{"pageNumber":"1608","pageRowStart":"40175","pageSize":"25","recordCount":40783,"records":[{"id":70009778,"text":"70009778 - 1969 - Geochemistry and origin of formation waters in the western Canada sedimentary basin-I. Stable isotopes of hydrogen and oxygen","interactions":[],"lastModifiedDate":"2020-11-29T20:38:46.584417","indexId":"70009778","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"Geochemistry and origin of formation waters in the western Canada sedimentary basin-I. Stable isotopes of hydrogen and oxygen","docAbstract":"<div id=\"abstracts\" class=\"Abstracts u-font-serif\"><div id=\"aep-abstract-id6\" class=\"abstract author\"><div id=\"aep-abstract-sec-id7\"><p>Stable isotopes of hydrogen and oxygen, together with chemical analyses, were determined for 20 surface waters, 8 shallow potable formation waters, and 79 formation waters from oil fields and gas fields. The observed isotope ratios can be explained by mixing of surface water and diagenetically modified sea water, accompanied by a process which enriches the heavy oxygen isotope. Mass balances for deuterium and total dissolved solids in the western Canada sedimentary basin demonstrate that the present distribution of deuterium in formation waters of the basin can be derived through mixing of the diagenetically modified sea water with not more than 2.9 times as much fresh water at the same latitude, and that the movement of fresh water through the basin has redistributed the dissolved solids of the modified sea water into the observed salinity variations. Statistical analysis of the isotope data indicates that although exchange of deuterium between water and hydrogen sulphide takes place within the basin, the effect is minimized because of an insignificant mass of hydrogen sulphide compared to the mass of formation water. Conversely, exchange of oxygen isotopes between water and carbonate minerals causes a major oxygen-18 enrichment of formation waters, depending on the relative masses of water and carbonate. Qualitative evidence confirms the isotopic fractionation of deuterium on passage of water through micropores in shales.</p></div></div></div>","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(69)90178-1","issn":"00167037","usgsCitation":"Hitchon, B., and Friedman, I., 1969, Geochemistry and origin of formation waters in the western Canada sedimentary basin-I. Stable isotopes of hydrogen and oxygen: Geochimica et Cosmochimica Acta, v. 33, no. 11, p. 1321-1349, https://doi.org/10.1016/0016-7037(69)90178-1.","productDescription":"29 p.","startPage":"1321","endPage":"1349","numberOfPages":"29","costCenters":[],"links":[{"id":219571,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada","state":"Alberta","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -120.14648437499999,\n              60.02095215374802\n            ],\n            [\n              -120.05859375,\n              53.74871079689897\n            ],\n            [\n              -118.037109375,\n              52.10650519075632\n            ],\n            [\n              -114.873046875,\n              49.95121990866204\n            ],\n            [\n              -114.521484375,\n              49.095452162534826\n            ],\n            [\n              -109.951171875,\n              49.03786794532644\n            ],\n            [\n              -109.951171875,\n              59.977005492196\n            ],\n            [\n              -120.14648437499999,\n              60.02095215374802\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"33","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a16d9e4b0c8380cd552aa","contributors":{"authors":[{"text":"Hitchon, B.","contributorId":40343,"corporation":false,"usgs":true,"family":"Hitchon","given":"B.","affiliations":[],"preferred":false,"id":357115,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Friedman, I.","contributorId":95596,"corporation":false,"usgs":true,"family":"Friedman","given":"I.","email":"","affiliations":[],"preferred":false,"id":357116,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70045464,"text":"70045464 - 1969 - Hydrology of the San Luis Valley, south-central Colorado","interactions":[],"lastModifiedDate":"2013-05-23T11:41:05","indexId":"70045464","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":375,"text":"Open-File Report","active":false,"publicationSubtype":{"id":6}},"title":"Hydrology of the San Luis Valley, south-central Colorado","docAbstract":"An investigation of the water resources of the Colorado part of the San Luis Valley was begun in 1966 by the U.S. Geological Survey, in cooperation with the Colorado Water Conservation Board. (See index map, fig. 1). The purpose of the investigation is to provide information for planning and implementing improved water-development and management practices. The major water problems in the San Luis Valley include (1) waterlogging, (2) waste of water by nonbeneficial evapotranspiration, (3) deterioration of ground-water chemical quality, and (4) failure of Colorado to deliver water to New Mexico and Texas in accordance with the Rio Grande Compact. This report describes the hydrologic environment, extent of water-resource development, and some of the problems related to that development. Information presented is based on data collected from 1966 to 1968 and on previous studies. Subsequent reports are planned as the investigation progresses. The San Luis Valley extends about 100 miles from Poncha Pass near the northeast corner of Saguache County, Colo., to a point about 16 miles south of the Colorado-New Mexico State line. The total area is 3,125 square miles, of which about 3,000 are in Colorado. The valley is nearly flat except for the San Luis Hills and a few other small areas. The Colorado part of the San Luis Valley, which is described in this report, has an average altitude of about 7,700 feet. Bounding the valley on the west are the San Juan Mountains and on the east the Sangre de Cristo Mountains. Most of the valley floor is bordered by alluvial fans deposited by streams originating in the mountains, the most extensive being the Rio Grande fan (see block diagram, fig. 2 in pocket). Most of the streamflow is derived from snowmelt from 4,700 square miles of watershed in the surrounding mountains. The northern half of the San Luis Valley is internally drained and is referred to as the closed basin. The lowest part of this area is known locally as the \"sump.\" The remainder of the valley is drained by the Rio Grande and its tributaries. The climate of the San Luis Valley is arid, and a successful agricultural economy would not be possible without irrigation. It is characterized by cold winters, moderate summers, and much sunshine. The average annual precipitation on the valley floor ranges from 7 to 10 inches. More than half the precipitation occurs from July to September. Moisture deficiency in the valley is shown by the graph comparing pan evaporation and precipitation {fig. 3}. For the years 1961-67 average pan evaporation for the period April through September was 52.25 inches, but average precipitation for the period was only 5.02 inches. Average annual precipitation was 7.8 inches. Owing to the short growing season (90-120 days), crops a.re restricted mainly to barley, oats, potatoes, and other vegetables.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Denver, CO","doi":"10.3133/70045464","collaboration":"Prepared in cooperation with the Colorado Water Conservation Board","usgsCitation":"Emery, P.A., Boettcher, A.J., Snipes, R., and Mcintyre, H., 1969, Hydrology of the San Luis Valley, south-central Colorado: Open-File Report, ii, 22 p.; 3 Plates: 23.79 x 27.78 inches or smaller, https://doi.org/10.3133/70045464.","productDescription":"ii, 22 p.; 3 Plates: 23.79 x 27.78 inches or smaller","numberOfPages":"26","additionalOnlineFiles":"Y","temporalStart":"1966-01-01","temporalEnd":"1968-12-31","costCenters":[{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true}],"links":[{"id":271022,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70045464/report-thumb.jpg"},{"id":272738,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70045464/report.pdf"},{"id":272739,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70045464/plate-2.pdf"},{"id":272740,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70045464/plate-4.pdf"},{"id":272741,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70045464/plate-7.pdf"}],"country":"United States","state":"Colorado","county":"Alamosa;Conejos;Costilla;Custer;Huerfano;Rio Grande;Saguache","otherGeospatial":"San Luis Valley","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -105.25,37.0 ], [ -105.25,38.5 ], [ -106.75,38.5 ], [ -106.75,37.0 ], [ -105.25,37.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"516fc466e4b05024ef3cd408","contributors":{"authors":[{"text":"Emery, P. A.","contributorId":49392,"corporation":false,"usgs":true,"family":"Emery","given":"P.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":477543,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Boettcher, A. J.","contributorId":25965,"corporation":false,"usgs":true,"family":"Boettcher","given":"A.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":477541,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Snipes, R.J.","contributorId":16813,"corporation":false,"usgs":true,"family":"Snipes","given":"R.J.","affiliations":[],"preferred":false,"id":477540,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mcintyre, H.J. Jr.","contributorId":34027,"corporation":false,"usgs":true,"family":"Mcintyre","given":"H.J.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":477542,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":70011514,"text":"70011514 - 1969 - Old Faithful: A physical model","interactions":[],"lastModifiedDate":"2026-02-06T14:25:27.07659","indexId":"70011514","displayToPublicDate":"1968-05-31T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Old Faithful: A physical model","docAbstract":"<p><span>No abstract available.&nbsp;</span></p>","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.160.3831.989","issn":"00368075","usgsCitation":"Fournier, R., 1969, Old Faithful: A physical model: Science, v. 163, no. 3864, p. 304-305, https://doi.org/10.1126/science.160.3831.989.","productDescription":"2 p.","startPage":"304","endPage":"305","costCenters":[],"links":[{"id":221373,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wyoming","otherGeospatial":"Old Faithful, Yellowstone National Park","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -111.05293341017678,\n              44.994541052877565\n            ],\n            [\n              -111.05293341017678,\n              44.23010093392659\n            ],\n            [\n              -110.03726656441582,\n              44.23010093392659\n            ],\n            [\n              -110.03726656441582,\n              44.994541052877565\n            ],\n            [\n              -111.05293341017678,\n              44.994541052877565\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"163","issue":"3864","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a6d56e4b0c8380cd750a1","contributors":{"authors":[{"text":"Fournier, R.O.","contributorId":73584,"corporation":false,"usgs":true,"family":"Fournier","given":"R.O.","email":"","affiliations":[],"preferred":false,"id":361299,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70159222,"text":"70159222 - 1968 - Geology and ground-water resources of Burlington County, New Jersey","interactions":[],"lastModifiedDate":"2015-11-12T13:58:35","indexId":"70159222","displayToPublicDate":"2010-02-02T05:15:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":126,"text":"New Jersey Division of Water Policy and Supply Special Report","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"26","title":"Geology and ground-water resources of Burlington County, New Jersey","docAbstract":"<p>Burlington County, which lies between Trenton, Atlantic City and Camden, has an area of 827 square miles. The county is in the Atlantic Coastal Plain physiographic province, has moderate temperatures and a dependable rainfall of 44 inches per year. The area is attracting new industries and additional population. Water usage is increasing with this economic growth; 26 mgd (million gallons per day) of ground water were used in 1960.</p>\n<p>The Raritan and Magothy Formations are the most prolific producers, but the Cohansey Sand and Kirkwood Formation have a great and, as yet, untapped potential. Small to moderately large supplies have been obtained from other aquifers. The maximum average potential recharge to the ground-water reservoirs is estimated to be about 790 mgd. Presently, most of it is rejected because the aquifers are essentially full. On this basis, it is believed that ground-water supplies in Burlington County are sufficient for the foreseeable future. However, well spacing must be planned to avoid local overdevelopment.