Coal in the Ferron Sandstone Member of the Mancos Shale of Cretaceous age has traditionally been mined by underground techniques in the Emery Coal Field in the southern end of Castle Valley in east-central Utah. However, approximately 99 million tons are recoverable by surface mining. Ground water in the Ferron is the sole source of supply for the town of Emery, but the aquifer is essentially untapped outside the Emery area.
The Ferron Sandstone Member crops out along the eastern edge of Castle Valley and generally dips 2 ? to 10 ? to the northwest. Sandstones in the Ferron are enclosed between relatively impermeable shale in the Tununk and Blue Gate Members of the Mancos Shale. Along the outcrop, the Ferron ranges in thickness from about 80 feet in the northern part of Castle Valley to 850 feet in the southern part. The Ferron also generally thickens in the subsurface downdip from the outcrop. Records from wells and test holes indicate that the full thickness of the Ferron is saturated with water in most areas downdip from the outcrop area.
Tests in the Emery area indicate that transmissivity of the Ferron sandstone aquifer ranges from about 200 to 700 feet squared per day where the Ferron is fully saturated. Aquifer transmissivity is greatest near the Paradise Valley-Joes Valley fault system where permeability has been increased by fracturing. Storage coefficient ranges from about 10 .6 to 10 -3 where the Ferron sandstone aquifer is confined and probably averages 5 x 10-2 where it is unconfined.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp2195","collaboration":"Prepared in cooperation with the United States Bureau of Land Management","usgsCitation":"Lines, G.C., Morrissey, D.J., Ryer, T.A., and Fuller, R.H., 1983, Hydrology of the Ferron Sandstone aquifer and effects of proposed surface-coal mining in Castle Valley, Utah, with a section on stratigraphy and a section on leaching of overburden: U.S. Geological Survey Water Supply Paper 2195, Report: vi, 40 p.; 3 Plates: 17.00 x 27.20 inches, https://doi.org/10.3133/wsp2195.","productDescription":"Report: vi, 40 p.; 3 Plates: 17.00 x 27.20 inches","numberOfPages":"46","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":30174,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2195/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing location of selected wells, springs, and test holes in and near Castle Valley, Utah, where ground-water information is available, 1980"},{"id":30175,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2195/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing the thickness of the Ferron sandstone member of the Mancos shale in Castle Valley, Utah"},{"id":423046,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25538.htm","linkFileType":{"id":5,"text":"html"}},{"id":138109,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2195/report-thumb.jpg"},{"id":30177,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2195/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":30176,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2195/plate-3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing the altitude of the top of the Ferron Sandstone member of the Mancos Shale in Castle Valley, Utah"}],"country":"United States","state":"Utah","otherGeospatial":"Castle Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -110.5,\n 39.75\n ],\n [\n -111.5,\n 39.75\n ],\n [\n -111.5,\n 38.5\n ],\n [\n -110.5,\n 38.5\n ],\n [\n -110.5,\n 39.75\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa7e4b07f02db667150","contributors":{"authors":[{"text":"Lines, Gregory C.","contributorId":50502,"corporation":false,"usgs":true,"family":"Lines","given":"Gregory","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":146406,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Morrissey, Daniel J.","contributorId":89875,"corporation":false,"usgs":true,"family":"Morrissey","given":"Daniel","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":146408,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ryer, Thomas A.","contributorId":100359,"corporation":false,"usgs":true,"family":"Ryer","given":"Thomas","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":146409,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Fuller, Richard H.","contributorId":66236,"corporation":false,"usgs":true,"family":"Fuller","given":"Richard","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":146407,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":28089,"text":"wri834053 - 1983 - Ground water in the northeast part of Twentynine Palms Marine Corps Base, Bagdad area, California","interactions":[],"lastModifiedDate":"2023-04-11T19:27:17.935961","indexId":"wri834053","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"83-4053","title":"Ground water in the northeast part of Twentynine Palms Marine Corps Base, Bagdad area, California","docAbstract":"The hydrologic characteristics of the Bagdad area, in the northeast part of Twentynine Palms Marine Corps Base, were investigated to determine the feasibility of obtaining a supply of ground water. Five test holes were drilled and three of these were completed with 6-inch casings. Ground water in the eastern part of the study area is high in dissolved solids; water from well 5N/11E-36H1 contains 252,000 milligrams per liter of dissolved solids, and well 4N/12E-7R1 contains 21,800 milligrams per liter of dissolved solids. The dissolved-solids concentration in water from the test wells on the west side of Ludlow fault is much lower; the dissolved solids in water from the three test wells ranges from 669 to 961 milligrams per liter. The recommended limits for chloride and fluoride were exceeded in water from test well 4N/10E-21K1, arsenic and fluoride in water from well 5N/9E-3B1, and chloride in water from test well 6N/9E-34F1. An estimated 640,000 acre-feet of water is stored in the alluvium west of the Ludlow fault, sufficient to provide for several small diameter wells for many years.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri834053","usgsCitation":"Koehler, J.H., 1983, Ground water in the northeast part of Twentynine Palms Marine Corps Base, Bagdad area, California: U.S. Geological Survey Water-Resources Investigations Report 83-4053, iv, 15 p., https://doi.org/10.3133/wri834053.","productDescription":"iv, 15 p.","costCenters":[],"links":[{"id":415591,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_35692.htm","linkFileType":{"id":5,"text":"html"}},{"id":56908,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1983/4053/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123623,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1983/4053/report-thumb.jpg"}],"country":"United States","state":"Calilfornia","otherGeospatial":"Twentynine Palms Marine Corps Base","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.74714785522053,\n 34.772980861725955\n ],\n [\n -116.74714785522053,\n 34.196058657436936\n ],\n [\n -115.70337642189573,\n 34.196058657436936\n ],\n [\n -115.70337642189573,\n 34.772980861725955\n ],\n [\n -116.74714785522053,\n 34.772980861725955\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66d7b2","contributors":{"authors":[{"text":"Koehler, J. H.","contributorId":108108,"corporation":false,"usgs":true,"family":"Koehler","given":"J.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":199198,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70011617,"text":"70011617 - 1983 - Structure, burial history, and petroleum potential of frontal thrust belt and adjacent foreland, southwest Montana","interactions":[],"lastModifiedDate":"2023-01-11T12:43:49.73678","indexId":"70011617","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":701,"text":"American Association of Petroleum Geologists Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Structure, burial history, and petroleum potential of frontal thrust belt and adjacent foreland, southwest Montana","docAbstract":"The frontal thrust belt in the Lima area of southwestern Montana consists of blind (nonsurfacing) thrusts of the Lima thrust system beneath the Lima anticline and the Tendoy thrust sheet to the west. The Tendoy sheet involves Mississippian through Cretaceous rocks of the southwest-plunging nose of the Mesozoic Blacktail-Snowcrest uplift that are thrust higher (northeast) onto the uplift. The front of the Tendoy sheet west of Lima locally has been warped by later compressive deformation which also involved synorogenic conglomerates of the structurally underlying Beaverhead Formation. To the north, recent extension faulting locally has dropped the front of the Tendoy sheet beneath Quaternary gravels. Rocks of the exposed Tendoy sheet have never been deeply buried, based on itrinite reflectance of <= 0.6%, conodont CAI (color alteration index) values that are uniformly 1, and on supporting organic geochemical data from Paleozoic rocks from the Tendoy thrust sheet. Directly above and west of the Tendoy sheet lie formerly more deeply buried rocks of the Medicine Lodge thrust system. Their greater burial depth is indicated by higher conodont CAI values. West-dipping post-Paleocene extension faults truncate much of the rear part of the Tendoy sheet and also separate the Medicine Lodge sheet from thrust sheets of the Beaverhead Range still farther west.
