae4","contributors":{"authors":[{"text":"Healy, J. H.","contributorId":48968,"corporation":false,"usgs":true,"family":"Healy","given":"J.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":466442,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mangan, G. B.","contributorId":86035,"corporation":false,"usgs":true,"family":"Mangan","given":"G.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":466443,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5220320,"text":"5220320 - 1963 - A modification of the line intercept method of sampling understory vegetation","interactions":[],"lastModifiedDate":"2025-02-27T17:46:41.813658","indexId":"5220320","displayToPublicDate":"2010-06-16T12:17:32","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2441,"text":"Journal of Range Management","active":true,"publicationSubtype":{"id":10}},"title":"A modification of the line intercept method of sampling understory vegetation","docAbstract":"

No abstract available.

","language":"English","publisher":"Allen Press","doi":"10.2307/3895028","usgsCitation":"Ripley, T., Johnson, F., and Moore, W., 1963, A modification of the line intercept method of sampling understory vegetation: Journal of Range Management, v. 16, no. 1, p. 9-11, https://doi.org/10.2307/3895028.","productDescription":"3 p.","startPage":"9","endPage":"11","numberOfPages":"3","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":193956,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"16","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b23e4b07f02db6adea3","contributors":{"authors":[{"text":"Ripley, T.H.","contributorId":45792,"corporation":false,"usgs":true,"family":"Ripley","given":"T.H.","email":"","affiliations":[],"preferred":false,"id":331620,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, F.M.","contributorId":78423,"corporation":false,"usgs":true,"family":"Johnson","given":"F.M.","email":"","affiliations":[],"preferred":false,"id":331622,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Moore, W.H.","contributorId":70868,"corporation":false,"usgs":true,"family":"Moore","given":"W.H.","email":"","affiliations":[],"preferred":false,"id":331621,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2390,"text":"wsp1757A - 1963 - Ground-water exploration in Al Marj area, Cyrenaica, United Kingdom of Libya","interactions":[],"lastModifiedDate":"2012-02-02T00:05:33","indexId":"wsp1757A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1757","chapter":"A","title":"Ground-water exploration in Al Marj area, Cyrenaica, United Kingdom of Libya","docAbstract":"The present report, based largely on fieldwork during 1959-61, describes the results of reconnaissance hydrogeologic studies and exploratory drilling to evaluate the general water-bearing properties of the rocks and the availability of groundwater supplies for irrigation, stock, and village uses in Al Marj area. These studies and the drilling were conducted under the auspices of the U.S. Operations Mission of the International Cooperation Administration. \r\n\r\nAl Marj area, located in the Province of Cyrenaica on the southern coast of the Mediterranean Sea, contains a land area of about 6,770 square kilometers. Along the Mediterranean shore is a narrow coastal plain that rises evenly to the base of an escarpment that forms the seaward front of an undulating plateau known as. Al Jabal al Akhgiar. The climate is semiarid; seasonal rainfall occurs during the winter months. Owing to orographic effects, the rainfall is somewhat higher in the Jabal than in the coastal plain. The average annual rainfall ranges from about 250 millimeters in the coastal plain to 450 millimeters on the Jabal. All the streams (wadis) of the area are ephemeral and flow only in response to heavy rains of the winter season. From a drainage divide on the Jabal some streams flow north and northwest toward the sea and the others, south and southeast to the interior desert. Solution features, such as limestone sink holes, are common in the coastal plain and a large solution depression occurs near Al Marj. \r\n\r\nThe rocks of A1 Marj area consist predominantly of limestone and some sandstone and shale; they range from Cretaceous to Miocene age. On the coastal plain Miocene limestone is locally mantled by Quaternary alluvial, beach and lagoonal deposits. The Miocene and older beds have a regional southerly dip. These rocks are broken by northeast-trending normal faults in the coastal and inland escarpments. \r\n\r\nThe ground-water reservoir is contained chiefly in fractures, bedding planes, and solution openings in the limestone country rock. The upper limit of this reservoir is