&nbsp;</p>","language":"English","publisher":"State of New Jersey Department of Convservation and Economic Development, Division of Water Policy and Supply","publisherLocation":"Trenton, N.J.","collaboration":"Prepared by the U.S. Geological Survey in cooperation with the State of New Jersey","usgsCitation":"Rush, F.E., 1968, Geology and ground-water resources of Burlington County, New Jersey: New Jersey Division of Water Policy and Supply Special Report 26, Report: ix, 66 p.;12 Plates: 20.86 x 12.88 inches or smaller.","productDescription":"Report: ix, 66 p.;12 Plates: 20.86 x 12.88 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":310065,"rank":14,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70159222.jpg"},{"id":311234,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70159222/plate-10.pdf","text":"Plate 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,{"id":38821,"text":"pp544E - 1968 - Seismic seiches from the March 1964 Alaska earthquake","interactions":[],"lastModifiedDate":"2021-08-17T20:30:42.561793","indexId":"pp544E","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1968","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":"544","chapter":"E","title":"Seismic seiches from the March 1964 Alaska earthquake","docAbstract":"Seismic seiches caused by the Alaska earthquake of March 27, 1964, were recorded at more than 850 surface-water gaging stations in North America and at 4 in Australia. In the United States, including Alaska and Hawaii, 763 of 6,435 gages registered seiches. Nearly all the seismic seiches were recorded at teleseismic distance. This is the first time such far-distant effects have been reported from surface-water bodies in North America. The densest occurrence of seiches was in States bordering the Gulf of Mexico. The seiches were recorded on bodies of water having a wide range in depth, width, and rate of flow. In a region containing many bodies of water, seiche distribution is more dependent on geologic and seismic factors than on hydro-dynamic ones. The concept that seiches are caused by the horizontal acceleration of water by seismic surface waves has been extended in this paper to show that the distribution of seiches is related to the amplitude distribution of short-period seismic surface waves. These waves have their greatest horizontal acceleration when their periods range from 5 to 15 seconds. Similarly, the water bodies on which seiches were recorded have low-order modes whose periods of oscillation also range from 5 to 15 seconds. Several factors seem to control the distribution of seiches. The most important is variations of thickness of low-rigidity sediments. This factor caused the abundance of seiches in the Gulf Coast area and along the edge of sedimentary overlaps. Major tectonic features such as thrust faults, basins, arches, and domes seem to control seismic waves and thus affect the distribution of seiches. Lateral refraction of seismic surface waves due to variations in local phase-velocity values was responsible for increase in seiche density in certain areas. For example, the Rocky Mountains provided a wave guide along which seiches were more numerous than in areas to either side. In North America, neither direction nor distance from the epicenter had any apparent effect on the distribution of seiches. Where seismic surface waves propagated into an area with thicker sediment, the horizontal acceleration increased about in proportion to the increasing thickness of the sediment. In the Mississippi Embayment however, where the waves emerged from high rigidity crust into the sediment, the horizontal acceleration increased near the edge of the embayment but decreased in the central part and formed a shadow zone. Because both seiches and seismic intensity depend on the horizontal acceleration from surface waves, the distribution of seiches may be used to map the seismic intensity that can be expected from future local earthquakes.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"The Alaska earthquake, March 27, 1964: effects on the hydrologic regimen (Professional Paper 544)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, DC","doi":"10.3133/pp544E","usgsCitation":"McGarr, A., and Vorhis, R.C., 1968, Seismic seiches from the March 1964 Alaska earthquake: U.S. Geological Survey Professional Paper 544, Report: 43 p.; 1 Plate: 39.97 inches x 27.98 inches, https://doi.org/10.3133/pp544E.","productDescription":"Report: 43 p.; 1 Plate: 39.97 inches x 27.98 inches","additionalOnlineFiles":"Y","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":388056,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4595.htm"},{"id":65745,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0544e/pp544e_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":65744,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0544e/pp544e_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":121872,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0544e/report-thumb.jpg"},{"id":104508,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0544e/index.html","linkFileType":{"id":5,"text":"html"},"description":"4595"}],"country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -124.8,24.5 ], [ -124.8,49.383333 ], [ -66.95,49.383333 ], [ -66.95,24.5 ], [ -124.8,24.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a09e4b07f02db5fa889","contributors":{"authors":[{"text":"McGarr, Arthur","contributorId":102548,"corporation":false,"usgs":true,"family":"McGarr","given":"Arthur","affiliations":[],"preferred":false,"id":220498,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Vorhis, Robert C.","contributorId":52555,"corporation":false,"usgs":true,"family":"Vorhis","given":"Robert","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":220497,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":39665,"text":"pp605C - 1968 - Effect of increased pumping of ground water in the Fairfield-New Baltimore area, Ohio - a prediction by analog-model study","interactions":[],"lastModifiedDate":"2012-02-02T00:09:56","indexId":"pp605C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"605","chapter":"C","title":"Effect of increased pumping of ground water in the Fairfield-New Baltimore area, Ohio - a prediction by analog-model study","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Ground water in the lower Great Miami River Valley, Ohio","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"ENGLISH","doi":"10.3133/pp605C","usgsCitation":"Spieker, A.M., 1968, Effect of increased pumping of ground water in the Fairfield-New Baltimore area, Ohio - a prediction by analog-model study: U.S. Geological Survey Professional Paper 605, p. C1-C34, https://doi.org/10.3133/pp605C.","productDescription":"p. C1-C34","costCenters":[],"links":[{"id":119441,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0605c/report-thumb.jpg"},{"id":67386,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0605c/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db625626","contributors":{"authors":[{"text":"Spieker, A. M.","contributorId":22824,"corporation":false,"usgs":true,"family":"Spieker","given":"A.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":221940,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":32657,"text":"pp516E - 1968 - A geophysical study in Grand Teton National Park and vicinity, Teton County, Wyoming","interactions":[],"lastModifiedDate":"2025-05-21T17:47:12.819568","indexId":"pp516E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"516","chapter":"E","title":"A geophysical study in Grand Teton National Park and vicinity, Teton County, Wyoming","docAbstract":"<p>An integrated geophysical study - comprising gravity, seismic refraction, and aeromagnetic surveys - was made of a 4,600-km<sup>2</sup> area in Grand Teton National Park and vicinity, Wyoming, for the purpose of obtaining a better understanding of the structural relationships in the region. The Teton range is largely comprised of Precambrian crystalline rocks and layered metasedimentary gneiss, but it also includes granitic gneiss, hornblende-plagioclase gneiss, granodiorite, and pegmatite and diabase dikes. Elsewhere, the sedimentary section is thick. The presence of each system except Silurian provides a chronological history of most structures. Uplift of the Teton-Gros Ventre area began in the Late Cretaceous; most of the uplift occurred after middle Eocene time. Additional uplift of the Teton Range and downfaulting of Jackson Hole began in the late Pliocene and continues to the present. </p><p>Bouguer anomalies range from -185 mgal over Precambrian rocks of the Teton Range to -240 mgal over low-density Tertiary and Cretaceous sedimentary rocks of Jackson Hole. The Teton fault (at the west edge of Jackson Hole), as shown by steep gravity gradients and seismic-refraction data, trends north-northeast away from the front of the Teton Range in the area of Jackson Lake. The Teton fault either is shallowly inclined in the Jenny Lake area, or it consists of a series of fault steps in the fault zone; it is approximately vertical in the Arizona Creek area. </p><p>Seismic-refraction data can be fitted well by a three-layer gravity model with velocities of 2.45 km per sec for the Tertiary and Cretaceous rocks above the Cloverly Formation, 3.9 km per sec for the lower Mesozoic rocks, and 6.1 km per sec for the Paleozoic (limestone and dolomite) and Precambrian rocks. Gravity models computed along two seismic profiles are in good agreement (σ=± 2 mgal) if density contrasts with the assumed 2.67 g per cm<sup>3</sup> Paleozoic and Precambrian rocks are assumed to be -0.35 and -0.10 g per cm<sup>3</sup> for the 2.45 and 3.9 km per sec velocity layers, respectively. The Teton Range has a maximum vertical uplift of about 7 km, as inferred from the maximum depth to basement of about 5 km. </p><p>Aeromagnetic data show a 400γ positive anomaly in the Gros Ventre Range, which trends out of the surveyed area at the east edge. Exposed Precambrian rocks contain concentrations of magnetite and hematite. A prominent anomaly of about 100γ is associated with the Gros Ventre Range, and 100γ anomalies are associated with the layered gneiss of the Teton Range. On this basis the unmapped Precambrian rocks of the Gross Ventre Range are interpreted as layered gneiss. The sources of the magnetic anomalies, as indicated by depth determination, are at the surface of the Precambrian rocks. A model fitted to a profile across the Gros Ventre Range gives a depth to the Precambrian surface and a susceptibility of 0.0004 emu (electromagnetic units) for the source, which is consistent with modal analyses of the layered gneisses. A residual magnetic map shows that the granitic rocks and layered gneiss probably continue beneath the floor of Jackson Hole east of the Teton fault. The location of aeromagnetic anomalies is consistent with the interpretation that the Teton fault diverges from the front of the Teton Range.</p>","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Geophysical field investigations, 1964-67 (Professional Paper 516)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp516E","usgsCitation":"Behrendt, J.C., Tibbetts, B.L., Bonini, W.E., Lavin, P.M., Love, J.D., and Reed, J., 1968, A geophysical study in Grand Teton National Park and vicinity, Teton County, Wyoming: U.S. Geological Survey Professional Paper 516, Report: v, 23 p.; 3 Plates: 14.00 × 20.00 inches or smaller, https://doi.org/10.3133/pp516E.","productDescription":"Report: v, 23 p.; 3 Plates: 14.00 × 20.00 inches or smaller","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":125352,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0516e/report-thumb.jpg"},{"id":60549,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0516e/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":394917,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4545.htm"},{"id":60546,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0516e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60547,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0516e/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60548,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0516e/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wyoming","county":"Teton County","otherGeospatial":"Grand Teton National Park and vicinity","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -111.0223388671875,\n              43.09697190802465\n            ],\n            [\n              -110.2313232421875,\n              43.09697190802465\n            ],\n            [\n              -110.2313232421875,\n              44.15068115978094\n            ],\n            [\n              -111.0223388671875,\n              44.15068115978094\n            ],\n            [\n              -111.0223388671875,\n              43.09697190802465\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd4957e4b0b290850ef129","contributors":{"authors":[{"text":"Behrendt, John Charles jbehrendt@usgs.gov","contributorId":74747,"corporation":false,"usgs":true,"family":"Behrendt","given":"John","email":"jbehrendt@usgs.gov","middleInitial":"Charles","affiliations":[],"preferred":false,"id":208873,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tibbetts, Benton L.","contributorId":105169,"corporation":false,"usgs":true,"family":"Tibbetts","given":"Benton","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":208875,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bonini, William E.","contributorId":87417,"corporation":false,"usgs":true,"family":"Bonini","given":"William","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":208874,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Lavin, Peter M.","contributorId":42087,"corporation":false,"usgs":true,"family":"Lavin","given":"Peter","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":208871,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Love, J. D.","contributorId":64620,"corporation":false,"usgs":true,"family":"Love","given":"J.","middleInitial":"D.","affiliations":[],"preferred":false,"id":208872,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Reed, John C. jreed@usgs.gov","contributorId":1259,"corporation":false,"usgs":true,"family":"Reed","given":"John C.","email":"jreed@usgs.gov","affiliations":[],"preferred":true,"id":208870,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}}