The Laramide Blacktail-Snowcrest uplift east of the frontal thrust belt is asymmetric. Its southeast, steeper limb is exposed along the Snowcrest Range. This limb extends southwestward in the complexly deformed Snowcrest structural terrane. Northwest-dipping thrusts on this limb involve basement rocks and probably merge with depth into a major sub-Snowcrest Range thrust. This major thrust borders and is chiefly responsible for the Blacktail-Snowcrest uplift and adjacent Ruby synclinorium to the southeast. Uniform conodont CAI values of 1 from both the southeast and northwest flanks of the Blacktail-Snowcrest uplift indicate that no thick cover of Upper Cretaceous or younger rocks extended over the flanks of the uplift. During Mississippian through Permian time, the area of later Laram de uplift underwent more rapid subsidence than the area of the Laramide Ruby syncline and the Centennial basin to the southeast. The inferred sub-Snowcrest Range thrust fault apparently represents a reactivated zone of basement weakness.
The intersection of thrust-belt and foreland trends, similar to the Uinta uplift area to the south, probably formed a number of structural traps for hydrocarbons which have not yet been tested. Potential petroleum source beds and reservoir rocks are both present in southwest Montana. However, remnants of Tertiary lava flows through much of the area, Tertiary to recent basin-and-range faulting, and supermaturity with respect to oil of Permian and older rocks in the western Centennial uplift area are additional factors which must be considered in any estimate of hydrocarbon potential of the Cordilleran overthrust belt and adjacent foreland in extreme southwestern Montana.
","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/03B5B6A0-16D1-11D7-8645000102C1865D","usgsCitation":"Perry, W.J., Wardlaw, B.R., Bostick, N.H., and Maughan, E.K., 1983, Structure, burial history, and petroleum potential of frontal thrust belt and adjacent foreland, southwest Montana: American Association of Petroleum Geologists Bulletin, v. 67, no. 5, p. 725-743, https://doi.org/10.1306/03B5B6A0-16D1-11D7-8645000102C1865D.","productDescription":"19 p.","startPage":"725","endPage":"743","numberOfPages":"19","costCenters":[],"links":[{"id":220984,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -112.5,\n 45\n ],\n [\n -112.5,\n 44.333\n ],\n [\n -112,\n 44.333\n ],\n [\n -112,\n 45\n ],\n [\n -112.5,\n 45\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"67","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b9c68e4b08c986b31d3ec","contributors":{"authors":[{"text":"Perry, W. J. Jr.","contributorId":64266,"corporation":false,"usgs":true,"family":"Perry","given":"W.","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":361554,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wardlaw, B. R.","contributorId":9269,"corporation":false,"usgs":true,"family":"Wardlaw","given":"B.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":361552,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bostick, N. H.","contributorId":67099,"corporation":false,"usgs":true,"family":"Bostick","given":"N.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":361555,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Maughan, E. K.","contributorId":25568,"corporation":false,"usgs":true,"family":"Maughan","given":"E.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":361553,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70012100,"text":"70012100 - 1983 - Eastern Devonian shales: Organic geochemical studies, past and present","interactions":[],"lastModifiedDate":"2012-03-12T17:19:06","indexId":"70012100","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Eastern Devonian shales: Organic geochemical studies, past and present","docAbstract":"The Eastern Devonian shales are represented by a sequence of sediments extending from New York state, south to the northern regions of Georgia and Alabama, and west into Ohio and to the Michigan and Ilinois Basins. Correlatives are known in Texas. The shale is regionally known by a number of names: Chattanooga, Dunkirk, Rhinestreet, Huron, Antrim, Ohio, Woodford, etc. These shales, other than those in Texas, have elicited much interest because they have been a source of unassociated natural gas. It is of particular interest, however, that most of these shales have no associated crude oil, in spite of the fact that they have some of the characteristics normally attributed to source beds. This paper addresses some of the organic geochemical aspects of the kerogen in these shales, in relation to their oil generating potential. Past organic geochemical studies on Eastern Devonian shales will be reviewed. Recent solid state 13C NMR studies on the nature of the organic matter in Eastern Devonian shales show that Eastern Devonian shales contain a larger fraction of aromatic carbon in their chemical composition. Thus, despite their high organic matter contents, their potential as a petroleum source rock is low, because the kerogen in these shales is of a \"coaly\" nature and hence more prone to producing natural gas.","largerWorkTitle":"Preprints Symposia","language":"English","issn":"05693799","usgsCitation":"Breger, I.A., Hatcher, P.G., Romankiw, L., and Miknis, F., 1983, Eastern Devonian shales: Organic geochemical studies, past and present, in Preprints Symposia, v. 28, no. 1.","startPage":"73","costCenters":[],"links":[{"id":221803,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"28","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0532e4b0c8380cd50cd0","contributors":{"authors":[{"text":"Breger, Irving A.","contributorId":65205,"corporation":false,"usgs":true,"family":"Breger","given":"Irving","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":362730,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hatcher, Patrick G.","contributorId":93625,"corporation":false,"usgs":true,"family":"Hatcher","given":"Patrick","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":362732,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Romankiw, L.A.","contributorId":85724,"corporation":false,"usgs":true,"family":"Romankiw","given":"L.A.","affiliations":[],"preferred":false,"id":362731,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Miknis, F.P.","contributorId":61564,"corporation":false,"usgs":true,"family":"Miknis","given":"F.P.","email":"","affiliations":[],"preferred":false,"id":362729,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70011600,"text":"70011600 - 1983 - The saltwater-freshwater interface in the Tertiary limestone aquifer, southeast Atlantic outer-continental shelf of the U.S.A.","interactions":[],"lastModifiedDate":"2025-04-11T16:49:26.1536","indexId":"70011600","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2342,"text":"Journal of Hydrology","active":true,"publicationSubtype":{"id":10}},"title":"The saltwater-freshwater interface in the Tertiary limestone aquifer, southeast Atlantic outer-continental shelf of the U.S.A.","docAbstract":"Hydrologic testing in an offshore oil well abandoned by Tenneco, Inc., determined the position of the saltwater-freshwater interface in Tertiary limestones underlying the Florida-Georgia continental shelf of the U.S.A. Previous drilling (JOIDES and U.S.G.S. AMCOR projects) established the existence of freshwater far offshore in this area. At the Tenneco well 55 mi. (∼88 km) east of Fernandina Beach, Florida, drill-stem tests made in the interval 1050–1070 ft. (320–326 m) below sea level in the Ocala Limestone recovered a sample with a chloride concentration of 7000 mg l−1. Formation water probably is slightly fresher. Pressure-head measurements indicated equivalent freshwater heads of 24–29 ft. (7.3–8.8 m) above sea level.