marked by a water table which generally lies within 40 meters of the land surface in the coastal plain but is 100 meters or more below the surface of most of the Jabal and the interior desert. The ground-water reservoir is replenished chiefly by infiltration from surface-water runoff in wadis and to less extent by direct infiltration of rainfall. Ground water moves north and northwest toward the Mediterranean Sea and south toward the interior desert from a ground-water divide near the crest of A1 Jabal al Akhgiar. Discharge of ground water takes place by submarine outflow, spring flow, evapotranspiration, and withdrawals from wells. \r\n\r\nWells, springs, and cisterns furnish almost all water supplies for municipal, village, stock and irrigation purposes. Bengasi, A1 Marj, and A1 Abyar are the only centers of population with municipal distribution systems. Drafts from individual dug wells used for irrigation in the coastal plain generally are no more than 10 to 15 cubic meters per day. In the Jabal and the interior desert drafts from individual stock and village wells are generally less than 10 cubic meters per day and from most wells only a few thousand liters per day. \r\n\r\nSome 21 test wells were put down during the present investigation to depths ranging from 30 to 309 meters. The yields obtained by test pump and bailer ranged from 45 to 0.6 cubic meters per hour. With few exceptions, well yields sufficient for stock and village requirements were obtained. Well yields sufficient for irrigation even on a moderate scale, however, are not everywhere available. In the Jabal and the interior desert the ground water is generally of good to fair chemical quality and suitable for most purposes. In the coastal plain, however, the ground water is in places moderately to highly mineralized, and consequently for irrigation use it must be applied to the land under optimum crop soil, and drainage conditions.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1757A","usgsCitation":"Newport, T., and Haddor, Y., 1963, Ground-water exploration in Al Marj area, Cyrenaica, United Kingdom of Libya: U.S. Geological Survey Water Supply Paper 1757, iii, 24 p. :ill., maps ;24 cm. + plates folded in pocket., https://doi.org/10.3133/wsp1757A.","productDescription":"iii, 24 p. :ill., maps ;24 cm. + plates folded in pocket.","costCenters":[],"links":[{"id":139184,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1757a/report-thumb.jpg"},{"id":28365,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28366,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757a/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28367,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1757a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66ce76","contributors":{"authors":[{"text":"Newport, T.G.","contributorId":80258,"corporation":false,"usgs":true,"family":"Newport","given":"T.G.","email":"","affiliations":[],"preferred":false,"id":145123,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Haddor, Yousef","contributorId":78722,"corporation":false,"usgs":true,"family":"Haddor","given":"Yousef","email":"","affiliations":[],"preferred":false,"id":145122,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":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":23477,"text":"ofr6363 - 1963 - Modified Parshall flume","interactions":[],"lastModifiedDate":"2013-08-01T15:19:18","indexId":"ofr6363","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":"63-63","title":"Modified Parshall flume","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey, Hydrologic Laboratory,","doi":"10.3133/ofr6363","issn":"0094-9140","usgsCitation":"Johnson, A., 1963, Modified Parshall flume: U.S. Geological Survey Open-File Report 63-63, 6 p. ill. ;27 cm., https://doi.org/10.3133/ofr6363.","productDescription":"6 p. ill. ;27 cm.","costCenters":[],"links":[{"id":156858,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1963/0063/report-thumb.jpg"},{"id":275867,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1963/0063/report.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4de4b07f02db627424","contributors":{"authors":[{"text":"Johnson, A.I.","contributorId":82676,"corporation":false,"usgs":true,"family":"Johnson","given":"A.I.","email":"","affiliations":[],"preferred":false,"id":190173,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":971,"text":"wsp1646 - 1963 - Ground-water geology of Grayson County, Texas","interactions":[],"lastModifiedDate":"2016-08-22T11:15:53","indexId":"wsp1646","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1646","title":"Ground-water geology of Grayson County, Texas","docAbstract":"