,{"id":55863,"text":"ofr68201 - 1968 - Statistical properties of dune profiles","interactions":[{"subject":{"id":55863,"text":"ofr68201 - 1968 - Statistical properties of dune profiles","indexId":"ofr68201","publicationYear":"1968","noYear":false,"title":"Statistical properties of dune profiles"},"predicate":"SUPERSEDED_BY","object":{"id":38800,"text":"pp562F - 1971 - Statistical properties of dune profiles","indexId":"pp562F","publicationYear":"1971","noYear":false,"chapter":"F","title":"Statistical properties of dune profiles"},"id":1}],"supersededBy":{"id":38800,"text":"pp562F - 1971 - Statistical properties of dune profiles","indexId":"pp562F","publicationYear":"1971","noYear":false,"title":"Statistical properties of dune profiles"},"lastModifiedDate":"2025-06-30T16:19:29.423741","indexId":"ofr68201","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-201","title":"Statistical properties of dune profiles","docAbstract":"<p>Properties of sand waves formed by subcritical unidirectional water currents are investigated by statistical analyses of records of streambed profiles. Records of bed elevation y as a function of distance x along the channel, y = y(x), and time records at a fixed point of the channel, y = y(t), were collected in three laboratory flumes that were 8 inches, 2 ft and 8 ft wide and in a straight alluvial channel that was 55 ft wide. For all cases, the bed material was fine sand. The continuous analogue records were converted to discrete data points and were analyzed by digital computer.</p><p>The analyses show that both types of records, y(x) and y(t), can be approximately represented as stationary Gaussian processes. When the data are standardized and the length or distance are expressed as ratios of the mean duration between zero-crossings of y, the statistical properties of all the flume data are similar, with no distinguishing characteristics that can be attributed to size of flume or to whether the bed forms were ripples or dunes. The field data, however, reflect the influence of large alternate bars that were not present in the flumes.</p><p>The Gaussian assumption, together with the spectral properties of the records as expressed by a dimensionless parameter, 6, permit predicting the distributions of maximum and minimum values of y between successive zeros of y. These distributions represent the probability distributions of the depth of local scour and fill due to the formation and migration of sand waves, and the parameters that specify the distributions relate approximately to flow velocity and depth.</p><p>Observed values of the number of zero and h-level crossings, the mean duration between zero crossings, and the mean duration of upward excursions of the process y(t) above the fixed level h compared reasonably well with theoretical values for the Gaussian model. The distribution of the duration of upward excursions is the conditional probability distribution of the rest period of a particle, given that it is deposited on the downstream face of a ripple or dune at the level h. Observed distributions of these durations can be approximated by a gamma distribution with parameters that relate to h, where h is measured in units of standard deviation from the mean bed level. These distributions and other probability distributions that enter into stochastic models of sediment transport can be determined either from the theoretical model or empirically from the observed data. The results of the study ,-show that even though the bed elevation deviates somewhat from the postulated normal distribution, reasonable estimates of many properties of the bed profiles can be derived from fairly simple statistical models.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr68201","usgsCitation":"Nordin, C., 1968, Statistical properties of dune profiles: U.S. Geological Survey Open-File Report 68-201, xiv, 137 p., https://doi.org/10.3133/ofr68201.","productDescription":"xiv, 137 p.","costCenters":[],"links":[{"id":491571,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0201/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":184022,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0201/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dde4b07f02db5e1e3f","contributors":{"authors":[{"text":"Nordin, C.F. Jr.","contributorId":100852,"corporation":false,"usgs":true,"family":"Nordin","given":"C.F.","suffix":"Jr.","affiliations":[],"preferred":false,"id":254388,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":3952,"text":"cir592 - 1968 - Interpreting pan-concentrate analysis of stream sediments in geochemical exploration for gold","interactions":[],"lastModifiedDate":"2017-06-25T13:10:19","indexId":"cir592","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"592","title":"Interpreting pan-concentrate analysis of stream sediments in geochemical exploration for gold","docAbstract":"A study of methods of collecting and processing samples to determine whether or not gold is present in areas of moderate size was undertaken in the northwestern part of the San Juan Mountains, Colo. As part of this study, 57 samples of pan concentrates were taken from streams draining three types of areas: (1)'barren' areas, where gold mineralization might be geologically possible but no deposits are known, (2) slightly mineralized areas that contain only a few known veins and prospects and small mines, and (3) well-mineralized areas that contain numerous veins and some very productive mines. The concentrate samples were analyzed by the fire-assay-atomic-absorption method. Replicate analyses of large samples gave results consistent enough to permit placing considerable confidence in the results obtained for smaller samples on which only one analysis was made. For general field practice, it is necessary to pan only enough sand and gravel to yield about 15 grams of concentrate. The analytical r6sults are also quantitatively compatible with known geologic relations and indicate that a few samples from a stream are adequate to distinguish between 'barren' and mineralized areas and to determine the relative amount of gold in mineralized areas. In other areas of similar gold deposits, data of this type should help decide whether more intensive search for gold deposits is justified.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir592","usgsCitation":"Fischer, R.P., and Fisher, F.S., 1968, Interpreting pan-concentrate analysis of stream sediments in geochemical exploration for gold: U.S. Geological Survey Circular 592, iii, 9 p. :illus., map. ;26 cm., https://doi.org/10.3133/cir592.","productDescription":"iii, 9 p. :illus., map. ;26 cm.","costCenters":[],"links":[{"id":31039,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1968/0592/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124627,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1968/0592/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d9e4b07f02db5dfc29","contributors":{"authors":[{"text":"Fischer, Richard Philip","contributorId":94283,"corporation":false,"usgs":true,"family":"Fischer","given":"Richard","email":"","middleInitial":"Philip","affiliations":[],"preferred":false,"id":147887,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fisher, Frederick S.","contributorId":17979,"corporation":false,"usgs":true,"family":"Fisher","given":"Frederick","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":147886,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":1785,"text":"wsp1876 - 1968 - Geology and ground-water resources of the lower Bighorn Valley, Montana","interactions":[],"lastModifiedDate":"2012-02-02T00:05:23","indexId":"wsp1876","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1876","title":"Geology and ground-water resources of the lower Bighorn Valley, Montana","docAbstract":"The Bighorn River has incised a deep, broad valley in Cretaceous strata along its 65-mile lower reach below the mouth of Bighorn Canyon in south-central Montana. It ceased downcutting at six different levels 100-200 feet apart, widening its flood plain and alluviating each level with about 30 feet of sandy gravel. These deposits are the only economic source of ground water in large areas of the valley where the underlying bedrock consists of relatively impermeable shale to great depths. Ground water in the alluvium is hard and in the irrigated lowlands is highly mineralized at those places where drainage is slow and discharge by evapotranspiration is great. \r\n\r\nThree bedrock sandstone aquifers are present at moderate depths along three separate reaches of the valley. The sandstones yield soft, moderately to highly mineralized water that contains a high percent sodium. \r\n\r\nWells in alluvial gravel of the irrigated lowlands can yield 100 gallons per minute at many places because the alluvium is fairly permeable and is readily recharged by infiltration of applied irrigation water, canal seepage, and ground water moving into the lowlands from the alluvium of tributary coulees. Seepage from the Two Leggins Canal in the central area probably is large. \r\n\r\nAlluvial gravel deposits have been mantled by thick alluvial and colluvial deposits of silty clay or silt that thin riverward. These fine-grained deposits drain slowly and confine ground water in alluvial gravel under artesian pressure at many places in the irrigated lowlands of the central and southern areas. The piezometric surface is close to the land surface at many places in the central area, and capillary rise and evapotranspiration in waterlogged ground has produced agriculturally harmful alkali deposits. \r\n\r\nWaterlogging of presently irrigated land in the central area will become more widespread if irrigation is extended to higher terraces to the west unless drainage ditches are installed along the base of high-terrace alluvium to intercept increased seepage and spring discharge. Additional provisions also may be required to intercept water moving through the alluvium of coulees.","language":"ENGLISH","publisher":"Geological Survey; for sale by the Supt. of Docs.] U.S. Govt. Print. Off.,","doi":"10.3133/wsp1876","usgsCitation":"Hamilton, L.J., and Paulson, Q., 1968, Geology and ground-water resources of the lower Bighorn Valley, Montana: U.S. Geological Survey Water Supply Paper 1876, v, 39 p. :illus., maps (1 fold. col. in pocket) ;24 cm., https://doi.org/10.3133/wsp1876.","productDescription":"v, 39 p. :illus., maps (1 fold. col. in pocket) ;24 cm.","costCenters":[],"links":[{"id":138376,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1876/report-thumb.jpg"},{"id":26919,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1876/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26920,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1876/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6854f5","contributors":{"authors":[{"text":"Hamilton, Louis J.","contributorId":53768,"corporation":false,"usgs":true,"family":"Hamilton","given":"Louis","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":144152,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Paulson, Q.F.","contributorId":107259,"corporation":false,"usgs":true,"family":"Paulson","given":"Q.F.","email":"","affiliations":[],"preferred":false,"id":144153,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":1270,"text":"wsp1586H - 1968 - Water-discharge determinations for the tidal reach of the Willamette River from Ross Island Bridge to Mile 10.3, Portland, Oregon","interactions":[],"lastModifiedDate":"2017-02-03T13:32:20","indexId":"wsp1586H","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1586","chapter":"H","title":"Water-discharge determinations for the tidal reach of the Willamette River from Ross Island Bridge to Mile 10.3, Portland, Oregon","docAbstract":"Water-discharge, velocity, and slope variations for a 3.7-mile-Iong