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The Capitol Reef area includes about 900 square miles in western Wayne and north-central Garfield Counties, Utah. It is along the border between the High Plateaus of Utah and the Canyon Lands sections of the Colorado' Plateaus province. Capitol Reef National Monument is in the eastern part of the mapped area.

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp363","usgsCitation":"Smith, J.F., Huff, L.C., Hinrichs, E.N., and Luedke, R.G., 1963, Geology of the Capitol Reef area, Wayne and Garfield Counties, Utah: U.S. Geological Survey Professional Paper 363, Report: iv, 102 p.; 2 Plates: 38.88 x 44.60 inches and 18.44 x 18.72 inches, https://doi.org/10.3133/pp363.","productDescription":"Report: iv, 102 p.; 2 Plates: 38.88 x 44.60 inches and 18.44 x 18.72 inches","numberOfPages":"107","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":495847,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4361.htm","linkFileType":{"id":5,"text":"html"}},{"id":140281,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0363/report-thumb.jpg"},{"id":112832,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0363/plate-2.pdf","text":"Plate 2","size":"1.16 MB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Structure contour map and wall sections of the Oyler Mine, Capitol Reef area"},{"id":112830,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0363/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":112831,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0363/plate-1.pdf","text":"Plate 1","size":"14.6 MB","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Geologic map and sections of the Capitol Reef area"}],"country":"United States","state":"Utah","county":"Garfield County, Wayne County","otherGeospatial":"Capitol Reef area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.625,\n 38.5\n ],\n [\n -111.25,\n 38.5\n ],\n [\n -111.25,\n 38.37317\n ],\n [\n -111.1296,\n 38.37317\n ],\n [\n -111.1296,\n 38.25\n ],\n [\n -111,\n 38.25\n ],\n [\n -111,\n 38\n ],\n [\n -111.5,\n 38\n ],\n [\n -111.5,\n 38.1167\n ],\n [\n -111.625,\n 38.1167\n ],\n [\n -111.625,\n 38.5\n ]\n ]\n ]\n }\n }\n ]\n}","publicComments":"Prepared on behalf of the U.S. Atomic Energy Commission.","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad4e4b07f02db683207","contributors":{"authors":[{"text":"Smith, J. Fred Jr.","contributorId":106482,"corporation":false,"usgs":true,"family":"Smith","given":"J.","suffix":"Jr.","email":"","middleInitial":"Fred","affiliations":[],"preferred":false,"id":152702,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Huff, Lyman C.","contributorId":47440,"corporation":false,"usgs":true,"family":"Huff","given":"Lyman","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":152699,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hinrichs, E. Neal","contributorId":46488,"corporation":false,"usgs":true,"family":"Hinrichs","given":"E.","email":"","middleInitial":"Neal","affiliations":[],"preferred":false,"id":152701,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Luedke, Robert G.","contributorId":18339,"corporation":false,"usgs":true,"family":"Luedke","given":"Robert","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":152700,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":6417,"text":"pp359 - 1963 - Economic geology of the Central City district, Gilpin County, Colorado","interactions":[{"subject":{"id":16011,"text":"ofr54285 - 1954 - Preliminary geologic and vein maps of part of the Central City district, Gilpin and Clear Creek Counties, Colorado","indexId":"ofr54285","publicationYear":"1954","noYear":false,"title":"Preliminary geologic and vein maps of part of the Central City district, Gilpin and Clear Creek Counties, Colorado"},"predicate":"SUPERSEDED_BY","object":{"id":6417,"text":"pp359 - 1963 - Economic geology of the Central City district, Gilpin County, Colorado","indexId":"pp359","publicationYear":"1963","noYear":false,"title":"Economic geology of the Central City district, Gilpin County, Colorado"},"id":1}],"lastModifiedDate":"2016-06-28T11:05:52","indexId":"pp359","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":"359","title":"Economic geology of the Central City district, Gilpin County, Colorado","docAbstract":"

The Central City district, in Gilpin County, Colo., is on the east flank of the Front Range, about 30 miles west of Denver. The district is the most important mining camp in the Front Range mineral belt, and has yielded more than $100 million worth of gold, silver, uranium, and base-metal ores since 1859. Gold accounts for about 85 percent of the dollar value of the ore. In recent years mining activity has been slack but from 1950 to 1955 the search for uranium ores stimulated prospecting and development.

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp359","usgsCitation":"Sims, P., Drake, A.A., and Tooker, E.W., 1963, Economic geology of the Central City district, Gilpin County, Colorado: U.S. Geological Survey Professional Paper 359, Report: 231 p.; 12 Plates: 57.77 x 39.75 inches and smaller, https://doi.org/10.3133/pp359.","productDescription":"Report: 231 p.; 12 Plates: 57.77 x 39.75 inches and smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":308639,"rank":302,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"}},{"id":308640,"rank":303,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"}},{"id":308641,"rank":304,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-4.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"}},{"id":112829,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0359/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139779,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0359/report-thumb.jpg"},{"id":308642,"rank":305,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-5.pdf","text":"Plate 5","linkFileType":{"id":1,"text":"pdf"}},{"id":308643,"rank":306,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-6.pdf","text":"Plate 6","linkFileType":{"id":1,"text":"pdf"}},{"id":308638,"rank":301,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"}},{"id":308644,"rank":307,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-7.pdf","text":"Plate 7","linkFileType":{"id":1,"text":"pdf"}},{"id":308645,"rank":308,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-8.pdf","text":"Plate 8","linkFileType":{"id":1,"text":"pdf"}},{"id":308646,"rank":309,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-9.pdf","text":"Plate 9","linkFileType":{"id":1,"text":"pdf"}},{"id":308647,"rank":310,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-10.pdf","text":"Plate 10","linkFileType":{"id":1,"text":"pdf"}},{"id":308649,"rank":312,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-12.pdf","text":"Plate 12","linkFileType":{"id":1,"text":"pdf"}},{"id":308648,"rank":311,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0359/plate-11.pdf","text":"Plate 11","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Colorado","county":"Gilpin County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-105.6743,39.93],[-105.6089,39.9302],[-105.4968,39.9298],[-105.4728,39.9302],[-105.4638,39.9292],[-105.4584,39.9297],[-105.4398,39.9364],[-105.4362,39.9364],[-105.4296,39.9327],[-105.426,39.9318],[-105.4212,39.9309],[-105.3966,39.9326],[-105.3968,39.9117],[-105.3958,39.8827],[-105.3939,39.8251],[-105.3945,39.7499],[-105.4035,39.7499],[-105.4101,39.7486],[-105.4143,39.7459],[-105.4185,39.745],[-105.4203,39.7454],[-105.4215,39.7482],[-105.4239,39.7518],[-105.4262,39.7527],[-105.4274,39.7532],[-105.4424,39.7528],[-105.4454,39.7528],[-105.4609,39.7551],[-105.4759,39.7566],[-105.4854,39.7566],[-105.4932,39.7584],[-105.4992,39.7603],[-105.5081,39.7631],[-105.5207,39.7654],[-105.532,39.7681],[-105.5392,39.7718],[-105.5434,39.7759],[-105.5445,39.78],[-105.5451,39.7818],[-105.5457,39.785],[-105.554,39.7909],[-105.5743,39.8018],[-105.5755,39.8036],[-105.5755,39.8109],[-105.576,39.8186],[-105.5778,39.8209],[-105.579,39.8213],[-105.5814,39.8213],[-105.5892,39.8177],[-105.5922,39.8159],[-105.597,39.8164],[-105.6,39.8182],[-105.603,39.8196],[-105.6119,39.8223],[-105.6191,39.8255],[-105.6239,39.8301],[-105.6274,39.8346],[-105.6298,39.8396],[-105.6334,39.8419],[-105.6471,39.846],[-105.6531,39.8474],[-105.6597,39.8474],[-105.6651,39.8465],[-105.6723,39.8461],[-105.6795,39.8466],[-105.6849,39.8484],[-105.6884,39.8507],[-105.6908,39.8548],[-105.6926,39.8634],[-105.6955,39.8734],[-105.6961,39.8783],[-105.6955,39.8861],[-105.6955,39.8892],[-105.6925,39.8933],[-105.6895,39.8978],[-105.6864,39.9064],[-105.684,39.91],[-105.6804,39.9141],[-105.6798,39.9182],[-105.6779,39.9241],[-105.6743,39.93]]]},\"properties\":{\"name\":\"Gilpin\",\"state\":\"CO\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db625ad8","contributors":{"authors":[{"text":"Sims, P.K.","contributorId":30191,"corporation":false,"usgs":true,"family":"Sims","given":"P.K.","email":"","affiliations":[],"preferred":false,"id":152684,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Drake, Avery A. Jr.","contributorId":81090,"corporation":false,"usgs":true,"family":"Drake","given":"Avery","suffix":"Jr.","middleInitial":"A.","affiliations":[],"preferred":false,"id":152685,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Tooker, E. W.","contributorId":102071,"corporation":false,"usgs":true,"family":"Tooker","given":"E.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":152686,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2206,"text":"wsp1475M - 1963 - Ground-water resources of the Bryce Canyon National Park area, Utah, with a section on the drilling of a test well","interactions":[{"subject":{"id":23797,"text":"ofr5866 - 1958 - Ground-water resources of the Bryce Canyon National Park area, Utah","indexId":"ofr5866","publicationYear":"1958","noYear":false,"title":"Ground-water resources of the Bryce Canyon National Park area, Utah"},"predicate":"SUPERSEDED_BY","object":{"id":2206,"text":"wsp1475M - 1963 - Ground-water resources of the Bryce Canyon National Park area, Utah, with a section on the drilling of a test well","indexId":"wsp1475M","publicationYear":"1963","noYear":false,"chapter":"M","title":"Ground-water resources of the Bryce Canyon National Park area, Utah, with a section on the drilling of a test well"},"id":1}],"lastModifiedDate":"2024-06-17T18:55:36.649675","indexId":"wsp1475M","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":"1475","chapter":"M","title":"Ground-water resources of the Bryce Canyon National Park area, Utah, with a section on the drilling of a test well","docAbstract":"