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

\n

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

\n

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

\n

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

\n

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

\n

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

\n

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

\n

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

\n

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

\n

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

\n

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

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1646","isbn":"pbk","usgsCitation":"Baker, E., 1963, Ground-water geology of Grayson County, Texas: U.S. Geological Survey Water Supply Paper 1646, Report: v, 61 p.; 6 Plates, https://doi.org/10.3133/wsp1646.","productDescription":"Report: v, 61 p.; 6 Plates","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":25516,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25517,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1646/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137044,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1646/report-thumb.jpg"},{"id":25511,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109998,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24841.htm","linkFileType":{"id":5,"text":"html"},"description":"24841"},{"id":25512,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25513,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25514,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25515,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1646/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668e7c","contributors":{"authors":[{"text":"Baker, E.T.","contributorId":11584,"corporation":false,"usgs":true,"family":"Baker","given":"E.T.","email":"","affiliations":[],"preferred":false,"id":142944,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1371,"text":"wsp1655 - 1963 - Ground water in the Pullman area, Whitman County, Washington","interactions":[{"subject":{"id":55768,"text":"ofr5746 - 1957 - Ground water in the Pullman area, Whitman county, Washington","indexId":"ofr5746","publicationYear":"1957","noYear":false,"title":"Ground water in the Pullman area, Whitman county, Washington"},"predicate":"SUPERSEDED_BY","object":{"id":1371,"text":"wsp1655 - 1963 - Ground water in the Pullman area, Whitman County, Washington","indexId":"wsp1655","publicationYear":"1963","noYear":false,"title":"Ground water in the Pullman area, Whitman County, Washington"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1655","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1655","title":"Ground water in the Pullman area, Whitman County, Washington","docAbstract":"This report presents the results of an investigation of the ground-water resources of the Pullman area, Whitman County, Wash. The investigation war made in cooperation with the State of Washington, Department of Conservation, Division of Water Resources, to determine whether the 1959 rate of ground-water withdrawal exceeded the perennial yield of the developed aquifers, and if so, (1) whether additional aquifers could be developed in the area, and (2) whether the yield of the developed aquifers could be increased by artificial recharge. The Pullman area includes the agricultural district surrounding the city of Pullman, in southeastern Whitman County, and the western two-thirds of the Moscow-Pullman basin, which extends into Latah County, Idaho. The mapped area comprises shout 250 square miles. \r\n\r\nThe area is in a region of smooth rolling hills formed by erosion of thick deposits of loess, which cover a dissected lava plain. The loess (Palouse formation of Pleistocene age) ranges in thickness from less than 1 foot to more than 150 feet. The underlying lava flows, part of the Columbia River basalt of Tertiary age, are nearly horizontal and form bluffs and low cliffs along the major streams. The total thickness of the basalt sequence in the area is not known, but it may be considerably greater than 1,000 feet beneath the city of Pullman. The basalt sequence is underlain by a basement mass of granite, granite gneiss, and quartzite, of pre-Tertiary age. \r\n\r\nThe most productive aquifers in the area are in the Columbia River basalt. They consist of the permeable zones, commonly occurring at the tops of individual lava flows, which may contain ground water under either artesian or water-table conditions. Two such permeable zones have produced more than 95 percent of the ground water used in the Pullman area, or as much as 870 million gallons per year (1957). These two zones are hydraulically connected and lie at depths ranging from about 50 to 170 feet below the land surface at Pullman. The area receives about 21 inches of precipitation annually, about two-thirds of it from October through March. 