At the coast (Fernandina Beach), a relatively thin transition zone separating freshwater and saltwater occurs at a depth of 2100 ft. (640 m) below sea level. Fifty-five miles (∼88 km) offshore, at the Tenneco well, the base of freshwater is ∼1100 ft. (∼335 m) below sea level. The difference in approximate depth to the freshwater-saltwater transition at these two locations suggests an interface with a very slight landward slope. Assuming the Hubbert interface equation applies here (because the interface and therefore freshwater flow lines are nearly horizontal) the equilibrium depth to the interface should be 40 times the freshwater head above sea level. Using present-day freshwater heads along the coast in the Hubbert equation results in depths to the interface of less than the observed 2100 ft. (640 m). Substituting predevelopment heads in the equation yields depths greater than 2100 ft. (640 m). Thus the interface appears to be in a transient position between the position that would be compatible with present-day heads and the position that would be compatible with predevelopment heads. This implies that some movement of the interface from the predevelopment position has occurred during the past hundred years. The implied movement is incompatible with the hypothesis that the freshwater occurring far offshore in this area is trapped water remaining since the Pleistocene Epoch.
","language":"English","publisher":"Elsevier","doi":"10.1016/0022-1694(83)90251-2","issn":"00221694","usgsCitation":"Johnston, R., 1983, The saltwater-freshwater interface in the Tertiary limestone aquifer, southeast Atlantic outer-continental shelf of the U.S.A.: Journal of Hydrology, v. 61, no. 1-3, p. 239-249, https://doi.org/10.1016/0022-1694(83)90251-2.","productDescription":"11 p.","startPage":"239","endPage":"249","costCenters":[],"links":[{"id":220712,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Florida, Georgia","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -82.49895094186574,\n 30.906206797439737\n ],\n [\n -82.49895094186574,\n 29.80296540535703\n ],\n [\n -81.27672743461723,\n 29.80296540535703\n ],\n [\n -81.27672743461723,\n 30.906206797439737\n ],\n [\n -82.49895094186574,\n 30.906206797439737\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"61","issue":"1-3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bafb0e4b08c986b324998","contributors":{"authors":[{"text":"Johnston, R.H.","contributorId":19536,"corporation":false,"usgs":true,"family":"Johnston","given":"R.H.","email":"","affiliations":[],"preferred":false,"id":361516,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70011241,"text":"70011241 - 1983 - LITHOLOGIC MAPPING USING LANDSAT THEMATIC MAPPER DATA.","interactions":[],"lastModifiedDate":"2012-03-12T17:18:28","indexId":"70011241","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"LITHOLOGIC MAPPING USING LANDSAT THEMATIC MAPPER DATA.","docAbstract":"The paper is in abstract form. It discusses the Landsat-4 Thematic Mapper (TM), with its new near infrared bands centered at 1. 65 mu m and 2. 20 mu m and spatial resolution of 30 m, which has been used to distinguish rocks containing minerals having ferric-iron absorption bands in the visible and near-infrared and Al-O and CO//3 absorption bands in the 2. 1-2. 4 mu m regions. On the basis of characteristic absorption bands, digitally processed TM data were used to differentiate vegetated from non-vegetated areas, limonitic from nonlimonitic rocks, rocks containing minerals having absorption bands in the near-infrared region from rocks lacking the infrared absorption bands. Specific minerals were detected in both the humid eastern and semi-arid western United States. The absorption bands in the near-infrared region were used to detect kaolinite in open-pit exposures of a kaolin mining district near Macon, Georgia; calcium carbonate in the beach sands along the east coast of Florida; and kaolinite, alunite, jarosite, sericite and gypsum in natural exposures near Boulder City, Nevada.","conferenceTitle":"Proceedings - Pecora VIII Symposium: Satellite Land Remote Sensing Advancements for the Eighties.","conferenceLocation":"Sioux Falls, ND, USA","language":"English","publisher":"Augustana Coll","publisherLocation":"Sioux Falls, SD, USA","usgsCitation":"Podwysocki, M.H., Salisbury, J., Jones, O.D., and Mimms, D., 1983, LITHOLOGIC MAPPING USING LANDSAT THEMATIC MAPPER DATA., Proceedings - Pecora VIII Symposium: Satellite Land Remote Sensing Advancements for the Eighties., Sioux Falls, ND, USA.","startPage":"169","costCenters":[],"links":[{"id":221432,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a40e9e4b0c8380cd65136","contributors":{"authors":[{"text":"Podwysocki, M. H.","contributorId":70391,"corporation":false,"usgs":true,"family":"Podwysocki","given":"M.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":360644,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Salisbury, J.W.","contributorId":78352,"corporation":false,"usgs":true,"family":"Salisbury","given":"J.W.","email":"","affiliations":[],"preferred":false,"id":360645,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Jones, O. D.","contributorId":42700,"corporation":false,"usgs":true,"family":"Jones","given":"O.