The water need at Bryce Canyon National Park in 1957 was about 1.3 million cubic feet for a tourist season that lasted from the middle of May to the middle of October. To evaluate the adequacy of water-supply sources, a hypothetical future need of 5 million cubic feet of water per season is used. This amount of water might be obtained from the East Fork of the Sevier River, from wells in the alluvium of the East Fork, from Yellow Creek Spring and nearby springs, which are below the canyon rim, or from a well drilled about 2,000 feet to the top of the Tropic shale. Although the present source of water, consisting of wells in the alluvium of East Creek valley, may be an important supplemental source in the future, it will not yield sufficient water in dry years to meet the total demand for water at the park.

The yield of Yellow Creek Spring and nearby springs is estimated at a total of 7.8 million cubic feet of water per season. The springs provide water of satisfactory chemical quality, and are a reliable source even in times of drought. A serious disadvantage of using this source of water is the difficulty of constructing a pipeline over extremely rugged terrain from the source to the lodge and headquarters area.

A well drilled to the top of the Tropic shale of Cretaceous age in the lodge and headquarters area might penetrate two or more aquifers, one at the base of the Wasatch formation of Eocene age and one or more in the Wahweap and Straight Cliffs sandstones of Cretaceous age. The yield of this well would depend to a large degree on the number of fractures encountered. To assure the most favorable conditions for intercepting fracture zones in the bedrock, a test-well site is proposed near the crest of a gentle anticline where tension fractures in the rocks should be common.

Shallow wells in the alluvium of East Creek valley cannot be depended upon to yield sufficient water in times of drought, but they are nevertheless an important source. The water-storage capacity of the alluvium of East Creek valley in the vicinity of the wells of the Utah Parks Co. is estimated at 1.4 million cubic feet. By lowering the water table in the valley uniformly without creating excessively large cones of depression, the alluvium could supply the 1.3 million cubic feet of water per season estimated as the water need in 1957. However, in times of drought this alluvium cannot supply the hypothetical future needs of 5 million cubic feet of water per season.

","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Hydrology of the Public Domain (Water Supply Paper 1475)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1475M","collaboration":"Prepared in cooperation with the National Park Service, Department of the Interior","usgsCitation":"Marine, I.W., 1963, Ground-water resources of the Bryce Canyon National Park area, Utah, with a section on the drilling of a test well: U.S. Geological Survey Water Supply Paper 1475, Report: iv, 46 p.; 3 Plates: 16.20 x 24.41 inches or smaller, https://doi.org/10.3133/wsp1475M.","productDescription":"Report: iv, 46 p.; 3 Plates: 16.20 x 24.41 inches or smaller","startPage":"441","endPage":"486","numberOfPages":"50","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true},{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":430318,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24416.htm","linkFileType":{"id":5,"text":"html"}},{"id":27877,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1475m/plate-2.pdf","text":"Plate 25","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"A, Map of East Creek Valley showing area underlain by alluvium; B, North-South section of East Creek Valley showing inferred maximum depth to bedrock and the position of the water table in May 1957"},{"id":27876,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1475m/plate-1.pdf","text":"Plate 24","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of Bryce Canyon National Park area, Utah, showing physiographic features and the location of springs and wells"},{"id":138341,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1475m/report-thumb.jpg"},{"id":27879,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1475m/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27878,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1475m/plate-3.pdf","text":"Plate 26","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Logs of the test well at Bryce Canyon National Park, Utah"}],"country":"United States","state":"Utah","otherGeospatial":"Bryce Canyon National Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -112.47262325325637,\n 37.73847091078626\n ],\n [\n -112.47262325325637,\n 37.27074325321638\n ],\n [\n -112.06792128542472,\n 37.27074325321638\n ],\n [\n -112.06792128542472,\n 37.73847091078626\n ],\n [\n -112.47262325325637,\n 37.73847091078626\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66dde6","contributors":{"authors":[{"text":"Marine, I. Wendell","contributorId":49339,"corporation":false,"usgs":true,"family":"Marine","given":"I.","email":"","middleInitial":"Wendell","affiliations":[],"preferred":false,"id":144825,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2058,"text":"wsp1475O - 1963 - Hydrologic and geologic reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California","interactions":[{"subject":{"id":23112,"text":"ofr5672 - 1956 - A brief hydrologic and geologic reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California","indexId":"ofr5672","publicationYear":"1956","noYear":false,"title":"A brief hydrologic and geologic reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California"},"predicate":"SUPERSEDED_BY","object":{"id":2058,"text":"wsp1475O - 1963 - Hydrologic and geologic reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California","indexId":"wsp1475O","publicationYear":"1963","noYear":false,"chapter":"O","title":"Hydrologic and geologic reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California"},"id":1},{"subject":{"id":52115,"text":"ofr6090 - 1960 - Summary of hydrologic conditions at Joshua Tree National Monument, Riverside County, California, 1956-1959","indexId":"ofr6090","publicationYear":"1960","noYear":false,"title":"Summary of hydrologic conditions at Joshua Tree National Monument, Riverside County, California, 1956-1959"},"predicate":"SUPERSEDED_BY","object":{"id":2058,"text":"wsp1475O - 1963 - Hydrologic and geologic reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California","indexId":"wsp1475O","publicationYear":"1963","noYear":false,"chapter":"O","title":"Hydrologic and geologic reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California"},"id":2}],"lastModifiedDate":"2023-01-06T22:49:59.861671","indexId":"wsp1475O","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":"1475","chapter":"O","displayTitle":"Hydrologic and Geologic Reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California","title":"Hydrologic and geologic reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California","docAbstract":"Pinto basin, in the north-central part of Riverside County, Calif., is a typical desert valley formed by downfaulting along several major fault zones. The valley is filled with alluvium, and ground water in the alluvium discharges as subsurface outflow through an alluvium-filled gap at the east end of the valley. Occasionally surface water from cloudburst floods also discharges in a wash through the gap at the east end of the valley.\r\n\r\nA northeastward extension of the major fault along the south side of the valley acts as a barrier to the discharge of ground water from the valley. The average ground-water gradient is less than 1 foot per mile across the main part of the valley above this barrier, but the water level drops abruptly across the fault. The ground-water storage capacity of the uppermost 100 feet of saturated alluvium beneath the central valley area is estimated to be about 230,000 acre-feet. All this water in storage occurs at depths greater than 95 feet below the land surface and cannot be reached by plants or animals. During 1959 virtually all the water pumped in the area was withdrawn from storage. However, the quantity of water pumped is small in relation to the total quantity in storage. Except for a small decline in head, no evidence indicates that the pumping will greatly impair the yield for many years or cause the water to deteriorate in quality.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Hydrology of the Public Domain","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1475O","usgsCitation":"Kunkel, F., 1963, Hydrologic and geologic reconnaissance of Pinto Basin, Joshua Tree National Monument, Riverside County, California: U.S. Geological Survey Water Supply Paper 1475, Report: iii, 24 p.; 1 Plate: 30.90 x 20.80 inches, https://doi.org/10.3133/wsp1475O.","productDescription":"Report: iii, 24 p.; 1 Plate: 30.90 x 20.80 inches","startPage":"537","endPage":"561","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":27600,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1475o/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27599,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1475o/plate-28.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138561,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1475o/report-thumb.jpg"}],"scale":"62500","country":"United States","state":"California","county":"Riverside County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -115.733,\n 33.9\n ],\n [\n -115.733,\n 34\n ],\n [\n -115.333,\n 34\n ],\n [\n -115.333,\n 33.9\n ],\n [\n -115.733,\n 33.9\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a29e4b07f02db6118db","contributors":{"authors":[{"text":"Kunkel, Fred","contributorId":47766,"corporation":false,"usgs":true,"family":"Kunkel","given":"Fred","email":"","affiliations":[],"preferred":false,"id":144611,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2044,"text":"wsp1606 - 1963 - Geology and ground-water resources of Montgomery County, Alabama","interactions":[],"lastModifiedDate":"2022-02-02T15:02:35.456462","indexId":"wsp1606","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1606","title":"Geology and ground-water resources of Montgomery County, Alabama","docAbstract":"