0nly a fraction of the precipitation reaches the aquifers; the remainder is returned to the atmosphere by evapotranspiration or leaves the area as surface runoff. The basalt is recharged mainly by infiltration from streams and downward percolation from the overlying loess. \r\n\r\nThe ground water moves generally westward. However, most water in the artesian aquifers tapped by wells in the vicinity of Pullman may move toward the city of Pullman, which is the center of major pumping. The rate of movement ranges from extremely slow in the loess and the massive basalt to very rapid in the permeable zones of basalt. The principal modes of discharge from the artesian aquifers are seepage to streams and pumpage from wells. The amount of natural discharge is unknown, but the pumpage ranged from about 340 to 870 million gallons per year, and during 1949-59 it averaged about 800 million gallons (2,500 ac-ft) per year. For about the last 25 years at least, the piezometric surface of the artesian zones has declined each year, indicating that the annual ground-water discharge from the artesian aquifers (including pumpage and natural discharge) has exceeded the recharge in the Pullman area. An analysis of the relation of pumpage to the decline in artesian level indicates that during 1952-59 an average of about 65 million gallons per year was removed from storage. Although the decline in artesian pressures has resulted in an increase in the recharge to the aquifers, the present rate of pumping may be equal to or even exceed the perennial yield of the artesian aquifer in the report area under natural conditions. \r\n\r\nGeologic and hydrologic conditions seem favorable for the existence of potentially good aquifers below those which are now extensively developed. The deep aquifers seem to have only a slight hydraulic connection with the overlying artesian basalt ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1655","usgsCitation":"Foxworthy, B., and Washburn, R., 1963, Ground water in the Pullman area, Whitman County, Washington: U.S. Geological Survey Water Supply Paper 1655, iv, 71 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1655.","productDescription":"iv, 71 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":110001,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24847.htm","linkFileType":{"id":5,"text":"html"},"description":"24847"},{"id":137288,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1655/report-thumb.jpg"},{"id":26462,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1655/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26463,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1655/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26464,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1655/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26465,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1655/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66d89c","contributors":{"authors":[{"text":"Foxworthy, B. L.","contributorId":45686,"corporation":false,"usgs":true,"family":"Foxworthy","given":"B. L.","affiliations":[],"preferred":false,"id":143651,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Washburn, R.L.","contributorId":89114,"corporation":false,"usgs":true,"family":"Washburn","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":143652,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":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 Southwest"},{"id":60779,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0372d/report.pdf","size":"8.12 MB","linkFileType":{"id":1,"text":"pdf"}},{"id":119889,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0372d/report-thumb.jpg"}],"country":"Mexico, United States","state":"Colorado, New Mexico, Texas","otherGeospatial":"Rio Grande basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -97.40478515625,\n 26.902476886279832\n ],\n [\n -97.9541015625,\n 26.80446076654616\n ],\n [\n -98.5693359375,\n 27.00040800352175\n ],\n [\n -99.16259765625,\n 27.800209937418252\n ],\n [\n -99.64599609375,\n 29.075375179558346\n ],\n [\n -99.90966796875,\n 29.439597566602902\n ],\n [\n -100.21728515624999,\n 29.630771207229\n ],\n [\n -101.14013671875,\n 30.12612436422458\n ],\n [\n 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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":1111,"text":"wsp1577 - 1963 - Ground-water geology and pump irrigation in Frenchman Creek Basin above Palisade, Nebraska","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1577","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1577","title":"Ground-water geology and pump irrigation in Frenchman Creek Basin above Palisade, Nebraska","docAbstract":"This report describes the geography, geology, and ground-water resources of that part of the Frenchman Creek basin upstream from Palisade, Nebr., an area of about 4,900 square miles. The basin includes all of Phillips County, Colo., and Chase County, Nebr., and parts of Logan, Sedgwick, Washington, and Yuma Counties, Colo., and Dundy, Hayes, Hitchcock, and Perkins Counties, Nebr. The land surface ranges from nearly flat to rolling; choppy hills and interdune saddles are common in the areas of dune sand, and steep bluffs and gullies cut the edges of the relatively flat loess plateaus. Most of the basin is drained by tributaries of Frenchman Creek, but parts of the sandhills are undrained. Farming and livestock raising are the principal industries. Irrigation with ground water has expanded rapidly since 1934. \r\n\r\nThe rocks exposed in the basin are largely unconsolidated and range in age from Pliocene to