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":360643,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mimms, D.L.","contributorId":39522,"corporation":false,"usgs":true,"family":"Mimms","given":"D.L.","email":"","affiliations":[],"preferred":false,"id":360642,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70011383,"text":"70011383 - 1983 - The compositionally zoned eruption of 1912 in the Valley of Ten Thousand Smokes, Katmai National Park, Alaska","interactions":[],"lastModifiedDate":"2020-10-03T15:51:38.932929","indexId":"70011383","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2499,"text":"Journal of Volcanology and Geothermal Research","active":true,"publicationSubtype":{"id":10}},"title":"The compositionally zoned eruption of 1912 in the Valley of Ten Thousand Smokes, Katmai National Park, Alaska","docAbstract":"On June 6–8, 1912, ∼ 15 km3 of magma erupted from the Novarupta caldera at the head of the Valley of Ten Thousand Smokes (VTTS), producing ∼ 20 km3 of air-fall tephra and 11–15 km3 of ash-flow tuff within ∼ 60 hours. Three discrete periods of ash-fall at Kodiak correlate, respectively, with Plinian tephra layers designated A, CD, and FG by Curtis (1968) in the VTTS. The ash-flow sequence overlapped with but outlasted pumice fall A, terminating within 20 hours of the initial outbreak and prior to pumice fall C. Layers E and H consist mostly of vitric dust that settled during lulls, and Layer B is the feather edge of the ash flow. The fall units filled and obscured the caldera, but arcuate and radial fissures outline a 6-km2 depression. The Novarupta lava dome and its ejecta ring were emplaced later within the depression. At Mt. Katmai, 10 km east of the 1912 vent, a 600-m-deep caldera of similar area also collapsed at about this time, probably owing to hydraulic connection with the venting magma system; but all known ejecta are thought to have erupted at Novarupta. Mingling of three distinctive magmas during the eruption produced an abundance of banded pumice, and mechanical mixing of chilled ejecta resulted in deposits with a wide range of bulk composition. Pumice in the initial fall unit (A) is 100% rhyolite, but fall units atop the ash flow are > 98% dacite; black andesitic scoria is common only in the ash flows and in near-vent air-fall tephra. Pumice counts show the first half of the ash-flow deposit to be 91–98% rhyolite, but progressive increases of dacite and andesite eventually reduced the rhyolitic component to < 2%. The later, rhyolite-poor flows were hotter, less mobile, and widely produced partially welded tuff and vapor-indurated sillar.
The main ash flow was too deflated and sluggish 16 km from the vent to surmount a 25-m-high moraine in its path but was diverted around it and continued 5 km down-valley, engulfing and charring trees but not toppling all of them. Thin ash-flow veneers feather 30–40 m up the enclosing valley walls but only where a constriction in the central VTTS locally raised the flow level. In the upper VTTS, the “high sand mark” is not a veneer but a marginal bench formed in thick tuff by differential compaction. Flooding from adjacent glaciers led to phreatic explosions that ejected blocks of tuff more welded than any yet exposed. A cluster of phreatic craters dammed a lake atop the tuff, the breaching of which caused a flood that scoured the ash-flow surface in the central VTTS, transported 50-cm blocks of welded tuff > 20 km to the lowermost VTTS, and deposited 1–8 m of debris there.
Rhyolitic ejecta contain only 1–2% phenocrysts but andesite and dacite have 30–45%. Quartz is present and augite absent only in the rhyolite, but all ejecta contain plagioclase, orthopyroxene, titanomagnetite, ilmenite, apatite, and pyrrhotite; rare olivine occurs in the andesite. The zoning ranges of phenocrysts in the rhyolitic and intermediate ejecta do not overlap. New chemical data show the bulk SiO2 range to be: rhyolite 77 ± 0.6, dacite 66-64.5, and andesite 61.5–58.5%. The dacitic and andesitic ejecta contrast in color and density, and it is not certain whether they form a compositional continuum. Analyses reported by Fenner within the 66–76% SiO2 range were of banded pumice and lava and of bulk tephra that mechanically fractionated and mixed during flight. Despite the gap of 10% SiO2, Fe-Ti-oxide temperatures show a continuous range from rhyolite (805–850°C) through dacite (855–955°C) to andesite (955–990°C). Thermal continuity and isotopic and trace-element data suggest that all were derived from a single magmatic system, whether or not they were physically contiguous before eruption. If the rhyolitic liquid separated from dacitic magma, extraction was so efficient that no dacitic phenocrysts were retained and no bulk compositions in the range 66–76% SiO2 were created; if it were a partial melt of roof rocks atop an intermediate magma body, then such rocks had no O- or Sr-isotopic contrast with the andesite-dacite magma and clearly did not include the Jurassic arkosic or granitic basement. The presence of Holocene domes of pre-1912 glassy dacite adjacent to the 1912 vent suggest that the 7 km3 (or more) of high-silica rhyolitic magma (a composition rare in the Aleutian arc) was generated in less than a few thousand years. The 1912 vent is semi-encircled by several andesitic stratocones and is as close to Mageik, Trident, and Griggs volcanoes as it is to Mt. Katmai. The erupted magma probably occupied only shallow levels of an extensive system of injection and storage under a cluster of several stratovolcanoes. Although Quaternary basalt is not known to have erupted here, the intrusion of basaltic magma probably sustains the greater-VTTS magmatic system.