tidal reach of the Willamette River at Portland, Oreg., were defined from discharge measurements and river stage data collected between July 1962 and January 1965. Observed water discharge during tide-affected flows, during floods, and during backwater from the Columbia River and recorded stages at each end of the river reach were used to determine water discharge from two mathematical models. These models use a finite-difference method to solve the equations of moderately unsteady open-channel streamflow, and discharges are computed by an electronic digital computer. \n\nDischarges computed by using the mathematical models compare satisfactorily with observed discharges, except during the period of backwater from the annual flood of the Columbia River. The flow resistance coefficients used in the models vary with discharge; for one model, the coefficients for discharges above 30,000 cfs (cubic feet per second) are 12 and 24 percent less than the coefficient used for discharges below 30,000 cfs. \n\nDaily mean discharges were determined by use of one mathematical model for approximately two-thirds of the water year, October 1963 through September 1964. Agreement of computed with routed daily mean discharges is fair; above 30,000 cfs, average differences between the two discharges are about 10 percent, and below 30,000 cfs, computed daily discharges are consistently greater (by as much as 25 percent) than routed discharges. The other model was used to compute discharges for the unusually high flood flows of December 1964.","language":"ENGLISH","publisher":"U.S. Govt. Printing Off.,","doi":"10.3133/wsp1586H","usgsCitation":"Dempster, G., and Lutz, G., 1968, Water-discharge determinations for the tidal reach of the Willamette River from Ross Island Bridge to Mile 10.3, Portland, Oregon: U.S. Geological Survey Water Supply Paper 1586, iv, 32 p. :ill. ;23 cm., https://doi.org/10.3133/wsp1586H.","productDescription":"iv, 32 p. :ill. ;23 cm.","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":265376,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1586h/report.pdf"},{"id":137480,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1586h/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6494d5","contributors":{"authors":[{"text":"Dempster, G.R.","contributorId":6038,"corporation":false,"usgs":true,"family":"Dempster","given":"G.R.","affiliations":[],"preferred":false,"id":143473,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lutz, Gale A.","contributorId":32507,"corporation":false,"usgs":true,"family":"Lutz","given":"Gale A.","affiliations":[],"preferred":false,"id":143474,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":23395,"text":"ofr68140 - 1968 - A geologic and hydrologic reconnaissance of Lava Beds National Monument and vicinity, California","interactions":[],"lastModifiedDate":"2012-02-02T00:08:12","indexId":"ofr68140","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-140","title":"A geologic and hydrologic reconnaissance of Lava Beds National Monument and vicinity, California","docAbstract":"Lava Beds National Monument is on the Modoc Plateau in Modoc and Siskiyou Counties. The principal geologic units in the vicinity are volcanic rocks, which in places are highly permeable and poorly permeable lake sedimentary deposits, all probably post-Oligocene in age. Yields and specific capacities of wells in the unconfined water body within volcanic rocks and lake deposits range widely, but in general are low in the lake deposits and higher in the volcanic rocks. A confined water body occurring in volcanic rocks underlying the lake deposits yields large quantities of water to three wells in the study area. \r\n\r\nDissolved-solids content of ground water generally increases in proportion to the thickness of lake deposits penetrated and to proximity of the lake deposits. Water from wells drilled in the volcanic rocks several miles from the lake deposits and from wells penetrating the confined water body in volcanic rocks underlying the lake deposits contains small to moderate quantities of dissolved solids. \r\n\r\nGround-water supplies can be developed almost anywhere in the study area by drilling wells to depths below the water table. In addition, there is a reasonable possibility of developing wells in a confined water body underlying the water-table system.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey, Water Resources Division,","doi":"10.3133/ofr68140","issn":"0094-9140","usgsCitation":"Hotchkiss, W.R., 1968, A geologic and hydrologic reconnaissance of Lava Beds National Monument and vicinity, California: U.S. Geological Survey Open-File Report 68-140, ii, 56 p., [1] folded leaf of plates :ill., maps ;27 cm., https://doi.org/10.3133/ofr68140.","productDescription":"ii, 56 p., [1] folded leaf of plates :ill., maps ;27 cm.","costCenters":[],"links":[{"id":156226,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0140/report-thumb.jpg"},{"id":52695,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0140/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":52696,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0140/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6ae67f","contributors":{"authors":[{"text":"Hotchkiss, W. R.","contributorId":61820,"corporation":false,"usgs":true,"family":"Hotchkiss","given":"W.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":190036,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":949,"text":"wsp1860 - 1968 - Electrical analog analysis of ground-water depletion in central Arizona","interactions":[],"lastModifiedDate":"2022-02-15T20:58:25.416238","indexId":"wsp1860","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1860","title":"Electrical analog analysis of ground-water depletion in central Arizona","docAbstract":"The Salt River Valley and the lower Santa Cruz River basin are the two largest agricultural areas in Arizona. The extensive use of ground water for irrigation has resulted in the need for a thorough appraisal of the present and future ground-water resources. The ground-water reservoir provides 80 percent (3.2 million acre-feet) of the total annual water supply. The amount of water pumped greatly exceeds the rate at which the ground-water supply is being replenished and has resulted in water-level declines of as much as 20 feet per year in some places. The depletion problem is of economic importance because ground water will become more expensive as pumping lifts increase and well yields decrease. The use of electrical-analog modeling techniques has made it possible to predict future ground-water levels under conditions of continued withdrawal in excess of the rate of replenishment. The electrical system is a representation of the hydrologic system: resistors and capacitors represent transmissibility and storage coefficients. The analogy between the two systems is accepted when the data obtained from the model closely match the field data in this instance, measured water-level change since 1923. The prediction of future water-table conditions is accomplished by a simple extension of the pumping trends to determine the resultant effect on the regional water levels. \r\n\r\nThe results of this study indicate the probable depths to water in central Arizona in 1974 and 1984 if the aquifer characteristics are accurately modeled and if withdrawal of ground water continues at the same rate and under the tame areal distribution as existed between 1958 and 1964. The greatest depths to water in 1984 will be more than 700 feet near Stanfield and more than 650 feet in Deer Valley and northeast of Gilbert. South of Eloy and northwest of Litchfield Park, a static water level of more than 550 feet is predicted. The total water-level decline in the 20-year period 1964-84 at the deepest points of the major cones of depression will range from 150 to 300 feet, and the average decline in the entire central Arizona area will be about 100 feet.","language":"English","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1860","usgsCitation":"Anderson, T.W., 1968, Electrical analog analysis of ground-water depletion in central Arizona: U.S. Geological Survey Water Supply Paper 1860, Report: iii, 21 p.; 4 Plates: 44.69 × 26.00 inches or smaller, https://doi.org/10.3133/wsp1860.","productDescription":"Report: iii, 21 p.; 4 Plates: 44.69 × 26.00 inches or smaller","costCenters":[],"links":[{"id":396005,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25084.htm"},{"id":25451,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1860/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25450,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1860/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25454,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1860/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25453,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1860/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25452,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1860/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138057,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1860/report-thumb.jpg"}],"country":"United States","state":"Arizona","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -112.4835205078125,\n              32.59773394005744\n            ],\n            [\n              -111.3299560546875,\n              32.59773394005744\n            ],\n            [\n              -111.3299560546875,\n              33.660353121928814\n            ],\n            [\n              -112.4835205078125,\n              33.660353121928814\n            ],\n            [\n              -112.4835205078125,\n              32.59773394005744\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abbe4b07f02db672556","contributors":{"authors":[{"text":"Anderson, T. W.","contributorId":105686,"corporation":false,"usgs":true,"family":"Anderson","given":"T.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":142905,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":12535,"text":"ofr683 - 1968 - Geology of the Gore Canyon-Kremmling area, Grand County, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:06:41","indexId":"ofr683","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-3","title":"Geology of the Gore Canyon-Kremmling area, Grand County, Colorado","docAbstract":"The Gore Canyon-Kremmling area is in the southwestern portion of the Kremmling 15-minute quadrangle, Colorado. Precambrian rocks are biotite gneiss, the Boulder Creek Granodiorite, granophyre dikes, and quartz veins. The Boulder Creek intrudes the biotite gneiss, and both of these units are cut by north-northwest-trending granophyre dikes and quartz veins. Biotite gneiss contains structure elements of a northwest and a northeast fold system. Lineations and foliations in the Boulder Creek are generally concordant to the northeast fold system . of the gneiss. \r\n\r\nLate Paleozoic to Mesozoic and Mesozoic sedimentary formations, in ascending order and with their approximate thicknesses, are the State Bridge Formation, 15 feet; the Chinle and Chugwater Formations undivided, 0-95 feet; the Sundance Formation, 0?-100 feet; the Morrison Formation, 250 feet; the Dakota Sandstone, 225 feet; the Benton Shale, 340 feet; the Niobrara Formation, 600 feet; and the Pierre Shale. Quaternary deposits are terrace, landslide, and modern flood-plain deposits. \r\n\r\nLaramide rock deformation is related to the Park Range uplift and includes faulting and, in the sediments, some folding. Some of the faults, including the regional Gore fault, are Precambrian structures reactivated in Laramide time.