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

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

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

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

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

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

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

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

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

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

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Doyle Blewer","contributorId":9633,"corporation":false,"usgs":true,"family":"Knowles","given":"Doyle","email":"","middleInitial":"Blewer","affiliations":[],"preferred":false,"id":144580,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reade, H. L.","contributorId":80244,"corporation":false,"usgs":true,"family":"Reade","given":"H. L.","affiliations":[],"preferred":false,"id":144582,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Scott, J. C.","contributorId":75901,"corporation":false,"usgs":true,"family":"Scott","given":"J.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":144581,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":32743,"text":"pp379 - 1963 - Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups","interactions":[],"lastModifiedDate":"2022-03-29T21:42:36.762876","indexId":"pp379","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"379","title":"Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups","docAbstract":"

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

","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp379","usgsCitation":"Denny, C.S., Lyford, W.H., and Goodlett, J.C., 1963, Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups: U.S. Geological Survey Professional Paper 379, Report: iv, 59 p.; 6 Plates: 41.94 × 24.00 inches or smaller, https://doi.org/10.3133/pp379.","productDescription":"Report: iv, 59 p.; 6 Plates: 41.94 × 24.00 inches or smaller","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":60663,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60662,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60661,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60660,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60659,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60664,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60665,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0379/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397823,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4377.htm"},{"id":121752,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0379/report-thumb.jpg"}],"scale":"250000","country":"United States","state":"New York, Pennsylvania","otherGeospatial":"Elmira-Williamsport region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.5,\n 41.1667\n ],\n [\n -76.25,\n 41.1667\n ],\n [\n -76.25,\n 42.5\n ],\n [\n -77.5,\n 42.5\n ],\n [\n -77.5,\n 41.1667\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae2e4b07f02db688b83","contributors":{"authors":[{"text":"Denny, Charles Storrow","contributorId":86331,"corporation":false,"usgs":true,"family":"Denny","given":"Charles","email":"","middleInitial":"Storrow","affiliations":[],"preferred":false,"id":209081,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lyford, Walter Henry","contributorId":43824,"corporation":false,"usgs":true,"family":"Lyford","given":"Walter","email":"","middleInitial":"Henry","affiliations":[],"preferred":false,"id":209080,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Goodlett, J. C.","contributorId":98771,"corporation":false,"usgs":true,"family":"Goodlett","given":"J.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":209082,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2031,"text":"wsp1595 - 1963 - Effects of hydraulic and geologic factors on streamflow of the Yakima River Basin, Washington","interactions":[],"lastModifiedDate":"2014-03-06T14:11:36","indexId":"wsp1595","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":"1595","title":"Effects of hydraulic and geologic factors on streamflow of the Yakima River Basin, Washington","docAbstract":"

The Yakima River basin, in south-central Washington, is the largest single river system entirely within the confines of the State. Its waters are the most extensively utilized of all the rivers in Washington.

\n
\n

The river heads high on the eastern slope of the Cascade Mountains, flows for 180 miles in a generally southeast direction, and discharges into the Columbia River. The western part of the basin is a mountainous area formed by sedimentary, volcanic, and metamorphic rocks, which generally have a low capacity for storing and transmitting water. The eastern part of the basin is. formed by a thick sequence of lava flows that have folded into long ridges and troughs. Downwarped structural basins between many of the ridges are partly filled with younger sedimentary deposits, which at some places are many hundreds of feet thick. The Yakima River flows from structural basin to structural basin through narrow water gaps that have been eroded through the anticlinal ridges. Each basin is also a topographic basin and a ground-water subbasin. A gaging station will measure the total outflow of a drainage area only if it is located at the surface outlet of a ground-water subbasin and then only if the stream basin is nearly coextensive with the ground-water subbasin. Many gaging stations in the Yakima basin are so located. The geology, hydrology, size. and location of 25 ground-water subbasins are described.

\n
\n

Since the settlement of the valley began, the development of the land and water resources have caused progressive changes in the natural regimen of the basin's runoff. These changes have resulted from diversion of water from the streams, the application of water on the land for irrigation, the storage and release of flood waters, the pumping of ground water, and other factors Irrigation in the Yakima basin is reported 'to have begun about 1864. In 1955 about 425,000 acres were under irrigation.

\n
\n

During the past 60-odd years many gaging stations have been operated at different sites within the basin. Only stations in the upper reaches, such as those below Keechelus, Kachess, or Cle Elum Lakes, give discharge records which are an accurate measure of the natural outflow of the drainage area. Farther down, stream, as the utilization of water becomes more extensive, the records at a gaging station show the discharge passing a particular point, but they do not reflect the natural outflow of the basin. Large canals divert water for use on lands above a station or carry it around a station for irrigation downstream. The deep sedimentary deposits within subbasins and the overlying alluvial gravels permit downvalley movement of large subsurface flows which bypass the gaging stations, except in the near vicinity of the water gaps. At the water gaps ground water rises to the surface, becoming streamflow, and can be accurately measured. The location of gaging stations within each subbasin is important, therefore, in determining whether the flow measured represents the total downvalley outflow or whether it is merely the surface-water component. Surface and subsurface factors that may affect the discharge records at each gaging station in the Yakima River basin include a description of upstream diversions, surface return flows, bypass canals, storage reservoirs, subsurface bypass flows, ground-water withdrawals, and other items. The available data are not sufficiently complete to permit a quantitative determination of the total basin yield at most gaging stations. However, data on the existing bypass channels, such as canals and drainage ditches, and on related subsurface movement of water provide valuable information necessary to proper use and interpretation of the streamflow records.

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1595","usgsCitation":"Kinnison, H.B., and Sceva, J.E., 1963, Effects of hydraulic and geologic factors on streamflow of the Yakima River Basin, Washington: U.S. Geological Survey Water Supply Paper 1595, Report: vii, 134 p.; 3 Plates: 29.5 x 30.0 inches or smaller, https://doi.org/10.3133/wsp1595.","productDescription":"Report: vii, 134 p.; 3 Plates: 29.5 x 30.0 inches or smaller","numberOfPages":"144","costCenters":[],"links":[{"id":137648,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1595/report-thumb.jpg"},{"id":27507,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1595/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27508,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1595/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27509,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1595/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27510,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1595/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"250000","country":"United States","state":"Washington","otherGeospatial":"Yakima River Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -124.8361,45.5437 ], [ -124.8361,49.0024 ], [ -116.9174,49.0024 ], [ -116.9174,45.5437 ], [ -124.8361,45.5437 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a29e4b07f02db611e92","contributors":{"authors":[{"text":"Kinnison, Hallard B.","contributorId":84337,"corporation":false,"usgs":true,"family":"Kinnison","given":"Hallard","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":144555,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sceva, Jack E.","contributorId":79086,"corporation":false,"usgs":true,"family":"Sceva","given":"Jack","email":"","middleInitial":"E.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":144554,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1849,"text":"wsp1724 - 1963 - Compilation of records of surface waters of the United States, October 1950 to September 1960: Part 2-B. South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","interactions":[],"lastModifiedDate":"2024-06-14T19:48:48.916459","indexId":"wsp1724","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":"1724","title":"Compilation of records of surface waters of the United States, October 1950 to September 1960: Part 2-B. South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","docAbstract":"