Recent. They comprise the Ogallala formation (Pliocene), the Sanborn formation (Pleistocene and Recent?), dune sand (Pleistocene and Recent), and alluvium (Recent). The rocks underlying the Ogallala are the Pierre shale (Late Cretaceous) and the White River group (Oligocene). The Pierre shale is relatively impermeable and yields little or no water to wells. The White River group also is relatively impermeable and yields little or no water to wells; however, small to moderate quantities of water possibly may be obtained from wells that penetrate fractured or 'porous' zones in the upper part of the White River group or permeable channel deposits within the group. The Ogallala formation is the main aquifer in the basin and yields moderate to large quantities of water to wells. The Sanborn formation and the dune sand generally lie above the water table, but in areas of high water table the dune sand yields small quantities of water to wells for domestic and stock supplies. The alluvium, which includes the low terrace deposits bordering the major streams, yields small to large quantities of water to wells. \r\n\r\nThe ground-water reservoir is recharged only from precipitation on the basin. Of the average annual precipitation of 19.5 inches, about 0.9 inch infiltrates to the water table, thereby contributing about 220,000 acre-feet of water annually to the ground-water reservoir. About 81 million acre-feet of water that could drain under gravity, and thus theoretically is available to wells, is held in groundwater storage in the basin. Water is discharged from the ground-water reservoir by wells, evaporation and transpiration, springs, seepage into streams, and movement into adjacent areas to the east and southeast. Most of the domestic, stock, and irrigation water supplies and all the public supplies are pumped from wells.\r\n\r\nDuring 1953, 96 wells were used to irrigate 10,000 acres of land with 19,000 acre-feet of water. About 34,000 acre-feet of water is evaporated and transpired annually in the valleys of the main streams and in areas of shallow water table in the sandhills. \r\n\r\nFrom the projection of base-flow measurements made during 1952, it was estimated that the average annual flow of Frenchman Creek into the reservoir above Enders Dam is about 57,000 acre-feet. By similar determinations, the average annual flow of Frenchman Creek at the gaging station at Palisade, Nebr., about 22 miles downstream from Enders Dam, is about 76,000 acre-feet, and the flow of Stinking Water Creek at the gaging station near Palisade is about 22,000 acre-feet. The combined flow of Frenchman and Stinking Water Creeks at their confluence near Palisade thus is about 98,000 acre-feet per year. About 90,000 acre-feet of ground water is estimated to move eastward each year across the Colorado-Nebraska State line within the basin. \r\n\r\nAdditional irrigation wells that will tap the Ogallala formation and the alluvium in the major valleys undoubtedly will be drilled. On the basis of current estimates of future irrigation.withdrawals, it is concluded that by the ","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1577","usgsCitation":"Cardwell, W.D., and Jenkins, E., 1963, Ground-water geology and pump irrigation in Frenchman Creek Basin above Palisade, Nebraska: U.S. Geological Survey Water Supply Paper 1577, vii, 472 p. :illus., diagrs., maps ;24 cm., https://doi.org/10.3133/wsp1577.","productDescription":"vii, 472 p. :illus., diagrs., maps ;24 cm.","costCenters":[],"links":[{"id":109991,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24763.htm","linkFileType":{"id":5,"text":"html"},"description":"24763"},{"id":138010,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1577/report-thumb.jpg"},{"id":25858,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25859,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25860,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25861,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25862,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25863,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25864,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25865,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25866,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25867,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1577/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25868,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1577/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668e74","contributors":{"authors":[{"text":"Cardwell, W. D. E.","contributorId":69120,"corporation":false,"usgs":true,"family":"Cardwell","given":"W.","email":"","middleInitial":"D. E.","affiliations":[],"preferred":false,"id":143195,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jenkins, Edward D.","contributorId":17972,"corporation":false,"usgs":true,"family":"Jenkins","given":"Edward D.","affiliations":[],"preferred":false,"id":143194,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":959,"text":"wsp1588 - 1963 - Ground-water geology of Bexar County, Texas","interactions":[],"lastModifiedDate":"2016-08-22T10:56:34","indexId":"wsp1588","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1588","title":"Ground-water geology of Bexar County, Texas","docAbstract":"