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr683","usgsCitation":"Barclay, C.V., 1968, Geology of the Gore Canyon-Kremmling area, Grand County, Colorado: U.S. Geological Survey Open-File Report 68-3, 187 p. ill., maps (some col.) ;29 cm., https://doi.org/10.3133/ofr683.","productDescription":"187 p. ill., maps (some col.) ;29 cm.","costCenters":[],"links":[{"id":145875,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0003/report-thumb.jpg"},{"id":40791,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0003/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":40792,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0003/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c8f8","contributors":{"authors":[{"text":"Barclay, C.S. Venable","contributorId":89525,"corporation":false,"usgs":true,"family":"Barclay","given":"C.S.","email":"","middleInitial":"Venable","affiliations":[],"preferred":false,"id":166294,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":2316,"text":"wsp1757I - 1968 - Ground-water hydrology of the Chad Basin in Bornu and Dikwa Emirates, northeastern Nigeria, with special emphasis on the flow life of the artesian system","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1757I","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1757","chapter":"I","title":"Ground-water hydrology of the Chad Basin in Bornu and Dikwa Emirates, northeastern Nigeria, with special emphasis on the flow life of the artesian system","docAbstract":"Bornu and Dikwa Emirates lie in the Nigerian sector of the Chad Basin, a vast region of interior drainage encompassing about 600,000 square miles of north-central Africa. The report area includes about 25,000 square miles of the basin that lie in Nigeria. Most of the area is a featureless plain that slopes gently northeast and east from the uplands of central Nigeria towards Lake Chad. On its eastern side the lake has one surface outlet which overflows only during exceptionally high stages of the lake. This outlet spills into the channel of Bahr al Ghazal, which in turn drains into the Bod616 depression. Because the lake is shallow, the shoreline fluctuates markedly with high and low stages corresponding to the wet and dry seasons. The semiarid climate of Bornu and Dikwa Emirates is characterized by a long dry season and a short wet season that correspond to seasonal winds. Annual rainfall ranges from 15 inches in the northern part of the area to 32 inches in the southern. \r\n\r\nThe Chad Basin in Dikwa and Bornu Emirates is underlain by interbedded sand and clay, collectively termed the Chad Formation. These alluvial and lactustrine sediments were deposited in or near Lake Chad whet it occupied a much greater area during Pliocene and Pleistocene time. The Chad Formation has a very slight primary dip in the direction of Lake Chad and conforms to the gentle slope of land surface. The known thickness of the formation ranges from a few feet where it overlies bedrock on the periphery of the basin to at least 1,800 feet at Maiduguri; however, its total thickness probably exceeds 2,000 feet in the central part of the basin. \r\n\r\nThree water-bearing units termed upper, middle, and lower zones occur within the Chad Formation. The upper zone yields water to numerous dug wells throughout the rural areas and also is .the major source of the Maiduguri municipal water .supply. The middle zone yields water from flowing artesian boreholes that have heads ranging from a few feet to 70 feet above land surface throughout a 13,000 square-mile area of the basin in Nigeria. The lower zone also yields water from flowing boreholes ; however, its areal extent has not been proved beyond the environs of Maiduguri. \r\n\r\nThe present investigation is concerned primarily with the middle zone, which is the source of water for some 190 flowing boreholes used as little-watering points in the Nigerian sector of the Chad Basin. The thickness of loads of waterbearing sand in the middle zone ranges from less than 1 foot to 200 feet, and the artesian head ranges from land surface at Maiduguri to 70 feet above land surface at Lake Chad. The depth to the top of the middle zone in the area of flowing boreholes ranges from 500 to 1,250 feet below land surface. The waterbearing properties of the middle zone differ greatly from place to place. Also, the yields of individual flowing boreholes generally range from 50 to 20,000 imperial gallons per hour (gph). On the basis of water availability, the middle zone can be divided as follows : Areas of high-, moderate-, and low-yield artesian aquifer ; areas of low- and moderate-yield subartesian aquifer ; and an area where the yields from boreholes are insignificant or the aquifer is missing. Recommended maximum rates of long-term withdrawal from individual boreholes for the three artesian areas range from 100 to 5,000 gph with boreholes spaced 5 to 10 miles apart. By limiting flows to the recommended maximum rates, the boreholes should continue to flow for at least 30 years. The present average use per borehole (265 gph in 1965) is considerably less than the recommended maximum rates. \r\n\r\nRecharge to the upper zone occurs in significant but as yet unmeasured quantities, mostly in the vicinity of the major streams. Apparently, however, no significant amount of recharge reaches the middle zone from the Upper zone. Although the middle zone is, in effect, being 'mined' by existing flowing wells, the present (1965) rate of withdrawal i","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1757I","usgsCitation":"Miller, R.E., Johnston, R., Olowu, J., and Uzoma, J., 1968, Ground-water hydrology of the Chad Basin in Bornu and Dikwa Emirates, northeastern Nigeria, with special emphasis on the flow life of the artesian system: U.S. Geological Survey Water Supply Paper 1757, iv, 48 p., https://doi.org/10.3133/wsp1757I.","productDescription":"iv, 48 p.","costCenters":[],"links":[{"id":137856,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1757i/report-thumb.jpg"},{"id":28147,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757i/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28148,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757i/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28149,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757i/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28150,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757i/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28151,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757i/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28152,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757i/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28153,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757i/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28154,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757i/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28155,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757i/plate-9.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28156,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1757i/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668a99","contributors":{"authors":[{"text":"Miller, Raymond E.","contributorId":67861,"corporation":false,"usgs":true,"family":"Miller","given":"Raymond","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":145001,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnston, R.H.","contributorId":19536,"corporation":false,"usgs":true,"family":"Johnston","given":"R.H.","email":"","affiliations":[],"preferred":false,"id":144999,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Olowu, J.A.I.","contributorId":68709,"corporation":false,"usgs":true,"family":"Olowu","given":"J.A.I.","email":"","affiliations":[],"preferred":false,"id":145002,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Uzoma, J.U.","contributorId":24327,"corporation":false,"usgs":true,"family":"Uzoma","given":"J.U.","email":"","affiliations":[],"preferred":false,"id":145000,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":1050,"text":"wsp1858 - 1968 - Use of water by riparian vegetation, Cottonwood Wash, Arizona","interactions":[{"subject":{"id":52443,"text":"ofr6519 - 1965 - Use of water by reparian vegetation, Cottonwood Wash, Arizona - A summary","indexId":"ofr6519","publicationYear":"1965","noYear":false,"title":"Use of water by reparian vegetation, Cottonwood Wash, Arizona - A summary"},"predicate":"SUPERSEDED_BY","object":{"id":1050,"text":"wsp1858 - 1968 - Use of water by riparian vegetation, Cottonwood Wash, Arizona","indexId":"wsp1858","publicationYear":"1968","noYear":false,"title":"Use of water by riparian vegetation, Cottonwood Wash, Arizona"},"id":1}],"lastModifiedDate":"2021-10-21T16:44:19.164517","indexId":"wsp1858","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1858","title":"Use of water by riparian vegetation, Cottonwood Wash, Arizona","docAbstract":"The change in water use as a result of the modification of riparian vegetation was measured in Cottonwood Wash, Mohave County, Ariz. A 4.1-mile length of the stream channel was selected and divided into a 2.6-mile upper reach and a 1.5-mile lower reach. Measurements of streamflow, ground-water levels, vegetation, and meteorological phenomena in the area defined the use of water by riparian vegetation under natural hydrologic conditions. Subsequent defoliation and eradication of the vegetation in the lower reach permitted the determination of the change in water use as a result of the modification. The computed average loss of water from the lower reach before modification was 80 acre-feet per growing season, a quantity which represented about 18 percent of the average flow entering the reach in the same period. The average loss after modification of the vegetation was 42 acre-feet per growing season, a quantity which represented about 12 percent of the average flow entering the reach in the same period.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1858","usgsCitation":"Bowie, J.E., and Kam, W., 1968, Use of water by riparian vegetation, Cottonwood Wash, Arizona: U.S. Geological Survey Water Supply Paper 1858, Report: iv, 62 p.; 1 Plate: 26.50 x 22.0 inches, https://doi.org/10.3133/wsp1858.","productDescription":"Report: iv, 62 p.; 1 Plate: 26.50 x 22.0 inches","costCenters":[],"links":[{"id":390744,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25078.htm"},{"id":25716,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1858/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25715,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1858/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137941,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1858/report-thumb.jpg"}],"scale":"12000","country":"United States","state":"Arizona","county":"Mohave County","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -113.53333333,\n              35.15\n            ],\n            [\n              -113.45,\n              35.15\n            ],\n            [\n              -113.45,\n              35.2\n            ],\n            [\n              -113.53333333,\n              35.2\n            ],\n            [\n              -113.53333333,\n              35.15\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a17e4b07f02db604255","contributors":{"authors":[{"text":"Bowie, James E.","contributorId":29393,"corporation":false,"usgs":true,"family":"Bowie","given":"James","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":143092,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kam, William","contributorId":85159,"corporation":false,"usgs":true,"family":"Kam","given":"William","email":"","affiliations":[],"preferred":false,"id":143093,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":2627,"text":"wsp1820 - 1968 - Summary of floods in the United States during 1962","interactions":[],"lastModifiedDate":"2017-09-04T16:53:29","indexId":"wsp1820","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1820","title":"Summary of floods in the United States during 1962","docAbstract":"<p>This report describes the most outstanding floods in the United Spates during 1962. The most damaging floods during the year occurred in February in southern Idaho and northern Nevada and Utah, and during the latter part of February and the early part of March in Kentucky and in the Cumberland River basin in Tennessee.</p><p>The floods in Idaho and adjacent areas of Nevada and Utah resulted from a combination of prolonged low-intensity rainfall, moderate amounts of snow on low-altitude areas, a period of high temperatures, and a glaze of ice over deeply frozen ground. The floods affected some of the most valuable agricultural land in the region and some of the most heavily populated areas in Idaho. Damage in Idaho was estimated at more than \\$7 million.</p><p>The floods in Kentucky and Tennessee were caused by two storms; precipitation exceeded 7 inches at places during the second storm. Damage in Kentucky totaled about \\$7 million.</p><p>Recordbreaking snowmelt floods occurred in March and April in southeastern South Dakota and adjacent areas. Many peak discharges were much greater than those that can be expected to occur on an average of once in 25 years. Peak discharges on the Floyd River and the Big Sioux River were the greatest snowmelt floods since 1881. Damage in South Dakota was estimated at \\$4 million.</p><p>Heavy rains during May and intense rains in early June caused flooding in Minnesota on tributaries of the Red River of the North. Peak discharges exceeded previous maximums at some areas in the basins of the Buffalo, Clearwater, and Wild Rice Rivers. Damage from the floods of May and June in Minnesota was about \\$5 million.</p><p>The greatest flood since 1920 in Rapid City, S. Dak., caused at out $600,000 damage in July. The great runoff of 3,300 cubic feet per second, from a relatively small area downstream from Pactola Reservoir, resulted from rainfall having an intensity greater than that for a 100-year recurrence interval.</p><p>Floods caused almost \\$3 million damage in three river basins' in western Florida in September. The greatest damage was in Sarasota where from 3 to 7 feet of water flooded homes and stores. About 70,000 acres of farmland and woodland was inundated.</p><p>Unusual floods of September in southern Arizona flooded areas up to 10 miles wide. Damage, which totaled about \\$3 million, was almost entirely to farms, as the flood area is sparsely populated.