No abstract available.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1724","usgsCitation":"Hendricks, E.L., Cameron, A.N., Carroon, L., Hansen, F.N., Patterson, A.O., and Robinson, W., 1963, Compilation of records of surface waters of the United States, October 1950 to September 1960: Part 2-B. South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River: U.S. Geological Survey Water Supply Paper 1724, Report: xii, 458 p.; 1 Plate: 35.00 x 41.14 inches, https://doi.org/10.3133/wsp1724.","productDescription":"Report: xii, 458 p.; 1 Plate: 35.00 x 41.14 inches","costCenters":[],"links":[{"id":138531,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1724/report-thumb.jpg"},{"id":27066,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1724/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27067,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1724/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":430230,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24908.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Alabama, Florida, Georgia, Mississippi","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -89.35737160282241,\n 33.698278832471075\n ],\n [\n -88.69702258338809,\n 29.84689443382446\n ],\n [\n -84.02132259900962,\n 29.215685882027515\n ],\n [\n -82.90484068869881,\n 26.14880673764703\n ],\n [\n -80,\n 24.253746260036237\n ],\n [\n -79.78658787948709,\n 26.693806508190136\n ],\n [\n -81.05147466245297,\n 30.22780449206561\n ],\n [\n -81.0735277820245,\n 32.40780522836887\n ],\n [\n -85.40127425116972,\n 34.94678899158691\n ],\n [\n -89.35737160282241,\n 33.698278832471075\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1de4b07f02db6a9981","contributors":{"authors":[{"text":"Hendricks, E. L.","contributorId":50126,"corporation":false,"usgs":true,"family":"Hendricks","given":"E.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":144248,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cameron, A. N.","contributorId":339421,"corporation":false,"usgs":false,"family":"Cameron","given":"A.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":904224,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Carroon, L.E.","contributorId":29880,"corporation":false,"usgs":true,"family":"Carroon","given":"L.E.","affiliations":[],"preferred":false,"id":904225,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Hansen, F. N.","contributorId":80544,"corporation":false,"usgs":true,"family":"Hansen","given":"F.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":904226,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Patterson, A. O.","contributorId":339422,"corporation":false,"usgs":false,"family":"Patterson","given":"A.","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":904227,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Robinson, W.H.","contributorId":91478,"corporation":false,"usgs":true,"family":"Robinson","given":"W.H.","email":"","affiliations":[],"preferred":false,"id":904228,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":1800,"text":"wsp1669G - 1963 - Low-flow frequency curves for selected long-term stream gaging stations in eastern United States","interactions":[],"lastModifiedDate":"2012-02-02T00:05:15","indexId":"wsp1669G","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":"1669","chapter":"G","title":"Low-flow frequency curves for selected long-term stream gaging stations in eastern United States","docAbstract":"Curves showing the magnitude and frequency of annual low flow at 85 streamgaging stations located in 17 States east and 5 States west of the Mississippi River have been smoothed and adjusted to one of four long-term periods. They are presented to show the similarity and dissimilarity of curves even in the same State and to provide background information for studies of the statistical properties of low-flow frequency curves and for studies of the relation between hydrologic environment and low flow. The results are presented as greatly reduced graphs to facilitate comparison and are summarized in tables from which expanded graphs can be plotted.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States, 1962","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"ENGLISH","publisher":"U.S. Govt. Print. Off. :\r\nfor sale by the Supt. of Docs., U.S. Govt. Print. Off.,","doi":"10.3133/wsp1669G","usgsCitation":"Hardison, C.H., and Martin, R.O., 1963, Low-flow frequency curves for selected long-term stream gaging stations in eastern United States: U.S. Geological Survey Water Supply Paper 1669, iv, 30 p. :ill., map ;24 cm., https://doi.org/10.3133/wsp1669G.","productDescription":"iv, 30 p. :ill., map ;24 cm.","costCenters":[],"links":[{"id":137012,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669g/report-thumb.jpg"},{"id":26955,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669g/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db648748","contributors":{"authors":[{"text":"Hardison, Clayton H.","contributorId":46073,"corporation":false,"usgs":true,"family":"Hardison","given":"Clayton","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144178,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Martin, Robert O.R.","contributorId":18737,"corporation":false,"usgs":true,"family":"Martin","given":"Robert","email":"","middleInitial":"O.R.","affiliations":[],"preferred":false,"id":144177,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1298,"text":"wsp1419 - 1963 - Geologic and hydrologic features of the San Bernardino area, California; with special reference to underflow across the San Jacinto fault","interactions":[{"subject":{"id":51238,"text":"ofr5358 - 1953 - San Bernardion Area, California: Three maps showing water-level contours for the San Bernardino area for spring 1936, spring 1945, and spring 1951; east-west geologic section from Colton to Mill Creek Canyon; geologic section from Shandin Hills southeast to Bryn Mawr; and water level profiles along the section from Colton to Mill Creek Canyon","indexId":"ofr5358","publicationYear":"1953","noYear":false,"title":"San Bernardion Area, California: Three maps showing water-level contours for the San Bernardino area for spring 1936, spring 1945, and spring 1951; east-west geologic section from Colton to Mill Creek Canyon; geologic section from Shandin Hills southeast to Bryn Mawr; and water level profiles along the section from Colton to Mill Creek Canyon"},"predicate":"SUPERSEDED_BY","object":{"id":1298,"text":"wsp1419 - 1963 - Geologic and hydrologic features of the San Bernardino area, California; with special reference to underflow across the San Jacinto fault","indexId":"wsp1419","publicationYear":"1963","noYear":false,"title":"Geologic and hydrologic features of the San Bernardino area, California; with special reference to underflow across the San Jacinto fault"},"id":1},{"subject":{"id":51253,"text":"ofr5376 - 1953 - Maps and sections showing ground-water conditions in the San Bernardino area, California","indexId":"ofr5376","publicationYear":"1953","noYear":false,"title":"Maps and sections showing ground-water conditions in the San Bernardino area, California"},"predicate":"SUPERSEDED_BY","object":{"id":1298,"text":"wsp1419 - 1963 - Geologic and hydrologic features of the San Bernardino area, California; with special reference to underflow across the San Jacinto fault","indexId":"wsp1419","publicationYear":"1963","noYear":false,"title":"Geologic and hydrologic features of the San Bernardino area, California; with special reference to underflow across the San Jacinto fault"},"id":2}],"lastModifiedDate":"2022-02-01T20:10:25.234553","indexId":"wsp1419","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":"1419","title":"Geologic and hydrologic features of the San Bernardino area, California; with special reference to underflow across the San Jacinto fault","docAbstract":"