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

\n

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

\n

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

\n

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

\n

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

\n

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

\n

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

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1588","usgsCitation":"Arnow, T., 1963, Ground-water geology of Bexar County, Texas: U.S. Geological Survey Water Supply Paper 1588, Report: v, 36 p.; 12 Plates, https://doi.org/10.3133/wsp1588.","productDescription":"Report: v, 36 p.; 12 Plates","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":25489,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25490,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25491,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25492,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25493,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25494,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1588/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109993,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24774.htm","linkFileType":{"id":5,"text":"html"},"description":"24774"},{"id":137509,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1588/report-thumb.jpg"},{"id":25482,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25483,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25484,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25485,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25486,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25487,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25488,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1588/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668dc9","contributors":{"authors":[{"text":"Arnow, Ted","contributorId":84733,"corporation":false,"usgs":true,"family":"Arnow","given":"Ted","affiliations":[],"preferred":false,"id":142918,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1916,"text":"wsp1539T - 1963 - Geology and ground-water resources of the Lake Dakota Plain area, South Dakota","interactions":[],"lastModifiedDate":"2016-04-05T09:58:33","indexId":"wsp1539T","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1539","chapter":"T","title":"Geology and ground-water resources of the Lake Dakota Plain area, South Dakota","docAbstract":"