","language":"English","publisher":"Elsevier","doi":"10.1016/0377-0273(83)90003-3","issn":"03770273","usgsCitation":"Hildreth, W., 1983, The compositionally zoned eruption of 1912 in the Valley of Ten Thousand Smokes, Katmai National Park, Alaska: Journal of Volcanology and Geothermal Research, v. 18, no. 1-4, p. 1-56, https://doi.org/10.1016/0377-0273(83)90003-3.","productDescription":"56 p.","startPage":"1","endPage":"56","numberOfPages":"56","costCenters":[],"links":[{"id":221521,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Katmai National Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -156.368408203125,\n 57.66303463288711\n ],\n [\n -153.25927734375,\n 57.66303463288711\n ],\n [\n -153.25927734375,\n 59.33318942659219\n ],\n [\n -156.368408203125,\n 59.33318942659219\n ],\n [\n -156.368408203125,\n 57.66303463288711\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"18","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505baa4ee4b08c986b3227c4","contributors":{"authors":[{"text":"Hildreth, W. 0000-0002-7925-4251","orcid":"https://orcid.org/0000-0002-7925-4251","contributorId":100487,"corporation":false,"usgs":true,"family":"Hildreth","given":"W.","affiliations":[],"preferred":false,"id":360971,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012067,"text":"70012067 - 1983 - Isotopic evidence from the eastern Canadian shield for geochemical discontinuity in the proterozoic mantle","interactions":[],"lastModifiedDate":"2012-03-12T17:19:03","indexId":"70012067","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2840,"text":"Nature","active":true,"publicationSubtype":{"id":10}},"title":"Isotopic evidence from the eastern Canadian shield for geochemical discontinuity in the proterozoic mantle","docAbstract":"Most workers agree that Proterozoic anorthosite massifs represent the crystallization products of mantle-derived magmas1,2, although the composition of the parental melts is a major unsolved petrological problem 3. As mantle-derived rocks, the massifs can be used as geochemical probes of their late Precambrian upper mantle sources. We report here Nd and Sr isotopic compositions of anorthosites and related rocks from the Grenville and Nain Provinces of the eastern Canadian shield. Here 75% of the Earth's known anorthosite is found in a 1,600-km belt from the Adirondack Mountains of northern New York State to the eastern coast of Labrador4 (Fig. 1). The results indicate that the massifs were derived from at least two distinct mantle source regions which were established before 1,650 Myr ago, and were episodically involved in magmatism over ???500 Myr. One reservoir, below the Grenville Province, and probably below much of the eastern Superior Province, was isotopically similar to the depleted, modern-day mid-ocean ridge basalt (MORB) source. The other reservoir was chondritic to moderately enriched, and is most easily identified in the Nain Province, but may have occurred scattered throughout the Superior Province. ?? 1983 Nature Publishing Group.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Nature","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1038/306679a0","issn":"00280836","usgsCitation":"Ashwal, L., and Wooden, J.L., 1983, Isotopic evidence from the eastern Canadian shield for geochemical discontinuity in the proterozoic mantle: Nature, v. 306, no. 5944, p. 679-680, https://doi.org/10.1038/306679a0.","startPage":"679","endPage":"680","numberOfPages":"2","costCenters":[],"links":[{"id":222455,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":205241,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1038/306679a0"}],"volume":"306","issue":"5944","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a3fb1e4b0c8380cd64736","contributors":{"authors":[{"text":"Ashwal, L.D.","contributorId":82060,"corporation":false,"usgs":true,"family":"Ashwal","given":"L.D.","email":"","affiliations":[],"preferred":false,"id":362654,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wooden, J. L.","contributorId":58678,"corporation":false,"usgs":true,"family":"Wooden","given":"J.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":362653,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70011374,"text":"70011374 - 1983 - Thermal areas on Kilauea and Mauna Loa Volcanoes, Hawaii","interactions":[],"lastModifiedDate":"2017-04-26T16:11:41","indexId":"70011374","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2499,"text":"Journal of Volcanology and Geothermal Research","active":true,"publicationSubtype":{"id":10}},"title":"Thermal areas on Kilauea and Mauna Loa Volcanoes, Hawaii","docAbstract":"Active thermal areas are concentrated in three areas on Mauna Loa and three areas on Kilauea. High-temperature fumaroles (115-362°C) on Mauna Loa are restricted to the summit caldera, whereas high-temperature fumaroles on Kilauea are found in the upper East Rift Zone (Mauna Ulu summit fumaroles, 562°C), middle East Rift Zone (1977 eruptive fissure fumaroles), and in the summit caldera. Solfataric activity that has continued for several decades occurs along border faults of Kilauea caldera and at Sulphur Cone on the southwest rift zone of Mauna Loa. Solfataras that are only a few years old occur along recently active eruptive fissures in the summit caldera and along the rift zones of Kilauea. Steam vents and hot-air cracks also occur at the edges of cooling lava ponds, on the summits of lava shields, along faults and graben fractures, and in diffuse patches that may reflect shallow magmatic intrusions.
","language":"English","publisher":"Elsevier Science","doi":"10.1016/0377-0273(83)90028-8","issn":"03770273","usgsCitation":"Casadevall, T.J., and Hazlett, R.W., 1983, Thermal areas on Kilauea and Mauna Loa Volcanoes, Hawaii: Journal of Volcanology and Geothermal Research, v. 16, no. 3-4, p. 173-188, https://doi.org/10.1016/0377-0273(83)90028-8.","productDescription":"16 p.","startPage":"173","endPage":"188","costCenters":[],"links":[{"id":221361,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Hawaii","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -155.5,\n 19.25\n ],\n [\n -155,\n 19.25\n ],\n [\n -155,\n 19.5\n ],\n [\n -155.5,\n 19.5\n ],\n [\n -155.5,\n 19.25\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"16","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb211e4b08c986b32559a","contributors":{"authors":[{"text":"Casadevall, Thomas J. 0000-0002-9447-6864 tcasadevall@usgs.gov","orcid":"https://orcid.org/0000-0002-9447-6864","contributorId":2734,"corporation":false,"usgs":true,"family":"Casadevall","given":"Thomas","email":"tcasadevall@usgs.gov","middleInitial":"J.","affiliations":[{"id":35995,"text":"Geology, Geophysics, and Geochemistry Science Center","active":true,"usgs":true}],"preferred":true,"id":360953,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hazlett, Richard W.","contributorId":89201,"corporation":false,"usgs":true,"family":"Hazlett","given":"Richard","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":360952,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70011370,"text":"70011370 - 1983 - Eruptive history of Mount Mazama and Crater Lake Caldera, Cascade Range, U.S.A.","interactions":[],"lastModifiedDate":"2018-10-24T16:06:30","indexId":"70011370","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2499,"text":"Journal of Volcanology and Geothermal Research","active":true,"publicationSubtype":{"id":10}},"title":"Eruptive history of Mount Mazama and Crater Lake Caldera, Cascade Range, U.S.A.","docAbstract":"New investigations of the geology of Crater Lake National Park necessitate a reinterpretation of the eruptive history of Mount Mazama and of the formation of Crater Lake caldera. Mount Mazama consisted of a glaciated complex of overlapping shields and stratovolcanoes, each of which was probably active for a comparatively short interval. All the Mazama magmas apparently evolved within thermally and compositionally zoned crustal magma reservoirs, which reached their maximum volume and degree of differentiation in the climactic magma chamber ∼ 7000 yr B.P.