This is the second in a series of interpretive reports on subsurface outflow from the ground-water basins of San Bernardino County, Calif., prepared by the U.S. Geological Survey in cooperation with the San Bernardino County Flood Control District. One principal purpose of the study was to estimate the ground-water outflow from the Bunker Hill basin to the Rialto-Colton basin across the San Jacinto fault, which, except locally, forms a nearly impermeable boundary between the two basins. In addition, the report deals qualitatively with the geology, the fault barriers that divide the area into several ground-water basins, the physical nature and degree of imperviousness of the barriers, the occurrence and movement of ground water and fluctuations of water level in the basins, and the chemical quality of surface and ground waters in the San Bernardino area. The report includes a geologic map and sections, water-level-contour maps and profiles, and hydrographs of selected well. The Santa Ana River, the principal stream, flows generally westward across the area. Channels of the river and its tributaries overlie a large irregular structural depression filled with alluvial deposits ranging in age from late Tertiary to Recent and forming a valley bounded on the north by the San Gabriel Mountains, on the east by the San Bernardino Mountains, and on the south by an irregular group of hills. Large alluvial fans underlie most of the area, but its landforms also include alluvial benches and terraces near the mountains, stream channels, and elongate hills, ridges, and scarps along the trace of the San Jacinto fault, which strikes northwestward across the valley about in the center of the area. This fault and others divide the area into ground-water basins, which include the Bunker Hill, Rialto-Colton, upper and lower Lytle and Chino basins. The water-bearing deposits include the following units: the younger alluvium. of Recent age, which occupies principally the backfilled channels beneath the Santa Ana River and its tributaries and through which ground water moves from Bunker Hill basin to Rialto-Colton basin; the older alluvium, of Pleistocene age, which is the principal water-bearing unit of the area and yields water to more than a thousand wells; and continental deposits of Tertiary to Quaternary age, which crop out along the southern margin of the area and locally along the San Gabriel Mountains on the north. The younger alluvium attains a maximum thickness of about 125 feet beneath the Santa Ana River south of San Bernardino. Locally in the Bunker Hill basin it is composed of two members, an upper member of relatively impermeable clay and a lower member of highly permeable material in which water is confined by the upper member. The older alluvium locally has a known thickness greater than 700 feet; elsewhere in the San Bernardino Valley it may exceed 1,400 feet. Locally, where ground water is confined in Bunker Hill basin, the older alluvium is divided into three permeable water-bearing zones separated from each other and from the younger alluvium above by less permeable zones. In parts of Chino and Rialto-Colton basins the alluvium consists of a coarse-grained facies along a former course of a major stream that is interfingered with and overlain by relatively fine-grained deposits. The permeability of the younger alluvium in the area beneath the Santa Ana River downstream from the San Jacinto fault was determined from tests to be about 2,700 gallons per day per square foot. The permeability of the coarse water-yielding materials of the older alluvium several miles downstream was estimated from tests to be about the same magnitude. Rocks that yield practically no water include continental rocks of Tertiary age, which are not exposed in the area but are tapped by wells in Rialto-Colton basin, and crystalline and metamorphic rocks of pre-Tertiary age that form the bedrock of the area.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1419","usgsCitation":"Dutcher, L., and Garrett, A., 1963, Geologic and hydrologic features of the San Bernardino area, California; with special reference to underflow across the San Jacinto fault: U.S. Geological Survey Water Supply Paper 1419, Report: vi, 114 p.; 19 Plates: \t37.00 × 52.19 inches or smaller, https://doi.org/10.3133/wsp1419.","productDescription":"Report: vi, 114 p.; 19 Plates: \t37.00 × 52.19 inches or smaller","costCenters":[],"links":[{"id":26304,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26303,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26302,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26301,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26300,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26299,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26298,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26297,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26296,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26295,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26294,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26293,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26310,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-19.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26292,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26309,"rank":417,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-18.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26308,"rank":416,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-17.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26307,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26306,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26305,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1419/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26311,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1419/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137046,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1419/report-thumb.jpg"},{"id":395239,"rank":22,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24373.htm"}],"country":"United States","state":"California","otherGeospatial":"San Bernardino area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.41638183593749,\n 33.96272530662602\n ],\n [\n -117.01675415039064,\n 33.96272530662602\n ],\n [\n -117.01675415039064,\n 34.1902217928623\n ],\n [\n -117.41638183593749,\n 34.1902217928623\n ],\n [\n -117.41638183593749,\n 33.96272530662602\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a81b0","contributors":{"authors":[{"text":"Dutcher, L.C.","contributorId":42191,"corporation":false,"usgs":true,"family":"Dutcher","given":"L.C.","email":"","affiliations":[],"preferred":false,"id":143522,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Garrett, Arthur A.","contributorId":38960,"corporation":false,"usgs":true,"family":"Garrett","given":"Arthur A.","affiliations":[],"preferred":false,"id":143521,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":35360,"text":"b1133C - 1963 - Geology and hydrology of the Elk River, Minnesota, nuclear-reactor site","interactions":[],"lastModifiedDate":"2018-03-19T10:38:39","indexId":"b1133C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1133","chapter":"C","title":"Geology and hydrology of the Elk River, Minnesota, nuclear-reactor site","docAbstract":"

The Elk River, Minn., nuclear-reactor site is on the east bluff of the Mississippi River about 35 miles northwest of Minneapolis and St. Paul. The area is underlain by about 70 to 180 feet of glacial drift, including at the top as much as 120 feet of outwash deposits (valley train) of the glacial Mississippi River. The underlying Cambrian bedrock consists of marine sedimentary formations including artesian sandstone aquifers. A hypothetically spilled liquid at the reactor site could follow one or both of two courses, thus: (1) It could flow over the land surface and through an artificial drainage system to the river in a matter of minutes; (2) part or nearly all of it could seep downward to the water table and then move laterally to the river. The time required might range from a few weeks to a year, or perhaps more. The St. Paul and Minneapolis water-supply intakes, 21 and 25 miles downstream, respectively, are the most critical points to be considered in the event of an accidental spill. Based on streamflow and velocity data for the Mississippi River near Anoka, the time required for the maximum concentration of a contaminant to travel from the reactor site to the St. Paul intake was computed to be about 8 hours, at the median annual maximum daily discharge. For this discharge, the maximum concentration at the intake would be about 0.0026 microcurie per cubic foot for the release of 1 curie of activity into the river near the reactor site.