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

\n

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

\n

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

\n

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

","language":"English","publisher":"U.S. Government Print Office","publisherLocation":"Washington, DC","doi":"10.3133/wsp1539T","usgsCitation":"Hopkins, W.B., and Petri, L., 1963, Geology and ground-water resources of the Lake Dakota Plain area, South Dakota: U.S. Geological Survey Water Supply Paper 1539, Report: v, 68 p.; 3 Plates: 26.00 x 40.33 inches or smaller, https://doi.org/10.3133/wsp1539T.","productDescription":"Report: v, 68 p.; 3 Plates: 26.00 x 40.33 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":137686,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1539t/report-thumb.jpg"},{"id":27236,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539t/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27237,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539t/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27238,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1539t/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27239,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1539t/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109986,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24741.htm","linkFileType":{"id":5,"text":"html"},"description":"24741"}],"country":"United States","state":"South Dakota","otherGeospatial":"Lake Dakota Plain","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -98.525390625,\n 44.68427737181225\n ],\n [\n -98.525390625,\n 45.82879925192134\n ],\n [\n -97.6025390625,\n 45.82879925192134\n ],\n [\n -97.6025390625,\n 44.68427737181225\n ],\n [\n -98.525390625,\n 44.68427737181225\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6854ff","contributors":{"authors":[{"text":"Hopkins, William B.","contributorId":54574,"corporation":false,"usgs":true,"family":"Hopkins","given":"William","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":144361,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Petri, Lester R.","contributorId":19534,"corporation":false,"usgs":true,"family":"Petri","given":"Lester R.","affiliations":[],"preferred":false,"id":144360,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2382,"text":"wsp1614 - 1963 - Water resources of Red River Parish, Louisiana","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1614","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":"1614","title":"Water resources of Red River Parish, Louisiana","docAbstract":"Red River Parish is on the eastern flank of the Sabine uplift in northwestern Louisiana. The 'area is underlain by lignitic clay and sand of Paleocene and Eocene age which dip to the east at the rate of about 30 feet per mile. The Red River is entrenched in these rocks in the western part of the parish. Alternating valley filling and erosion during the Quaternary period have resulted in the present lowland with flanking terraces. \r\n\r\nIn the flood-plain area moderate to large quantities of very hard, iron-bearing water, suitable for irrigation, are available to wells in the alluvial sand and gravel of Quaternary age. The aquifer ranges in thickness from 20 to slightly more than 100 feet. It is recharged by downward seepage of rainfall through overlying clay and silt, by inflow from older sands adjacent to and beneath the entrenched valley, and by infiltration from the streams where the water table is below stream level during flood stages or as a result of pumping. Water levels are highest in the middle of the valley. Ground water moves mainly toward the Red River on the east and Bayou Pierre on the west, but small amounts move down the valley. Computations based on water-level and aquifer-test data indicate that the Quaternary alluvium contains more than 330 billion gallons of ground water in storage and that the maximum discharge of ground water to the streams is slightly more than 30 mgd (million gallons per day). At times of high river stage, surface water flows into the aquifer at a rate that depends in part upon the height and duration of the river stage. \r\n\r\nModerate supplies of soft, iron-bearing water may be obtained from dissected Pleistocene terrace deposits that flank the flood plains of the Red River and Black Lake Bayou. However, the quantity of water that can be pumped from these deposits varies widely from place to place because of differences in the areal extent and saturated thickness of the segments of the deposits; this extent and thickness are governed in turn by the amount of erosion the deposits have undergone. Beds of fine-grained lignitic sands of Tertiary age contain water of generally good quality to depths of 150 to 450 feet. The thinness and low permeability of the sands restrict their development to low-yield wells. Water from these sands in the western part of the parish, where they lie beneath the alluvial valley, is more mineralized than that from the younger Tertiary sands exposed in the east-central area. \r\n\r\nStreamflow records have been collected on the principal streams in Red River Parish since 1939. Additional spot low-flow data were obtained on several small streams originating within the parish for a study made in connection with the preparation of this report. Quality-of-water data for streams in the parish were collected on an occasional spot-sampling basis prior to and during this investigation. The largest source of surface water in the parish is the Red River, which drains approximately 63,400 square miles upstream from the parish. The Red River has an average flow of about 13,100 cfs (cubic feet per second), or about 8,500 mgd. Many of the streams that drain the upland area are not dependable sources of supply because their flows are not well sustained during dry seasons.\r\n\r\nThe average annual precipitation over the parish is about 52 inches, of which about 17 inches becomes runoff; this runoff is equivalent to a continuous flow of about 1.25 cfs per square mile. Seasonal and annual runoff varies, but no significant trends have been noticed.\r\n\r\nThe principal surface-water problems in the parish pertain to flood control, drainage, irrigation, and navigation. Flood problems have been alleviated considerably by the operation of Denison Dam (Lake Texoma), the completion of levees on the Red River, channel improvements on Bayou Pierre, and the completion of Wallace Lake reservoir on Cypress Bayou. There are wet lands along the Red River that would be very productive if properly drained ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1614","usgsCitation":"Newcome, R., and Page, L.V., 1963, Water resources of Red River Parish, Louisiana: U.S. Geological Survey Water Supply Paper 1614, v, 133 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1614.","productDescription":"v, 133 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":109996,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24808.htm","linkFileType":{"id":5,"text":"html"},"description":"24808"},{"id":137824,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1614/report-thumb.jpg"},{"id":28344,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28345,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28346,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28347,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28348,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28349,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28350,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28351,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28352,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28353,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28354,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28355,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28356,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28357,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1614/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a16e4b07f02db603d22","contributors":{"authors":[{"text":"Newcome, Roy","contributorId":14796,"corporation":false,"usgs":true,"family":"Newcome","given":"Roy","affiliations":[],"preferred":false,"id":145113,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Page, Leland Vernon","contributorId":95450,"corporation":false,"usgs":true,"family":"Page","given":"Leland","email":"","middleInitial":"Vernon","affiliations":[],"preferred":false,"id":145114,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":64960,"text":"i331 - 1963 - Preliminary glacial map of North Dakota","interactions":[],"lastModifiedDate":"2022-04-12T18:13:19.871184","indexId":"i331","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":320,"text":"IMAP","code":"I","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"331","title":"Preliminary glacial map of North Dakota","docAbstract":"