</p><p>In addition to the floods just mentioned, 15 others of lesser magnitude are considered outstanding enough to be included in this annual summary.</p>","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1820","collaboration":"Prepared in cooperation with Federal, State, and local agencies","usgsCitation":"Rostvedt, J., 1968, Summary of floods in the United States during 1962: U.S. Geological Survey Water Supply Paper 1820, vii, 134 p., https://doi.org/10.3133/wsp1820.","productDescription":"vii, 134 p.","numberOfPages":"142","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":28944,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1820/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138161,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1820/report-thumb.jpg"}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b04e4b07f02db699283","contributors":{"authors":[{"text":"Rostvedt, J.O.","contributorId":24757,"corporation":false,"usgs":true,"family":"Rostvedt","given":"J.O.","email":"","affiliations":[],"preferred":false,"id":145525,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":1010,"text":"wsp1853 - 1968 - Flow pattern and related chemical quality of ground water in the \"500-foot\" sand in the Memphis area, Tennessee","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1853","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1853","title":"Flow pattern and related chemical quality of ground water in the \"500-foot\" sand in the Memphis area, Tennessee","docAbstract":"The '500-foot' sand is the major source of water supply for the Memphis area. Thick layers of impervious clay above and below the sand confine the water in the aquifer under artesian pressure and also protect the aquifer from contamination. Recharge from rainfall enters the '500-foot' sand in the outcrop, or intake area south and east of Memphis. Recharge from other aquifers enters the sand wherever the confining beds are breached or absent. Some of the recharge that enters the '500-foot' sand in eastern Arkansas moves down the gradients created by pumping in the Memphis area. All discharge from the '500-foot' sand in the Memphis area results from well pumping. \r\n\r\nSince 1886 continuous withdrawals at gradually increasing rates of pumping have lowered water levels and altered hydraulic gradients in the area. These withdrawals have resulted in changes in direction and velocity of movement of water through the '500-foot' sand. Water in the sand in the southeaster n part of the Memphis area normally moves from the (outcrop area east and south of Memphis northwestward toward points of withdrawal. In the northwestern part of the area, water moves southeastward toward points of withdrawal. A flow-net analysis of the aquifer shows that the rate of water movement through the '500-foot' sand in 1964, toward the major cones of depression in the Memphis area, was about 350 feet per year, or 1 mile in 15 years. A flow-net analysis projected for the year 1975 indicates the rate will increase by about 20 percent in the 12-year period 1964-75. \r\n\r\nWater in the '500-foot' sand in the Memphis area is generally a calcium magnesium sodium bicarbonate type. It is soft, low in dissolved solids, high in concentrations of iron and carbon dioxide, and slightly to moderately corrosive. The softest and least mineralized water occurs in the southeastern part of the area, and the water becomes slightly harder and more mineralized as it moves downdip toward Memphis. The hardest and most mineralized water occurs in the northwestern part of the area. \r\n\r\nThe variations in chemical quality of water en route through the '500-foot' sand are virtually proportional to increases or decreases of the major chemical constituents. The variations are chiefly attributed to the mixing or blending of water from different directions or sources of recharge as wells are pumped. As water levels are lowered by continuous pumping in the future, increasing rates of recharge from the outcrop areas and from shallow aquifers will probably cause little, if any, change in chemical quality of the water. Certainly, the effects on quality are not expected to be detrimental. \r\n\r\nAlthough future changes in chemical quality of water in the '500-foot' sand in the Memphis area will probably be neither intense nor extensive, some changes can be anticipated as a result of man's activities associated with the continued growth and development of the area. Increased pumping at existing pumping centers will deepen existing cones of depression and thereby increase gradients. These increases will not necessarily cause a change in chemical quality unless the increases in pumping are unevenly distributed. If a major well field were developed in the '500-foot' sand in the southwestern part of the Memphis area, little change in quality would result because water would be caused to move toward the well field from both the northwest and southeast. This movement would not affect the blending of updip and downdip water at other well fields If water were impounded in the Wolf River a few miles upstream from Memphis, the impoundment could furnish recharge, at least temporarily, to the '500-foot' sand. It is improbable that any detrimental effects on the chemical quality of the water supply of Memphis would result, because the water in the impoundment would probably be softer ,and less mineralized than the water in the '500-foot' sand in that area.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1853","usgsCitation":"Bell, E.A., and Nyman, D.J., 1968, Flow pattern and related chemical quality of ground water in the \"500-foot\" sand in the Memphis area, Tennessee: U.S. Geological Survey Water Supply Paper 1853, iv, 27 p. :illus., maps (2 fold. col. in pocket) ;24 cm., https://doi.org/10.3133/wsp1853.","productDescription":"iv, 27 p. :illus., maps (2 fold. col. in pocket) ;24 cm.","costCenters":[],"links":[{"id":137979,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1853/report-thumb.jpg"},{"id":25605,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1853/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25606,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1853/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25607,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1853/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25608,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1853/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25609,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1853/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b25e4b07f02db6aee77","contributors":{"authors":[{"text":"Bell, Edwin Allen","contributorId":84340,"corporation":false,"usgs":true,"family":"Bell","given":"Edwin","email":"","middleInitial":"Allen","affiliations":[],"preferred":false,"id":143020,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nyman, Dale J.","contributorId":28584,"corporation":false,"usgs":true,"family":"Nyman","given":"Dale","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":143019,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":16658,"text":"ofr68334 - 1968 - Computer technique for tracing seismic rays in two-dimensional geological models","interactions":[{"subject":{"id":16658,"text":"ofr68334 - 1968 - Computer technique for tracing seismic rays in two-dimensional geological models","indexId":"ofr68334","publicationYear":"1968","noYear":false,"title":"Computer technique for tracing seismic rays in two-dimensional geological models"},"predicate":"SUPERSEDED_BY","object":{"id":70042621,"text":"70042621 - 1970 - A computer program to trace seismic ray distribution in complex two-dimensional geological models","indexId":"70042621","publicationYear":"1970","noYear":false,"title":"A computer program to trace seismic ray distribution in complex two-dimensional geological models"},"id":1}],"supersededBy":{"id":70042621,"text":"70042621 - 1970 - A computer program to trace seismic ray distribution in complex two-dimensional geological models","indexId":"70042621","publicationYear":"1970","noYear":false,"title":"A computer program to trace seismic ray distribution in complex two-dimensional geological models"},"lastModifiedDate":"2013-01-14T16:20:41","indexId":"ofr68334","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-334","title":"Computer technique for tracing seismic rays in two-dimensional geological models","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr68334","usgsCitation":"Yacoub, N.K., Scott, J.H., and McKeown, F.A., 1968, Computer technique for tracing seismic rays in two-dimensional geological models: U.S. Geological Survey Open-File Report 68-334, 65 p. ill., maps ;27 cm., https://doi.org/10.3133/ofr68334.","productDescription":"65 p. ill., maps ;27 cm.","costCenters":[],"links":[{"id":149544,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a651d","contributors":{"authors":[{"text":"Yacoub, Nazieh K.","contributorId":84389,"corporation":false,"usgs":true,"family":"Yacoub","given":"Nazieh","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":173233,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Scott, James Henry","contributorId":60211,"corporation":false,"usgs":true,"family":"Scott","given":"James","email":"","middleInitial":"Henry","affiliations":[],"preferred":false,"id":173232,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McKeown, F. A.","contributorId":106100,"corporation":false,"usgs":true,"family":"McKeown","given":"F.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":173234,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":2053,"text":"wsp1862 - 1968 - Geology and ground-water resources of the Deer Lodge Valley, Montana","interactions":[],"lastModifiedDate":"2012-02-02T00:05:22","indexId":"wsp1862","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1862","title":"Geology and ground-water resources of the Deer Lodge Valley, Montana","docAbstract":"The Deer Lodge Valley is a basin trending north-south within Powell, Deer Lodge, and Silver Bow Counties in west-central Montana, near the center of the Northern Rocky Mountains physiographic province. It trends northward between a group of relatively low, rounded mountains to the east and the higher, more rugged Flint Creek Range to the west. The Clark Fork and its tributaries drain the valley in a northerly direction. The climate is semiarid and is characterized by long cold winters and short cool summers. Agriculture and ore refining are the principal industries. Both are dependent on large amounts of water. The principal topographic features are a broad lowland, the Clark Fork flood plain, bordered by low fringing terraces that are in turn bordered by broad, high terraces, which slope gently upward to the mountains. The high terraces have been mostly obscured in the south end of the valley by erosion and by recent deposition of great coalescent fans radiating outward frown the mouths of various tributary canyons. \r\n\r\nThe mountains east of the Deer Lodge Valley are formed mostly of Cretaceous sedimentary and volcanic rocks and a great core of Upper Cretaceous to lower Tertiary granitic rocks; those west of the valley are formed of Precambrian to Cretaceous sedimentary rocks and a core of lower Tertiary granitic rocks. Field relationships, gravimetric data, and seismic data indicate that the valley is a deep graben, which formed in early Tertiary time after emplacement of the Boulder and Philipsburg batholiths. During the Tertiary Period the valley was partly filled to a maximum depth of more than 5,500 feet with erosional detritus that came from the surrounding mountains and was interbedded with minor amounts of volcanic ejecta. This material accumulated in a great variety of local environments. Consequently the resultant deposits are of extremely variable lithology in lateral and vertical sequence. The deposits grade from unconsolidated to well-cemented and from clay to boulder-sized aggregates. Throughout most of the area the strata dip gently towards the valley axis, but along the western margins of the valley they dip steeply into the mountains. \r\n\r\nIn late Pliocene or early Pleistocene the Tertiary strata were eroded to a nearly regular valley divide surface. In the western part of the valley the erosion surface was thinly mantled by glacial debris from the Flint Creek Range. Still later, probably during several interglacial intervals, the Clark Fork and its tributaries entrenched themselves in the Tertiary strata to an average depth of about 150 feet. The resultant erosional features were further modified by Wisconsin to Recent glaciofluvial deposition.