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/b1133C","collaboration":"Prepared in cooperation with the U.S. Atomic Energy Commission","usgsCitation":"Norvitch, R.F., Schneider, R., and Godfrey, R.G., 1963, Geology and hydrology of the Elk River, Minnesota, nuclear-reactor site: U.S. Geological Survey Bulletin 1133, Document: iv, 25 p.; 2 Plates: 18 x 16 inches, https://doi.org/10.3133/b1133C.","productDescription":"Document: iv, 25 p.; 2 Plates: 18 x 16 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":63222,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1133c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":63223,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1133c/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":63224,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1133c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109385,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20849.htm","linkFileType":{"id":5,"text":"html"},"description":"20849"},{"id":165594,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1133c/report-thumb.jpg"}],"country":"United States","state":"Minnesota","city":"Elk River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.61209869384766,\n 45.261596972270866\n ],\n [\n -93.61209869384766,\n 45.3297027614069\n ],\n [\n -93.51133346557617,\n 45.3297027614069\n ],\n [\n -93.51133346557617,\n 45.261596972270866\n ],\n [\n -93.61209869384766,\n 45.261596972270866\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b468c","contributors":{"authors":[{"text":"Norvitch, Ralph F.","contributorId":65456,"corporation":false,"usgs":true,"family":"Norvitch","given":"Ralph","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":214511,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schneider, Robert","contributorId":102460,"corporation":false,"usgs":true,"family":"Schneider","given":"Robert","email":"","affiliations":[],"preferred":false,"id":214513,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Godfrey, Richard G.","contributorId":100046,"corporation":false,"usgs":true,"family":"Godfrey","given":"Richard","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":214512,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1198,"text":"wsp1611 - 1963 - Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina","interactions":[{"subject":{"id":51133,"text":"ofr5275 - 1952 - Results of chloride determinations of water samples from observation wells in the Savannah area, Georgia, October 1952","indexId":"ofr5275","publicationYear":"1952","noYear":false,"title":"Results of chloride determinations of water samples from observation wells in the Savannah area, Georgia, October 1952"},"predicate":"SUPERSEDED_BY","object":{"id":1198,"text":"wsp1611 - 1963 - Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina","indexId":"wsp1611","publicationYear":"1963","noYear":false,"title":"Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina"},"id":1},{"subject":{"id":51881,"text":"ofr55189 - 1955 - A summary of the artesian-water resources in the Savannah area, Georgia, and an outline of additional studies needed","indexId":"ofr55189","publicationYear":"1955","noYear":false,"title":"A summary of the artesian-water resources in the Savannah area, Georgia, and an outline of additional studies needed"},"predicate":"SUPERSEDED_BY","object":{"id":1198,"text":"wsp1611 - 1963 - Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina","indexId":"wsp1611","publicationYear":"1963","noYear":false,"title":"Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina"},"id":2},{"subject":{"id":52045,"text":"ofr49107 - 1949 - Ground-water investigations in the Savannah area, Georgia - South Carolina","indexId":"ofr49107","publicationYear":"1949","noYear":false,"title":"Ground-water investigations in the Savannah area, Georgia - South Carolina"},"predicate":"SUPERSEDED_BY","object":{"id":1198,"text":"wsp1611 - 1963 - Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina","indexId":"wsp1611","publicationYear":"1963","noYear":false,"title":"Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina"},"id":3}],"lastModifiedDate":"2022-12-13T22:42:58.178248","indexId":"wsp1611","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":"1611","title":"Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina","docAbstract":"The Savannah area consists of about 2,300 square miles of the Coastal Plain along the coast of eastern Georgia and southeastern South Carolina. Savannah is near the center of the area. Most of the large ground-water developments are in or near Savannah. About 98 percent of the approximately 60 mgd of ground water used is pumped from the principal artesian aquifer, which is composed of about 600 feet of limestone of middle Eocene, Oligocene, and early Miocene ages. \r\n\r\nIndustrial and other wells of large diameter yield as much as 4,200 gpm from the principal artesian aquifer. Pumping tests and flow-net analyses show that the coefficient of transmissibility averages about 200,000 gpd per ft in the immediate Savannah area. The specific capacity of wells in the principal artesian aquifer generally is about 50 gpm per ft of drawdown. The coefficient of storage of the principal artesian aquifer is about 0.0003 in the Savannah area. \r\n\r\nUnderlying the Savannah area are a series of unconsolidated and semiconsolidated sediments ranging in age from Late Cretaceous to Recent. The Upper Cretaceous, Paleocene, and lower Eocene sediments supply readily available and usable water in other parts of the Coastal Plain, but although the character and physical properties of these formations are similar in the Savannah area to the same properties in other areas, the hydraulic and structural conditions appear to be different. Deep test wells are needed to evaluate the ground-water potential of these rocks. \r\n\r\nThe lower part of the sediments of middle Eocene age acts as a confining layer to the vertical movement of water into or out of the principal artesian aquifer. Depending on the location and depth, the principal artesian aquifer consists of from one to five geologic units. The lower boundary of the aquifer is determined by a reduction in permeability and an increase in salt-water content. Although the entire limestone section is considered water bearing, most of the ground water used in the area comes from the upper part of the Ocala limestone of late Eocene age and the limestones of Oligocene age. The greatest volume of water comes from the upper part of the Ocala limestone, but the greatest number of wells are supplied from the rocks of Oligocene age. The Tampa limestone and Hawthorn formation of early Miocene age are generally water bearing; the amount and quality of the water depends on the location. The water from some wells in the Tampa and most of the water from the Hawthorn is high in hydrogen sulfide. \r\n\r\nIn the northeastern part of the area the principal artesian aquifer is close to the land surface. Here the confining layer is thin and in some of the estauaries it may be completely cut through by the scouring action of the streams during tidal fluctuations. In this part of the area artesian groundwater at one time discharged from the aquifer as submarine springs. Now a reverse effect may be occurring; ocean and river water may be entering the aquifer. \r\n\r\nThe silts, clays, and very fine sands of the upper Miocene and Pliocene ( ?) series generally have low permeabilities and form the upper confining layer for the principal artesian aquifer. Although all the sediments overlying the principal artesian aquifer are considered to be part of the confining layer, locally some of the upper units are water bearing. \r\n\r\nThe uppermost geologic units in the Savannah area are sediments of Pliocene ( ?) to Recent age and consist of sands, silts, and clays with shell and gravel beds which are a source of water for shallow wells. \r\n\r\nThe first large ground-water supply from the principal artesian aquifer was developed in 1886 by the city of Savannah. Additional municipal and industrial supplies have been developed since that time. Pumpage progressively increased to a peak of 62 mgd in 1957. Outside of the city and industrial area the 1957 pumpage was about 9 mgd. In 1958 the total pumpage in the Savannah area was about 68 mgd or about 3 mgd less th","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1611","usgsCitation":"Counts, H.B., and Donsky, E., 1963, Salt-water encroachment, geology, and ground-water resources of Savannah area, Georgia and South Carolina: U.S. Geological Survey Water Supply Paper 1611, Report: v, 100 p.; 6 Plates: 18.00 x 24.00 inches or smaller, https://doi.org/10.3133/wsp1611.","productDescription":"Report: v, 100 p.; 6 Plates: 18.00 x 24.00 inches or smaller","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":26070,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1611/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26076,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1611/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26075,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1611/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26074,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1611/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26073,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1611/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26072,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1611/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137867,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1611/report-thumb.jpg"},{"id":26071,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1611/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":410421,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24801.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Georgia, South Carolina","city":"Savannah","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.5,\n 31.75\n ],\n [\n -80.667,\n 31.75\n ],\n [\n -80.667,\n 32.75\n ],\n [\n -81.5,\n 32.75\n ],\n [\n -81.5,\n 31.75\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ee4b07f02db5fdee4","contributors":{"authors":[{"text":"Counts, H. 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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":41127,"text":"ofr6328 - 1963 - Preliminary geologic map of part of the Rapid City East quadrangle, South Dakota","interactions":[{"subject":{"id":41127,"text":"ofr6328 - 1963 - Preliminary geologic map of part of the Rapid City East quadrangle, South Dakota","indexId":"ofr6328","publicationYear":"1963","noYear":false,"title":"Preliminary geologic map of part of the Rapid City East quadrangle, South Dakota"},"predicate":"SUPERSEDED_BY","object":{"id":63245,"text":"gq986 - 1972 - Geologic map of the Rapid City East quadrangle, Pennington County, South Dakota","indexId":"gq986","publicationYear":"1972","noYear":false,"title":"Geologic map of the Rapid City East quadrangle, Pennington County, South Dakota"},"id":1}],"supersededBy":{"id":63245,"text":"gq986 - 1972 - Geologic map of the Rapid City East quadrangle, Pennington County, South Dakota","indexId":"gq986","publicationYear":"1972","noYear":false,"title":"Geologic map of the Rapid City East quadrangle, Pennington County, South Dakota"},"lastModifiedDate":"2019-11-26T10:55:01","indexId":"ofr6328","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":"63-28","title":"Preliminary geologic map of part of the Rapid City East quadrangle, South Dakota","docAbstract":"

No abstract available.

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The segment of the abandoned pre-Pleistocene Teays Valley between Scary and Huntington, W. Va. stands 130-240 feet above the Ohio and Kanawha rivers, and its bedrock floor slopes westward at about 0.6 foot per mile. The bedrock floor is overlain by highly weathered gravel in which a soil profile developed; only resistant siliceous materials remain. As much as 100 feet of locally derived sediments overlies the basal gravel. Sand was deposited at each end of the valley but in the east-central part it grades laterally into a laminated silty clay that was deposited during a period of ponding, probably in Kansan time. These deposits are deeply eroded. Probably during Illinoian time, ponding at a lower level resulted in deposition of a younger silty clay in the western part of the valley. This silty clay is weathered to a depth of about 14 feet. During a brief ponding in Wisconsin time, a widely scattered veneer of ice-rafted unweathered pebbles of igneous and metamorphic rocks was deposited. This veneer represents the youngest Pleistocene deposits in the valley and it occurs as much as 110 feet above the present Ohio River. Depositional, weathering, erosional, and topographic evidence argues that the Teays Valley in West Virginia was abandoned in late Tertiary or early Pleistocene time by normal stream-capture processes and that prolonged weathering followed. © 1963, The Geological Society of America, Inc.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[251:GHOTTV]2.0.CO;2","issn":"00167606","usgsCitation":"Rhodehamel, E., and Carlston, C., 1963, Geologic history of the teays valley in West Virginia: Geological Society of America Bulletin, v. 74, no. 3, p. 251-274, https://doi.org/10.1130/0016-7606(1963)74[251:GHOTTV]2.0.CO;2.","productDescription":"24 p.","startPage":"251","endPage":"274","costCenters":[],"links":[{"id":370269,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"West Virginia 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C.","contributorId":91517,"corporation":false,"usgs":true,"family":"Rhodehamel","given":"E. C.","affiliations":[],"preferred":false,"id":777490,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Carlston, C.W.","contributorId":26062,"corporation":false,"usgs":true,"family":"Carlston","given":"C.W.","affiliations":[],"preferred":false,"id":777491,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70221118,"text":"70221118 - 1963 - Early pennsylvanian currents in the southern Appalachian Mountains","interactions":[],"lastModifiedDate":"2021-06-04T12:02:11.312222","indexId":"70221118","displayToPublicDate":"1963-11-01T11:00:12","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Early pennsylvanian currents in the southern Appalachian Mountains","docAbstract":"

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

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

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

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

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

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

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

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

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[1439:EPCITS]2.0.CO;2","usgsCitation":"Schlee, J., 1963, Early pennsylvanian currents in the southern Appalachian Mountains: Geological Society of America Bulletin, v. 74, no. 12, p. 1439-1451, https://doi.org/10.1130/0016-7606(1963)74[1439:EPCITS]2.0.CO;2.","productDescription":"13 p.","startPage":"1439","endPage":"1451","costCenters":[],"links":[{"id":386132,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Kentucky, Tennessee, Alabama, Georgia","otherGeospatial":"southern Appalachian Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.58447265624999,\n 37.16031654673677\n ],\n [\n -84.561767578125,\n 35.71975793933433\n ],\n [\n -86.59423828125,\n 34.66935854524543\n ],\n [\n -85.902099609375,\n 34.161818161230386\n ],\n [\n -81.090087890625,\n 36.54494944148322\n ],\n [\n -80.595703125,\n 37.06394430056685\n ],\n [\n -81.58447265624999,\n 37.16031654673677\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"74","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Schlee, John","contributorId":16078,"corporation":false,"usgs":true,"family":"Schlee","given":"John","affiliations":[],"preferred":false,"id":816796,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221798,"text":"70221798 - 1963 - Reef Creek Detachment Fault, Northwestern Wyoming","interactions":[],"lastModifiedDate":"2021-07-07T13:13:32.878063","indexId":"70221798","displayToPublicDate":"1963-07-07T08:10:45","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Reef Creek Detachment Fault, Northwestern Wyoming","docAbstract":"

he Reef Creek fault is in northwestern Wyoming, a few miles east of the northeast border of Yellowstone National Park. It lies within the area covered by the more extensive Heart Mountain fault. Like that fault, it is a décollement or detachment fault in which strata became detached along a basal shearing plane and moved laterally on a slightly inclined fault surface. At the most northwesterly exposures the Reef Creek fault parallels the bedding; southeastward it cuts upward across the bedding as a transgressive fault and becomes a fault in which the allochthonous blocks moved on the surface of the ground. The fault blocks consist chiefly of the Madison Limestone of Mississippian age and volcanic tuffs and breccias of the Cathedral Cliffs Formation of early or middle Eocene age. The Reef Creek fault blocks are scattered over a 7- by 14-mile area, but a considerable part of the scattering is due to “piggy-back” transportation on the Heart Mountain fault blocks.