The history displayed in the caldera walls begins with construction of the andesitic Phantom Cone ∼ 400,000 yr B.P. Subsequently, at least 6 major centers erupted combinations of mafic andesite, andesite, or dacite before initiation of the Wisconsin Glaciation ∼ 75,000 yr B.P. Eruption of andesitic and dacitic lavas from 5 or more discrete centers, as well as an episode of dacitic pyroclastic activity, occurred until ∼ 50,000 yr B.P.; by that time, intermediate lava had been erupted at several short-lived vents. Concurrently, and probably during much of the Pleistocene, basaltic to mafic andesitic monogenetic vents built cinder cones and erupted local lava flows low on the flanks of Mount Mazama. Basaltic magma from one of these vents, Forgotten Crater, intercepted the margin of the zoned intermediate to silicic magmatic system and caused eruption of commingled andesitic and dacitic lava along a radial trend sometime between ∼ 22,000 and ∼ 30,000 yr B.P. Dacitic deposits between 22,000 and 50,000 yr old appear to record emplacement of domes high on the south slope. A line of silicic domes that may be between 22,000 and 30,000 yr old, northeast of and radial to the caldera, and a single dome on the north wall were probably fed by the same developing magma chamber as the dacitic lavas of the Forgotten Crater complex. The dacitic Palisade flow on the northeast wall is ∼ 25,000 yr old. These relatively silicic lavas commonly contain traces of hornblende and record early stages in the development of the climatic magma chamber.
Some 15,000 to 40,000 yr were apparently needed for development of the climactic magma chamber, which had begun to leak rhyodacitic magma by 7015 ± 45 yr B.P. Four rhyodacitic lava flows and associated tephras were emplaced from an arcuate array of vents north of the summit of Mount Mazama, during a period of ∼ 200 yr before the climactic eruption. The climactic eruption began 6845 ± 50 yr B.P. with voluminous airfall deposition from a high column, perhaps because ejection of ∼ 4−12 km3 of magma to form the lava flows and tephras depressurized the top of the system to the point where vesiculation at depth could sustain a Plinian column. Ejecta of this phase issued from a single vent north of the main Mazama edifice but within the area in which the caldera later formed. The Wineglass Welded Tuff of Williams (1942) is the proximal featheredge of thicker ash-flow deposits downslope to the north, northeast, and east of Mount Mazama and was deposited during the single-vent phase, after collapse of the high column, by ash flows that followed topographic depressions. Approximately 30 km3 of rhyodacitic magma were expelled before collapse of the roof of the magma chamber and inception of caldera formation ended the single-vent phase. Ash flows of the ensuing ring-vent phase erupted from multiple vents as the caldera collapsed. These ash flows surmounted virtually all topographic barriers, caused significant erosion, and produced voluminous deposits zoned from rhyodacite to mafic andesite. The entire climactic eruption and caldera formation were over before the youngest rhyodacitic lava flow had cooled completely, because all the climactic deposits are cut by fumaroles that originated within the underlying lava, and part of the flow oozed down the caldera wall.
A total of ∼ 51−59 km3 of magma was ejected in the precursory and climactic eruptions, and ∼ 40−52 km3 of Mount Mazama was lost by caldera formation. The spectacular compositional zonation shown by the climactic ejecta — rhyodacite followed by subordinate andesite and mafic andesite — reflects partial emptying of a zoned system, halted when the crystal-rich magma became too viscous for explosive fragmentation. This zonation was probably brought about by convective separation of low-density, evolved magma from underlying mafic magma. Confinement of postclimactic eruptive activity to the caldera attests to continuing existence of the Mazama magmatic system.
","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Journal of Volcanology and Geothermal Research","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1016/0377-0273(83)90004-5","issn":"03770273","usgsCitation":"Bacon, C., 1983, Eruptive history of Mount Mazama and Crater Lake Caldera, Cascade Range, U.S.A.: Journal of Volcanology and Geothermal Research, v. 18, no. 1-4, p. 57-115, https://doi.org/10.1016/0377-0273(83)90004-5.","productDescription":"59 p.","startPage":"57","endPage":"115","numberOfPages":"59","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":221285,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Mount Mazama, Crater Lake, Cascade Range","volume":"18","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0a57e4b0c8380cd522f6","contributors":{"authors":[{"text":"Bacon, C. R. 0000-0002-2165-5618","orcid":"https://orcid.org/0000-0002-2165-5618","contributorId":21522,"corporation":false,"usgs":true,"family":"Bacon","given":"C. R.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":false,"id":360936,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":44504,"text":"wri834045 - 1983 - Hydrogeologic and water-quality characteristics of the Prairie du Chien-Jordan aquifer, Southeast Minnesota","interactions":[],"lastModifiedDate":"2023-03-13T21:29:01.182397","indexId":"wri834045","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"83-4045","title":"Hydrogeologic and water-quality characteristics of the Prairie du Chien-Jordan aquifer, Southeast Minnesota","docAbstract":"Quality of water in the Prairie du Chien-Jordan aquifer is generally good, except for some localized contamination, Coal-tar derivatives that contaminate the aquifer in St. Louis Park, a western suburb in the Twin Cities Metropolitan Area, pose the most serious threat to water quality. High hardness and iron concentration limit suitability for municipal and industrial use in parts of extreme southeast Minnesota. Confining beds of bedrock and drift, however, protect most of the aquifer from surface pollutants.
The Prairie du Chien-Jordan aquifer is part of a sequence of sedimentary bedrock units in southeast Minnesota. The Jordan Sandstone is a white to yellow, fine- to coarse-grained sandstone. The Prairie du Chien Group comprises two dolomitic formations that are vuggy and fractured and interbedded with thin layers of shale. The aquifer formations were deposited in Paleozoic seas that occupied the Hollandale embayment. The aquifer dips toward the interior of the embayment where it is as deep as 750 feet below land surface and as thick as 500 feet.
Permeability is secondary in the Prairie du Chien Group because of solution cavities and fractures, and intergranular in the Jordan Sandstone. Water in the aquifer is confined except in the eastern part. Water generally flows to the north and east into the Minnesota and Mississippi Rivers. A ground-water divide separates part of the flow southward into Iowa. This aquifer supplies more water than any other bedrock one in the State.
Calcium magnesium bicarbonate type water is most common in the aquifer. Calcium and sulfate and, to a lesser degree sodium and magnesium, increase in concentration toward the southwestern part of the study area. Bicarbonate concentration, on the other hand, decreases toward the southwestern corner of the study area. Leakage from overlying Cretaceous deposits is the source of much of the sulfate and other minerals in the southwest.