\r\n\r\nThree east-west cross .sections and a corrected gravity map were drawn for the \r\nvalley. They indicate a maximum depth of fill of more than 5,500 feet in the \r\nsouthern part. Depths decrease to the north to approximately 2,300 feet near \r\nthe town of Deer Lodge. \r\n\r\nThe principal source of ground water in the Deer Lodge Valley is the upper few hundred feet of unconsolidated valley fill. Most of the wells tapping these deposits range in depth from a few feet to 250 feet. Water levels range from somewhat above land surface (in flowing wells) to about 150 feet below. Yields of the wells range from a few gallons per minute to 1,000 gallons per minute. Generally, wells having the highest yields are on the flood plain of the Clark Fork or the coalescent fans of Warm Springs and Mill Creeks. \r\n\r\nDischarge of ground water by seepage into streams, by evapotranspiration, and by pumping from wells causes a gradual lowering of the water table. Each spring and early summer, seepage of water from irrigation and streams and infiltration of water from snowmelt and precipitation replenish the ground-water reservoir. Seasonal fluctuation of the water table generally is less than 10 feet. The small yearly water table fluctuation indicates that recharge about balances discharge from th","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1862","usgsCitation":"Konizeski, R.L., McMurtrey, R.G., and Brietkrietz, A., 1968, Geology and ground-water resources of the Deer Lodge Valley, Montana: U.S. Geological Survey Water Supply Paper 1862, iv, 55 p. :illus., maps (2 fold. col. in pocket) ;24 cm., https://doi.org/10.3133/wsp1862.","productDescription":"iv, 55 p. :illus., maps (2 fold. col. in pocket) ;24 cm.","costCenters":[],"links":[{"id":138459,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1862/report-thumb.jpg"},{"id":27580,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1862/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27581,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1862/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27582,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1862/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685593","contributors":{"authors":[{"text":"Konizeski, Richard L.","contributorId":80248,"corporation":false,"usgs":true,"family":"Konizeski","given":"Richard","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":144602,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McMurtrey, R. G.","contributorId":36913,"corporation":false,"usgs":true,"family":"McMurtrey","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":144601,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brietkrietz, Alex","contributorId":34111,"corporation":false,"usgs":true,"family":"Brietkrietz","given":"Alex","email":"","affiliations":[],"preferred":false,"id":144600,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":2589,"text":"wsp1852 - 1968 - Water resources of King County, Washington","interactions":[],"lastModifiedDate":"2023-01-03T21:32:56.352719","indexId":"wsp1852","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1852","title":"Water resources of King County, Washington","docAbstract":"<p>Although the total supply of water in King County is large, water problems are inevitable because of the large and rapidly expanding population. The county contains a third of the 3 million people in Washington, most of the population being concentrated in the Seattle metropolitan area. </p><p>King County includes parts of two major physiographic features: the western area is part of the Puget Sound Lowland, and the eastern area is part of the Cascade Range. In these two areas, the terrain, weather, and natural resources (including water) contrast markedly. </p><p>Average annual precipitation in the county is about 80 inches, ranging from about 30 inches near Puget Sound to more than 150 inches in parts of the Cascades. Annual evapotranspiration is estimated to range from 15 to 24 inches. </p><p>Average annual runoff ranges from about 15 inches in the lowlands to more than 100 inches in the mountains. Most of the streamflow is in the major basins of the county--the Green-Duwamish, Lake Washington, and Snoqualmie basins. The largest of these is the Snoqualmie River basin (693 square miles), where average annual runoff during the period 1931-60 was about 79 inches. During the same period, annual runoff in the Lake Washington basin ( 607 square miles) averaged about 32 inches, and in the Green-Duwamish River basin (483 square miles), about 46 inches. Seasonal runoff is generally characterized by several high-flow periods in the winter, medium flows in the spring, and sustained low flows in the summer and fall. </p><p>When floods occur in the county they come almost exclusively between October and March. The threat of flood damage is greatest on the flood plaits of the larger rivers, but in the Green-Duwamish Valley the threat was greatly reduced with the completion of Howard A. Hanson Dam in 1962. In the Snoqualmie River basin, where no such dam exists, the potential damage from a major flood increases each year as additional land is developed in the Snoqualmie Valley. </p><p>Only moderate amounts of sediment are transported by most streams in the county, except during short periods of heavy rain in the winter. The temperature and chemical quality of surface waters are well suited to the requirements of fisheries and for municipal, industrial, and domestic supplies. Little treatment is needed for most uses of surface water, except where the water is subject to pollution. </p><p>Most recoverable ground water in the county occurs in the Puget Sound Lowland, where great volumes of unconsolidated sedimentary deposits were left by the continental glaciers of the Pleistocene Epoch. Bedrock, most of which is in the Cascade Range, contains very little ground water. Numerous springs, largely undeveloped, occur in several parts of the county. </p><p>Most of the ground water is of good to excellent quality except for excessive iron, which in some places may require treatment of the water before it is suitable for domestic or industrial use. </p><p>Excluding water used for hydroelectric-power, recreation, and fisheries, more than 80 percent of the water used in the county is provided by municipal-supply systems. Each of the major river basins includes municipal watersheds that provide large supplies of excellent water. By the 1980's, more than 90 percent of the county's population will probably be served by the Seattle municipal supply. With full development, Seattle's water system would have a capacity sufficient to supply more than 2 million people with 300 gallons per person per day. Most industrial and commercial establishments in the county obtain water from public supply systems. </p><p>The most serious water problem in the county at present (1965) is the threat of pollution in the densely populated areas. The immediate threat in the Seattle area is being reduced by the sewage-treatment program of the Municipality of Metropolitan Seattle, which will eliminate the discharge of waste into Lake Washington. Expected increases in population and industry will introduce new problems that will require additional planning to assure adequate water quality for fisheries, recreation, and other uses.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1852","usgsCitation":"Richardson, D., Bingham, J., Madison, R.J., and Williams, R., 1968, Water resources of King County, Washington: U.S. Geological Survey Water Supply Paper 1852, Report: v, 74 p.; 2 Plates: 20.00 x 22.80 inches and 20.00 x 19.24 inches, https://doi.org/10.3133/wsp1852.","productDescription":"Report: v, 74 p.; 2 Plates: 20.00 x 22.80 inches and 20.00 x 19.24 inches","costCenters":[],"links":[{"id":411295,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25068.htm","linkFileType":{"id":5,"text":"html"}},{"id":28866,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1852/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28865,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1852/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28864,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1852/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137575,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1852/report-thumb.jpg"}],"country":"United States","state":"Washington","county":"King 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Donald","contributorId":68288,"corporation":false,"usgs":true,"family":"Richardson","given":"Donald","email":"","affiliations":[],"preferred":false,"id":145452,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bingham, J.W.","contributorId":35295,"corporation":false,"usgs":true,"family":"Bingham","given":"J.W.","email":"","affiliations":[],"preferred":false,"id":145451,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Madison, R. J.","contributorId":84734,"corporation":false,"usgs":true,"family":"Madison","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":145453,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Williams, R.","contributorId":7686,"corporation":false,"usgs":true,"family":"Williams","given":"R.","affiliations":[],"preferred":false,"id":145450,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":1006,"text":"wsp1859C - 1968 - Analysis of water quality of the Mahoning River in Ohio","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1859C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1859","chapter":"C","title":"Analysis of water quality of the Mahoning River in Ohio","docAbstract":"The Mahoning River drains the densely populated and industrialized Warren-Youngstown area in northeastern Ohio. Significant chemical constituents and physical properties generally regarded as important in establishing water-quality standards for the Mahoning River are evaluated on the basis of hydrologic conditions and water use. Most of the interpretations and the appraisal of water-quality conditions are based on data collected from January 1963 to December 1965. Generally, streamflow during this period was lower than during a selected long-term reference period ; however, extremely low flows that occurred in the reference period did not occur in the 3-year study period. \r\n\r\nWater temperatures of the Mahoning River at Pricetown and Leavittsburg were not affected by thermal loading. Water temperatures at those stations ranged from the freezing point to 78?F during the 1963-65 period. Downstream from Leavittsburg, the use of large quantities of water for industrial cooling caused critical thermal loading during periods of low streamflow. Maximum water temperatures were 108?F and 104?F at Struthers and Lowellville, respectively. Water temperatures of the Mahoning River were lower during high water discharges and increased with higher steel-production indices. Flow augmentation and modifications in industrial processes have improved the water-temperature conditions in recent years. \r\n\r\nA combination of oxygen-consuming materials and warmed water from industrial and municipal wastes discharged into the lower reaches of the Mahoning River frequently depleted the dissolved-oxygen content. At Lowellville, the river water had a dissolved-oxygen content of 5 ppm (parts per million) or less for 67 percent of the time and 3 ppm or less for 16 percent of the time during the study period. The percentage of saturation of dissolved oxygen followed a similar trend. Both the dissolved-oxygen concentration and the percentage of saturation were noticeably lower downstream from Leavittsburg during the warm months when water temperatures were high and streamflow was low. The dissolved-oxygen content in the Mahoning River at Leavittsburg and Pricetown was almost always at acceptable levels. \r\n\r\nThe calculated dissolved-solids concentration of the Mahoning River ranged from 150 to 450 ppm at Leavittsburg and from 200 ppm to 650 ppm at Lowellville. Industrial use of the water caused an increase in the dissolved-solids concentration at Lowellville. During one steel-mill shutdown the average dissolved-solids concentration decreased from about 360 to about 280 ppm. \r\n\r\nChloride concentrations in the Mahoning River ranged from 42 ppm at Pricetown to 108 ppm at Struthers. The chloride load at 50-percent flow duration was 9 and 69 tons per day at Pricetown and Lowellville, respectively. The chloride content of the Mahoning River was well within acceptable levels. \r\n\r\nSulfate from wastes disposal and acid mine drainage made up the largest quantity of dissolved-solids load in the Mahoning River. The sulfate load at 50-percent flow duration increased from 38 tons per day at Pricetown to 300 tons per day at Lowellville. At Pricetown the sulfate load ranged from about 2 to 588 tons per day, while at Lowellville, downstream from the industrialized area, the range was from 106 to 2,420 tons per day. Comparison of sulfate loads during periods of steel production with periods of steel-mill shutdown indicated that during low flow about half the sulfate load at Lowellville was derived from steel-mill wastes when the production index was 100. \r\n\r\nThe alkalinity load of the Mahoning River at 50-percent flow duration increased from Pricetown (23 tons per day) to Lowellville (41 tons per day). During steel production the alkalinity of the water showed a marked decrease from