The Reef Creek fault is younger than the Cathedral Cliffs Formation and older than the middle Eocene early basic breccia. Consequently, the rocks transported by it were emplaced either in late early Eocene or in early middle Eocene time. Both the Reef Creek fault and the South Fork fault are older than the principal movement along the Heart Mountain fault. The movement of all three fault masses was southeastward, and the mechanics of their emplacement is believed to have been similar. Movement was due in part to gravity, but considering the low slope involved, gravity alone seems to be inadequate. The shaking motion of many earthquakes is suggested as a contributing force which acted in conjunction with the constant force of gravity.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[1225:RCDFNW]2.0.CO;2","usgsCitation":"Pierce, W., 1963, Reef Creek Detachment Fault, Northwestern Wyoming: GSA Bulletin, v. 74, no. 10, p. 1225-1236, https://doi.org/10.1130/0016-7606(1963)74[1225:RCDFNW]2.0.CO;2.","productDescription":"12 p.","startPage":"1225","endPage":"1236","costCenters":[],"links":[{"id":386990,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wyoming","otherGeospatial":"Reef Creek Detachment Fault","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -110.23681640625,\n 44.22945656830167\n ],\n [\n -108.91845703124999,\n 44.22945656830167\n ],\n [\n -108.91845703124999,\n 45.089035564831036\n ],\n [\n -110.23681640625,\n 45.089035564831036\n ],\n [\n -110.23681640625,\n 44.22945656830167\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"74","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Pierce, William G.","contributorId":103349,"corporation":false,"usgs":true,"family":"Pierce","given":"William G.","affiliations":[],"preferred":false,"id":818760,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221089,"text":"70221089 - 1963 - Saline ground water — A little used and unmapped resource","interactions":[],"lastModifiedDate":"2021-06-01T19:19:26.466115","indexId":"70221089","displayToPublicDate":"1963-07-01T14:16:32","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Saline ground water — A little used and unmapped resource","docAbstract":"

Vast quantities of saline ground water await new commercial uses and economical demineralization processes for recognition as a valuable resource. Saline ground water is more widely distributed than any other natural resource, occurring throughout the United States and in geologic formations ranging from the oldest to the youngest. The Coastal Plain has the greatest reserve of fresh water in the country, but at depths ranging from a few feet to about 3,500 feet most of the fresh‐water aquifers also contain large quantities of brackish water. Paleozoic formations in the east‐central United States have long been producers of saline water as commercial brines and in association with oil and gas. The volume of saline ground water perhaps exceeds the fresh ground‐water supply in the Great Plains Region. The greater part of the Western Mountain Region is generally deficient in fresh ground water; however, saline water is present in highly permeable deposits in numerous closed basins and along saline streams. In each of these major ground‐water regions small to very large amounts of saline water can be pumped from wells ranging from a few tens of feet to several thousand feet in depth. Knowledge of saline water distribution is general and inadequate, having been attained as a by‐product of investigations of fresh‐water supplies. This knowledge should be expanded as technological advances in demineralization processes enhance the importance of saline water for potential supply in numerous water‐deficient areas. 

","language":"English","publisher":"Wiley Blackwell","doi":"10.1111/j.1745-6584.1963.tb01921.x","usgsCitation":"Poole, J.L., 1963, Saline ground water — A little used and unmapped resource: Groundwater, v. 1, no. 3, p. 18-20, https://doi.org/10.1111/j.1745-6584.1963.tb01921.x.","productDescription":"3 p.","startPage":"18","endPage":"20","costCenters":[],"links":[{"id":386068,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"1","issue":"3","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Poole, J. L.","contributorId":40583,"corporation":false,"usgs":true,"family":"Poole","given":"J.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":816722,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221085,"text":"70221085 - 1963 - Composite dike of andesite and rhyolite at Klondyke, Arizona","interactions":[],"lastModifiedDate":"2021-06-01T19:01:24.681121","indexId":"70221085","displayToPublicDate":"1963-07-01T13:55:24","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Composite dike of andesite and rhyolite at Klondyke, Arizona","docAbstract":"

A composite dike of probable Tertiary age intrudes Precambrian granodiorite 6 miles north of Klondyke, Arizona. The dike is exposed discontinuously for about 1500 feet along the strike and has a core of porphyritic rhyolite 15-20 feet thick flanked by coarsely porphyritic andesite 1-2 feet thick. Field evidence indicates that the rhyolite is later than the andesite but that the core of the original andesite dike was still hot and unconsolidated at the time of intrusion of the rhyolite. Chemically, the rhyolite is nearly identical to a large alkali granite pluton of Tertiary age exposed 1 mile east. The andesite component is similar both petrographically and chemically to lavas exposed in the region, but a direct relationship could not be established. Meager evidence suggests that the two dike components were derived from separate magma bodies rather than being differentiates of a single magma.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[1049:CDOAAR]2.0.CO;2","usgsCitation":"Simons, F.S., 1963, Composite dike of andesite and rhyolite at Klondyke, Arizona: Geological Society of America Bulletin, v. 74, no. 8, p. 1049-1056, https://doi.org/10.1130/0016-7606(1963)74[1049:CDOAAR]2.0.CO;2.","productDescription":"8 p.","startPage":"1049","endPage":"1056","costCenters":[],"links":[{"id":386059,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona","otherGeospatial":"Klondyke area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -110.61035156249999,\n 32.967195229355916\n ],\n [\n -110.2642822265625,\n 32.967195229355916\n ],\n [\n -110.2642822265625,\n 33.119150226768866\n ],\n [\n -110.61035156249999,\n 33.119150226768866\n ],\n [\n -110.61035156249999,\n 32.967195229355916\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"74","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Simons, Frank S.","contributorId":42203,"corporation":false,"usgs":true,"family":"Simons","given":"Frank","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":816714,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221078,"text":"70221078 - 1963 - Overlapping of late mesozoic orogens in western Idaho","interactions":[],"lastModifiedDate":"2021-06-01T17:57:50.73863","indexId":"70221078","displayToPublicDate":"1963-04-01T12:53:24","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Overlapping of late mesozoic orogens in western Idaho","docAbstract":"

Early formed rocks of the border zone of the Idaho batholith are thrust westward over the low-grade metavolcanic rocks of the Seven Devils Mountains. Late intrusions of the border zone cut out upper plate rocks and contact-metamorphose lower plate rocks. Granitic intrusions in the Seven Devils complex are metamorphosed near the border zone of the Idaho batholith. Such relationships are interpreted in the light of a regional synthesis to indicate the overlapping and oblique truncation of the eastern part of a belt deformed largely during Jurassic time by the western part of a tectonic belt active during early stages of the middle Cretaceous events that produced the Idaho batholith. 