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

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/i331","usgsCitation":"Colton, R.B., Lemke, R.W., and Lindvall, R.M., 1963, Preliminary glacial map of North Dakota: U.S. Geological Survey IMAP 331, 1 Plate: 57.64 x 36.26 inches, https://doi.org/10.3133/i331.","productDescription":"1 Plate: 57.64 x 36.26 inches","costCenters":[],"links":[{"id":189317,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/imap/0331/report-thumb.jpg"},{"id":360513,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/imap/0331/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":398560,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_1676.htm"}],"scale":"500000","country":"United States","state":"North 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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":2857,"text":"wsp1619E - 1963 - Ground-water resources of the Alma area, Michigan","interactions":[{"subject":{"id":51114,"text":"ofr5244 - 1952 - Ground-water conditions in the Alma area, Michigan","indexId":"ofr5244","publicationYear":"1952","noYear":false,"title":"Ground-water conditions in the Alma area, Michigan"},"predicate":"SUPERSEDED_BY","object":{"id":2857,"text":"wsp1619E - 1963 - Ground-water resources of the Alma area, Michigan","indexId":"wsp1619E","publicationYear":"1963","noYear":false,"chapter":"E","title":"Ground-water resources of the Alma area, Michigan"},"id":1}],"lastModifiedDate":"2017-02-06T13:03:59","indexId":"wsp1619E","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":"E","title":"Ground-water resources of the Alma area, Michigan","docAbstract":"

The Alma area consists of 30 square miles in the northwestern part of Gratiot County, Mich. It is an area of slight relief gently rolling hills and level plains and is an important agricultural center in the State.

The Saginaw formation, which forms the bedrock surface in part of the area, is of relatively low permeability and yields water containing objectionable amounts of chloride. Formations below the Saginaw are tapped for brine in and near the Alma area.

The consolidated rocks of the Alma area are mantled by Pleistocene glacial deposits, which are as much as 550 feet thick where preglacial valleys were eroded into the bedrock. The glacial deposits consist of till, glacial-lake deposits, and outwash. Till deposits are at the surface along the south-trending moraines that cross the area, and they underlie other types of glacial deposits at depth throughout the area. The till deposits are of low permeability and are not a source of water to wells, though locally they include small lenses of permeable sand and gravel.

In the western part of the area, including much of the city of Alma, the glacial-lake deposits consist primarily of sand and are a source of small supplies of water. In the northeastern part of the area the lake deposits are predominantly clayey and of low permeability.

Sand and gravel outwash yields moderate and large supplies of water within the area. Outwash is present at the surface along the West Branch of the Pine River. A more extensive deposit of outwash buried by the lake deposits is the source of most of the ground water pumped at Alma. The presence of an additional deposit of buried outwash west and southwest of the city is inferred from the glacial history of the area. Additional water supplies that may be developed from these deposits are probably adequate for anticipated population and industrial growth.

Water levels have declined generally in the vicinity of the city of Alma since 1920 in response to pumping for municipal and industrial supplies. The declines are not excessive, and during the late 1950's water levels in parts of Alma have risen slightly, because of dispersion of the pumping stations.

The ground water in the Alma area generally is very hard and high in iron. Locally, the buried outwash that underlies the city of Alma is contaminated by phenolic substances. This limits the amount of ground water available for municipal supply within the city, although reclamation of the contaminated part of the aquifer is considered feasible.

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1619E","collaboration":"Prepared in cooperation with the Michigan Geological Survey and the city of Alma","usgsCitation":"Vanlier, K.E., 1963, Ground-water resources of the Alma area, Michigan: U.S. Geological Survey Water Supply Paper 1619, Document: v, 66 p.; 2 Plates: 19 x 13 inches and 15.5 x 13.5 inches, https://doi.org/10.3133/wsp1619E.","productDescription":"Document: v, 66 p.; 2 Plates: 19 x 13 inches and 15.5 x 13.5 inches","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":29450,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619e/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139080,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1619e/report-thumb.jpg"},{"id":29451,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1619e/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29449,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Michigan","city":"Alma","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -84.67729568481445,\n 43.36450174266976\n ],\n [\n -84.67729568481445,\n 43.39313609017517\n ],\n [\n -84.6269130706787,\n 43.39313609017517\n ],\n [\n -84.6269130706787,\n 43.36450174266976\n ],\n [\n -84.67729568481445,\n 43.36450174266976\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d5ad","contributors":{"authors":[{"text":"Vanlier, Kenneth E.","contributorId":47351,"corporation":false,"usgs":true,"family":"Vanlier","given":"Kenneth","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":145914,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}