Leavittsburg downstream to Lowellville. However, during steel-mill shutdowns the chemical composition of the river at Youngstown and Lowellville was similar to that at Leavittsburg. Acid mine drainag","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1859C","usgsCitation":"Bednar, G.A., Collier, C.R., and Cross, W.P., 1968, Analysis of water quality of the Mahoning River in Ohio: U.S. Geological Survey Water Supply Paper 1859, iv, 32 p. :ill. (some col.) ;24 cm., https://doi.org/10.3133/wsp1859C.","productDescription":"iv, 32 p. :ill. (some col.) ;24 cm.","costCenters":[],"links":[{"id":137950,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1859c/report-thumb.jpg"},{"id":25585,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1859c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25586,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1859c/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67ec8d","contributors":{"authors":[{"text":"Bednar, Gene A.","contributorId":81881,"corporation":false,"usgs":true,"family":"Bednar","given":"Gene","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":143010,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Collier, Charles R.","contributorId":57821,"corporation":false,"usgs":true,"family":"Collier","given":"Charles","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143009,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cross, William Perry","contributorId":21137,"corporation":false,"usgs":true,"family":"Cross","given":"William","email":"","middleInitial":"Perry","affiliations":[],"preferred":false,"id":143008,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":4683,"text":"twri08A1 - 1968 - Methods of measuring water levels in deep wells","interactions":[],"lastModifiedDate":"2012-02-02T00:05:31","indexId":"twri08A1","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":336,"text":"Techniques of Water-Resources Investigations","code":"TWRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"08-A1","title":"Methods of measuring water levels in deep wells","docAbstract":"Accurate measurement of water levels deeper than 1,000 feet in wells requires specialized equipment. Corrections for stretch and thermal expansion of measuring tapes must be considered, and other measuring devices must be calibrated periodically. Bore-hole deviation corrections also must be made. \r\nDevices for recording fluctuation of fluid level usually require mechanical modification for use at these depths. A multichannel recording device utilizing pressure transducers has been constructed. This device was originally designed to record aquifer response to nearby underground nuclear explosions but can also be used for recording data from multi-well pumping tests.\r\nBottom-hole recording devices designed for oil-field use have been utilized in a limited manner. These devices were generally found to lack the precision required, in ground-water investigations at the Nevada Test Site but may be applicable in other areas. A newly developed bottom-hole recording pressure gauge of improved accuracy has been used with satisfactory results.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/twri08A1","issn":"0565-596X","usgsCitation":"Garber, M.S., and Koopman, F.C., 1968, Methods of measuring water levels in deep wells: U.S. Geological Survey Techniques of Water-Resources Investigations 08-A1, iv, 23 p. :ill. ;26 cm. Reprinted in 1979., https://doi.org/10.3133/twri08A1.","productDescription":"iv, 23 p. :ill. ;26 cm. Reprinted in 1979.","costCenters":[],"links":[{"id":139159,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":244,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/twri/twri8a1/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a54e4b07f02db62bfd8","contributors":{"authors":[{"text":"Garber, M. S.","contributorId":6433,"corporation":false,"usgs":true,"family":"Garber","given":"M.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":149618,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Koopman, F. C.","contributorId":40586,"corporation":false,"usgs":true,"family":"Koopman","given":"F.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":149619,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":13513,"text":"ofr6897 - 1968 - The geologic classification of the meteorites","interactions":[],"lastModifiedDate":"2012-02-02T00:06:38","indexId":"ofr6897","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-97","title":"The geologic classification of the meteorites","docAbstract":"The meteorite classes of Prior and Mason are assigned to three proposed genetic groups on the basis of a combination of compositional, mineralogical, and elemental characteristics: l) the calcium-poor, volatile-rich carbonaceous chondrites and achondrites; 2) the calcium-poor, volatile-poor chondrites (enstatite, bronzite, hypersthene, and pigeonite), achondrites (enstatite, hypersthene, and pigeonite), stonyirons (pallasites, siderophyre), and irons; and, 3) the calcium-rich (basaltic) achondrites. Chondrites are correlated with calcium-poor achondrites and the silicate phase of the pallasitic meteorites on Fe contents of olivine and pyroxene; and with metal of the stony-irons and irons on the basis of trace elements (Ga and Ge). Transitions in structure and texture between the chondrites and achondrites are recognized. The Van Schmus-Wood chemical-petrologic classification of the chondrites has been modified and expanded to a mineralogic-petrologic classification of the chondrites and calcium-poor achondrites. \r\n\r\nChondrites apparently are the first rocks of the solar system. Paragenetic and textural relations in the Murray carbonaceous chondrite shed new light on the manner of accretion, and on the character of dispersed solid materials ('dust', and chondrules and metal) that existed in the solar system before accretion. \r\n\r\nTwo pre-accretionary mineral assemblages (components) are recognized in the carbonaceous chondrites and in the unequilibrated volatile-poor chondrites. They are: 1) a 'low temperature' water-, rare gas-, and carbon-bearing component; and, 2) a high temperature anhydrous silicate and metal component. Paragenetic relations indicate that component 2 materials predate chondrite formation. An accretionary assemblage (component 3) also is recognized in the carbonaceous chondrites and in the unequilibrated volatile-poor chondrites. Component 3 consists of very fine grains of olivine and pyroxene, which occur as pervasive disseminations, as small irregular aggregates of grains, and as large subround to round, finely granular accretional chondrules. \r\n\r\nEvidence in Murray indicates that component 3 silicates precipitated abruptly and at low pressures, possibly from a high temperature gas, in an environment that contained dispersed component 1 and 2 materials. All component 3 aggregates in Murray contain component 1 material, most commonly as flakes, and locally as tiny granules and larger spherules, some of which are hollow and some of which were broken prior to their mechanical incorporation in accretionary chondrules. Accretion may have occurred as ices associated with dispersed water-bearing component 1 materials temporarily melted during the precipitation of component 3 silicates, and then abruptly refroze to form an icy cementing material. Group 1 materials may be cometary, and group 2 materials may be asteroidal. Schematic models are proposed. \r\n\r\nEvidence is reviewed for the lunar origin of the pyroxeneplagioclase achondrites. On the basis of natural remanent magnetism, it is suggested that the very scarce diopside-olivine achondrites may be samples from Mars. A classification of the meteorite breccias, including the calcium-poor and calcium-rich mesosiderites, and irons that contain silicate fragments, is proposed. A fragmentation history of the meteorites is outlined on the basis of evidence in the polymict breccias, and from gas retention ages in stones and exposure ages in irons. Cometal impacts appear to have caused the initial fragmentation, stud possibly the perturbation of orbits, of two inferred asteroidal bodies (enstatite and bronzite), one and possibly both events occurring before 2000 m.y. ago. Several impacts apparently occurred on the inferred hypersthene body in the interval 1000 to 2000 m.y. ago. \r\n\r\nMajor breakups of the three bodies apparently occurred as the result of interasteroidal collisions at about 900 m.y. ago, and 600 to 700 m.y. ago. The breakups were followed by a number of fr","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6897","usgsCitation":"Elston, D.P., 1968, The geologic classification of the meteorites: U.S. Geological Survey Open-File Report 68-97, 271 p. ill. (some folded, some col.) ;30 cm., https://doi.org/10.3133/ofr6897.","productDescription":"271 p. ill. (some folded, some col.) ;30 cm.","costCenters":[],"links":[{"id":144632,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0097/report-thumb.jpg"},{"id":41989,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41990,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41991,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41992,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41993,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41994,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41995,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41996,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0097/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d9f5","contributors":{"authors":[{"text":"Elston, Donald Parker","contributorId":38150,"corporation":false,"usgs":true,"family":"Elston","given":"Donald","email":"","middleInitial":"Parker","affiliations":[],"preferred":false,"id":167926,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":14038,"text":"ofr68122 - 1968 - Geology of the Golden Zone mine area, Alaska","interactions":[],"lastModifiedDate":"2025-09-25T20:51:34.846063","indexId":"ofr68122","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-122","title":"Geology of the Golden Zone mine area, Alaska","docAbstract":"The Golden Zone mine area, in the upper Chulitna district, is underlain mainly by siltstone and tuff, volcanic conglomerate and breccia, and limestone. These rocks were invaded, probably in the Tertiary, by dikes and a small stock of porphyry. The ore deposits of the area are the Golden Zone breccia pipe, a nearly vertical body about in the center of the porphyry stock, and steeply dipping veins. Most veins strike north to northeast and are commonly only 1-5 feet thick, but locally are as much as 15 feet thick. Both pipe and vein deposits are gold deposits of low to moderate grade that are characterized by abundant arsenopyrite; some contain possibly economic amounts of copper, lead and zinc minerals. Of the deposits of the mine area, only the Golden Zone has been explored to any extent, and both it and some of. the veins deserve further exploration to determine their potential.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr68122","usgsCitation":"Hawley, C.C., Clark, A.L., and Benfer, J.A., 1968, Geology of the Golden Zone mine area, Alaska: U.S. Geological Survey Open-File Report 68-122, Report: 18 p.; 1 Plate: 25.60 × 20.18 inches, https://doi.org/10.3133/ofr68122.","productDescription":"Report: 18 p.; 1 Plate: 25.60 × 20.18 inches","costCenters":[],"links":[{"id":496185,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8250.htm","linkFileType":{"id":5,"text":"html"}},{"id":42692,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0122/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42691,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0122/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":147063,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0122/report-thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Golden Zone mine area","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -149.667,\n              63.225\n            ],\n            [\n              -149.667,\n              63.202\n            ],\n            [\n              -149.628,\n              63.202\n            ],\n            [\n              -149.628,\n              63.225\n            ],\n            [\n              -149.667,\n              63.225\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acfe4b07f02db6801bd","contributors":{"authors":[{"text":"Hawley, C. C.","contributorId":102070,"corporation":false,"usgs":true,"family":"Hawley","given":"C.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":168834,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Clark, Allen L.","contributorId":96258,"corporation":false,"usgs":true,"family":"Clark","given":"Allen","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":168833,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Benfer, J. Alan","contributorId":81500,"corporation":false,"usgs":true,"family":"Benfer","given":"J.","email":"","middleInitial":"Alan","affiliations":[],"preferred":false,"id":168832,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
]}