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[779:OOLMOI]2.0.CO;2","usgsCitation":"Hamilton, W., 1963, Overlapping of late mesozoic orogens in western Idaho: Geological Society of America Bulletin, v. 74, no. 6, p. 779-787, https://doi.org/10.1130/0016-7606(1963)74[779:OOLMOI]2.0.CO;2.","productDescription":"9 p.","startPage":"779","endPage":"787","costCenters":[],"links":[{"id":386054,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Idaho","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.02636718749999,\n 49.009050809382046\n ],\n [\n -117.1142578125,\n 46.34692761055676\n ],\n [\n -116.47705078125,\n 45.67548217560647\n ],\n [\n -117.26806640625,\n 44.32384807250689\n ],\n [\n -117.09228515624999,\n 43.8028187190472\n ],\n [\n -117.0703125,\n 42.01665183556825\n ],\n [\n -111.09374999999999,\n 41.95131994679697\n ],\n [\n -111.11572265625,\n 44.99588261816546\n ],\n [\n -112.30224609374999,\n 44.49650533109348\n ],\n [\n -113.09326171875,\n 44.402391829093915\n ],\n [\n -113.04931640625,\n 44.809121700077355\n ],\n [\n -113.88427734374999,\n 45.69083283645816\n ],\n [\n -114.36767578124999,\n 46.694667307773116\n ],\n [\n -115.86181640625001,\n 47.73932336136857\n ],\n [\n -116.01562499999999,\n 48.004625021133904\n ],\n [\n -116.05957031249999,\n 48.96579381461063\n ],\n [\n -117.02636718749999,\n 49.009050809382046\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"74","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hamilton, Warren","contributorId":14819,"corporation":false,"usgs":true,"family":"Hamilton","given":"Warren","affiliations":[],"preferred":false,"id":816708,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70195915,"text":"70195915 - 1963 - Late Pleistocene glacial drainage in the Devils Lake Region, North Dakota","interactions":[],"lastModifiedDate":"2018-03-07T16:17:10","indexId":"70195915","displayToPublicDate":"1963-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Late Pleistocene glacial drainage in the Devils Lake Region, North Dakota","docAbstract":"

The Devils Lake region of northeastern North Dakota is covered with glacial drift deposited by the Leeds lobe of the Mankato Substage of the Wisconsin Stage of the Pleistocene and is underlain by Pierre Shale of Cretaceous age. Associated with the Sheyenne River, which flows through the southern part of the region in a deep trench, are many stream terraces, spillways, deposits of ice-contact stratified drift, and eroded ground-moraine areas. Six stages of drainage have been established to which these various features can be assigned. In the first two stages the features formed as melt water drained to the glacial James River south of the region and as the ice front stood at and later retreated from the site of the Heimdal moraine, a recessional moraine of the Leeds lobe. The later stages occurred after the valley of the Sheyenne River was free of ice and after glacial Lake Souris northwest of the region drained down the valley to glacial Lake Agassiz in the eastern part of the state. Features originating during the four later stages are largely related to the deposition of the North Viking moraine (another, more northern, recessional moraine of the Leeds lobe) and subsequent retreat of the ice from the moraine. Discharge from the local Devils and Stump lakes and from glacial Lake Souris also were of considerable importance in the genesis of many features.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1963)74[859:LPGDIT]2.0.CO;2","usgsCitation":"Aronow, S., 1963, Late Pleistocene glacial drainage in the Devils Lake Region, North Dakota: GSA Bulletin, v. 74, no. 7, p. 859-874, https://doi.org/10.1130/0016-7606(1963)74[859:LPGDIT]2.0.CO;2.","productDescription":"16 p.","startPage":"859","endPage":"874","costCenters":[{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":352309,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"North Dakota","otherGeospatial":"Devils Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -99.25,\n 47.75\n ],\n [\n -98.25,\n 47.75\n ],\n [\n -98.25,\n 48\n ],\n [\n -99.25,\n 48\n ],\n [\n -99.25,\n 47.75\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"74","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5aff6264e4b0da30c1bfde80","contributors":{"authors":[{"text":"Aronow, Saul","contributorId":59509,"corporation":false,"usgs":true,"family":"Aronow","given":"Saul","email":"","affiliations":[],"preferred":false,"id":730482,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1149,"text":"wsp1669C - 1963 - Hydrology of upper Black Earth Creek basin, Wisconsin, with a section on surface water","interactions":[{"subject":{"id":52076,"text":"ofr6029 - 1960 - A preliminary report of the geology and ground-water resources of Upper Black Earth Creek Basin, Wisconsin, with a section on surface water","indexId":"ofr6029","publicationYear":"1960","noYear":false,"title":"A preliminary report of the geology and ground-water resources of Upper Black Earth Creek Basin, Wisconsin, with a section on surface water"},"predicate":"SUPERSEDED_BY","object":{"id":1149,"text":"wsp1669C - 1963 - Hydrology of upper Black Earth Creek basin, Wisconsin, with a section on surface water","indexId":"wsp1669C","publicationYear":"1963","noYear":false,"chapter":"C","title":"Hydrology of upper Black Earth Creek basin, Wisconsin, with a section on surface water"},"id":1}],"lastModifiedDate":"2023-11-27T21:46:12.820397","indexId":"wsp1669C","displayToPublicDate":"1963-01-01T00:00:00","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":"1669","chapter":"C","title":"Hydrology of upper Black Earth Creek basin, Wisconsin, with a section on surface water","docAbstract":"

The upper Black Earth Creek drainage basin has an area of 46 square miles and is in Dane County in south-central Wisconsin. The oldest rock exposed in the valley walls is the sandstone of Late Cambrian age. Dolomite of the Prairie du Chien Group of Ordovician age overlies the sandstone and forms the. resistant cap on the hills. The St. Peter Sandstone, Platteville and Decorah Formations, and Galena Dolomite, all Ordovician in age, form a narrow belt along the southern boundary of the area. Outwash and alluvium of Pleistocene and Recent age fill the valleys. The eastern half of the area was glaciated and is covered with till. The sandstone of Late Cambrian age and the sand and gravel of the outwash deposits are hydraulically connected. Ground water occurs under unconfined (water-table) conditions in the western unglaciated part of the basin and under artesian conditions beneath the till locally in the eastern part. The source of most of the ground water is direct infiltration of precipitation; however, some ground water enters the area as underflow from the south. About 7 inches of the 30 inches of average annual precipitation recharges the ground-water reservoir. The ground water generally moves toward Black Earth Creek where it is discharged. Some ground water moves out of the basin as underflow beneath the valley of Black Earth Creek, and some is discharged by evapotranspiration or is withdrawn by pumping from wells. Water levels in shallow nonartesian wells respond rapidly to precipitation. The effect of precipitation on water levels in artesian wells is slower and more subdued. Water levels are generally highest in spring and lowest in fall and winter. The flow of upper Black Earth Creek is derived mostly from ground-water discharge, except during short periods of and immediately after precipitation when most of the flow is derived from surface runoff. The runoff from upper Black Earth Creek basin decreased from an average of 8.72 inches per square mile of drainage area in 1955 to 5.55 inches in 1958; the decrease reflects the generally decreasing precipitation and declining water levels in the basin during that period. On July 10, 1958, the discharge from the basin was 0.367 cubic feet per second per square mile, and the greatest discharge was 0.84 cubic feet per second per square mile from the southwest subbasin. The ground water has an average temperature of about 50°F. It is a calcium magnesium bicarbonate type water and is very hard.

","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States (Water-Supply Paper 1669)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1669C","collaboration":"Prepared in cooperation with the Wisconsin Geological and Natural History Survey","usgsCitation":"Cline, D.R., and Busby, M., 1963, Hydrology of upper Black Earth Creek basin, Wisconsin, with a section on surface water: U.S. Geological Survey Water Supply Paper 1669, Report: iv, 27 p.; 5 Plates:18.00 x 15.65 inches or smaller, https://doi.org/10.3133/wsp1669C.","productDescription":"Report: iv, 27 p.; 5 Plates:18.00 x 15.65 inches or smaller","numberOfPages":"32","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":25944,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137643,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669c/report-thumb.jpg"},{"id":25940,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669c/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25939,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":422984,"rank":8,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24862.htm","linkFileType":{"id":5,"text":"html"}},{"id":25941,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669c/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25943,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669c/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25942,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669c/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","county":"Dane County","otherGeospatial":"Black Earth Creek","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -89.81494903564453,\n 43.04079076668198\n ],\n [\n -89.81494903564453,\n 43.21193220073775\n ],\n [\n -89.52999114990234,\n 43.21193220073775\n ],\n [\n -89.52999114990234,\n 43.04079076668198\n ],\n [\n -89.81494903564453,\n 43.04079076668198\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fc7d5","contributors":{"authors":[{"text":"Cline, Denzel R.","contributorId":87910,"corporation":false,"usgs":true,"family":"Cline","given":"Denzel","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143260,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Busby, Mark W.","contributorId":83099,"corporation":false,"usgs":true,"family":"Busby","given":"Mark W.","affiliations":[],"preferred":false,"id":143259,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}