This report is one of a series on the hydrogeology and water quality of the 14 principal aquifers in Minnesota prepared by the U. S. Geological Survey. The U. S. Environmental Protection Agency requested these studies because of the need for information to develop its Underground Injection Control Program.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri834045","collaboration":"Prepared in cooperation with the U.S. Environmental Protection Agency","usgsCitation":"Ruhl, J.F., Wolf, R.J., and Adolphson, D.G., 1983, Hydrogeologic and water-quality characteristics of the Prairie du Chien-Jordan aquifer, Southeast Minnesota: U.S. Geological Survey Water-Resources Investigations Report 83-4045, 2 Plates: 39.28 x 33.33 inches and 39.08 x 33.41 inches, https://doi.org/10.3133/wri834045.","productDescription":"2 Plates: 39.28 x 33.33 inches and 39.08 x 33.41 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":170272,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":414057,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_35685.htm","linkFileType":{"id":5,"text":"html"}},{"id":81880,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1983/4045/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":81879,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1983/4045/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Minnesota","otherGeospatial":"Prairie du Chien-Jordan aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -92.8619384765625,\n 45.71385093029221\n ],\n [\n -93.3837890625,\n 45.706179285330855\n ],\n [\n -93.8507080078125,\n 45.65628792636447\n ],\n [\n -94.207763671875,\n 45.583289756006316\n ],\n [\n -94.3011474609375,\n 45.46783598133375\n ],\n [\n -94.39453125,\n 45.232349197513116\n ],\n [\n -94.537353515625,\n 45.058001435398296\n ],\n [\n -94.7186279296875,\n 44.85197466334987\n ],\n [\n -94.89990234375,\n 44.629573191951046\n ],\n [\n -94.976806640625,\n 44.53959000445632\n ],\n [\n -95.3118896484375,\n 44.465151013519616\n ],\n [\n -95.4052734375,\n 44.296332880058706\n ],\n [\n -95.3118896484375,\n 44.12702800650004\n ],\n [\n -94.97131347656249,\n 43.91768033000405\n ],\n [\n -94.8944091796875,\n 43.504736854976954\n ],\n [\n -91.23046875,\n 43.504736854976954\n ],\n [\n -91.219482421875,\n 43.57243174740972\n ],\n [\n -91.2799072265625,\n 43.628123412124616\n ],\n [\n -91.241455078125,\n 43.75522505306928\n ],\n [\n -91.263427734375,\n 43.83452678223684\n ],\n [\n -91.3897705078125,\n 43.96909818325174\n ],\n [\n -91.461181640625,\n 44.008620115415354\n ],\n [\n -91.5655517578125,\n 44.03232064275084\n ],\n [\n -91.636962890625,\n 44.06390660801779\n ],\n [\n -91.73583984374999,\n 44.11125397357153\n ],\n [\n -91.8402099609375,\n 44.18614312298759\n ],\n [\n -91.8896484375,\n 44.24913396886894\n ],\n [\n -91.9500732421875,\n 44.32384807250689\n ],\n [\n -91.9720458984375,\n 44.35527821160296\n ],\n [\n -92.1148681640625,\n 44.41416430998939\n ],\n [\n -92.21923828124999,\n 44.44554600843547\n ],\n [\n -92.31262207031249,\n 44.49650533109348\n ],\n [\n -92.31262207031249,\n 44.53959000445632\n ],\n [\n -92.5048828125,\n 44.574817404670306\n ],\n [\n -92.57080078125,\n 44.59829048984011\n ],\n [\n -92.6641845703125,\n 44.65693173288727\n ],\n [\n -92.8070068359375,\n 44.750634493861064\n ],\n [\n -92.74658203125,\n 44.85586880735725\n ],\n [\n -92.7630615234375,\n 44.90646871709883\n ],\n [\n -92.74658203125,\n 44.94536144236941\n ],\n [\n -92.7850341796875,\n 45.03859654645257\n ],\n [\n -92.79602050781249,\n 45.06964120886863\n ],\n [\n -92.74108886718749,\n 45.11230010229608\n ],\n [\n -92.7630615234375,\n 45.178164812206376\n ],\n [\n -92.757568359375,\n 45.27488643704894\n ],\n [\n -92.691650390625,\n 45.36372498305678\n ],\n [\n -92.6641845703125,\n 45.398449976304086\n ],\n [\n -92.6531982421875,\n 45.463983441272745\n ],\n [\n -92.6751708984375,\n 45.48324350868221\n ],\n [\n -92.7191162109375,\n 45.533288879467456\n ],\n [\n -92.7630615234375,\n 45.56021795715051\n ],\n [\n -92.8179931640625,\n 45.56021795715051\n ],\n [\n -92.88940429687499,\n 45.57175504130605\n ],\n [\n -92.8729248046875,\n 45.6178796835697\n ],\n [\n -92.8619384765625,\n 45.71385093029221\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a50e4b07f02db628d15","contributors":{"authors":[{"text":"Ruhl, J. F.","contributorId":81866,"corporation":false,"usgs":true,"family":"Ruhl","given":"J.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":229896,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wolf, R. J.","contributorId":21518,"corporation":false,"usgs":true,"family":"Wolf","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":229895,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Adolphson, D. G.","contributorId":106081,"corporation":false,"usgs":true,"family":"Adolphson","given":"D.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":229897,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":46989,"text":"ofr821030 - 1983 - Geologic map of the Mitten Lake, Half Dome Crag, Hyde Creek, East Glacier Park, Big Rock, and Magee Range quadrangles, Pondera and Glacier Counties, Montana","interactions":[],"lastModifiedDate":"2023-08-25T18:26:40.347672","indexId":"ofr821030","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","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":"82-1030","title":"Geologic map of the Mitten Lake, Half Dome Crag, Hyde Creek, East Glacier Park, Big Rock, and Magee Range quadrangles, Pondera and Glacier Counties, Montana","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr821030","usgsCitation":"Mudge, M.R., Earhart, R., Perry, W.J., and Bohannon, R.G., 1983, Geologic map of the Mitten Lake, Half Dome Crag, Hyde Creek, East Glacier Park, Big Rock, and Magee Range quadrangles, Pondera and Glacier Counties, Montana: U.S. Geological Survey Open-File Report 82-1030, 1 Plate: 34.92 x 32.46 inches, https://doi.org/10.3133/ofr821030.","productDescription":"1 Plate: 34.92 x 32.46 inches","costCenters":[],"links":[{"id":108422,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13625.htm","linkFileType":{"id":5,"text":"html"},"description":"13625"},{"id":83892,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1982/1030/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":172698,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"Montana","county":"Glacier County, Pondera County","otherGeospatial":"Mitten Lake, Half Dome Crag, Hyde Creek, East Glacier Park, Big Rock, and Magee Ranch quadrangles","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -113.25,\n 48.5\n ],\n [\n -113.25,\n 48.25\n ],\n [\n -112.875,\n 48.25\n ],\n [\n -112.875,\n 48.5\n ],\n [\n -113.25,\n 48.5\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db696904","contributors":{"authors":[{"text":"Mudge, Melville Rhodes","contributorId":77119,"corporation":false,"usgs":true,"family":"Mudge","given":"Melville","email":"","middleInitial":"Rhodes","affiliations":[],"preferred":false,"id":234447,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Earhart, R.L.","contributorId":73175,"corporation":false,"usgs":true,"family":"Earhart","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":234446,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Perry, W. J. Jr.","contributorId":64266,"corporation":false,"usgs":true,"family":"Perry","given":"W.","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":234445,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bohannon, R. G.","contributorId":61808,"corporation":false,"usgs":true,"family":"Bohannon","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":234444,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70135757,"text":"70135757 - 1983 - Crustal structure beneath the southern Appalachians: Nonuniqueness of gravity modeling","interactions":[],"lastModifiedDate":"2017-08-24T12:56:52","indexId":"70135757","displayToPublicDate":"1982-12-27T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1796,"text":"Geology","active":true,"publicationSubtype":{"id":10}},"title":"Crustal structure beneath the southern Appalachians: Nonuniqueness of gravity modeling","docAbstract":"Gravity models computed for a profile across the long-wavelength paired negative-positive Bouguer anomalies of the southern Appalachian Mountains show that the large negative anomaly can be explained by a crustal root zone, whereas the steep gradient and positive anomaly east of the root may be explained equally well by three different geometries: a suture zone, a mantle upwarp, or a shallow body. Seismic data support the existence of a mountain root but are inadequate to resolve differences among the three possible geometries for the positive anomaly. The presence of outcropping mafic and ultramafic rocks in the southern Appalachians and the inferred tectonic history of the Appalachian orogen are most consistent with the suture-zone model. Crust similar to continental crust probably exists beneath the Coastal Plain and inner continental shelf where the gravity anomalies return to near-zero values.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0091-7613(1983)11<611:CSBTSA>2.0.CO;2","usgsCitation":"Hutchinson, D.R., Grow, J., and Klitgord, K.D., 1983, Crustal structure beneath the southern Appalachians: Nonuniqueness of gravity modeling: Geology, v. 11, no. 10, p. 611-615, https://doi.org/10.1130/0091-7613(1983)11<611:CSBTSA>2.0.CO;2.","productDescription":"5 p.","startPage":"611","endPage":"615","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":186,"text":"Coastal and Marine Geology Program","active":true,"usgs":true}],"links":[{"id":296724,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Appalachian Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -69.01611328125,\n 47.502358951968596\n ],\n [\n -66.6650390625,\n 45.336701909968106\n ],\n [\n -86.484375,\n 31.82156451492074\n ],\n [\n -88.2861328125,\n 33.65120829920497\n ],\n [\n -69.01611328125,\n 47.502358951968596\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"11","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"549165bfe4b0d0759afaad80","contributors":{"authors":[{"text":"Hutchinson, Deborah R. 0000-0002-2544-5466 dhutchinson@usgs.gov","orcid":"https://orcid.org/0000-0002-2544-5466","contributorId":521,"corporation":false,"usgs":true,"family":"Hutchinson","given":"Deborah","email":"dhutchinson@usgs.gov","middleInitial":"R.","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":536831,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Grow, John A.","contributorId":51739,"corporation":false,"usgs":true,"family":"Grow","given":"John A.","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":536832,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Klitgord, Kim D.","contributorId":82307,"corporation":false,"usgs":true,"family":"Klitgord","given":"Kim","email":"","middleInitial":"D.","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":536833,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":30341,"text":"wri824093 - 1982 - Effects of land use on ground-water quality in the East Everglades, Dade County, Florida","interactions":[],"lastModifiedDate":"2021-12-13T12:30:20.981613","indexId":"wri824093","displayToPublicDate":"2021-12-12T20:45:00","publicationYear":"1982","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"82-4093","title":"Effects of land use on ground-water quality in the East Everglades, Dade County, Florida","docAbstract":"Groundwater quality characteristics of the Biscayne aquifer from September 1978 through June 1979 were determined for seven land use areas within the East Everglades in Dade County, Florida. Four agricultural areas, two low-density residential areas, and Chekika Hammock State Park were investigated. The effects of land use on the groundwater were minimal in all areas; only iron , which occurs naturally in high concentrations in the Everglades, exceeded potable groundwater standards. Potassium and nitrate concentrations in certain samples increased over background concentrations in the agricultural areas. Groundwater at Chekika Hammock State Park and at a citrus grove is contaminated by brackish water flowing from an artesian well. The soil at the agricultural areas had higher concentrations of chromium, copper, and manganese than at the two residential areas or at Chekika Hammock State Park. One residential area (Coopertown) had the highest concentrations of lead and zinc and detectable polychlorinated biphenyls. Chlorinated-hydrocarbon insecticide residues in soil at three agricultural areas were higher than background concentrations. (Author 's abstract)","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri824093","collaboration":"Prepared in cooperation with the Metropolitan Dade County Planning Department","usgsCitation":"Waller, B., 1982, Effects of land use on ground-water quality in the East Everglades, Dade County, Florida: U.S. Geological Survey Water-Resources Investigations Report 82-4093, viii, 75 p., https://doi.org/10.3133/wri824093.","productDescription":"viii, 75 p.","costCenters":[{"id":27821,"text":"Caribbean-Florida Water Science Center","active":true,"usgs":true}],"links":[{"id":124279,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1982/4093/coverthb.jpg"},{"id":59134,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1982/4093/wri824093.pdf","text":"Report","size":"1.56 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 82-4093"}],"country":"United States","state":"Florida","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -80.66162109375,\n 25.18505888358067\n ],\n [\n -79.98046875,\n 25.18505888358067\n ],\n [\n -79.98046875,\n 25.997549919572112\n ],\n [\n -80.66162109375,\n 25.997549919572112\n ],\n [\n -80.66162109375,\n 25.18505888358067\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
Precipitation averages 47 inches per year and provides an abundant supply of water. About 20 inches returns to the atmosphere as evapotranspiration, and the remainder either flows directly to streams or percolates to the water table, eventually discharging to Long Island Sound. Small quantities of water are exported from the basin by the New Haven and Meridan Water Departments, and small quantities are imported by the New Britain Water Department and Metropolitan Direct Commission. Precipitation during 1931-60 resulted in an average annual runoff of 302 billion gallons. In inflow from the Connecticut River is added to the average annual runoff, the 4,370 billion gallon s per year is potentially available for water ue.
\nThe domestic, institutional, commercial, and industrial (other than cooling water) water use for 1970 was 7 billion gallons, which is only 3 percent of the total water used, whereas 97 percent of the total is cooling water for power plants. Approximately 60 percent of the 7 billion gallons is treated before being discharged back to the streams.
\nThe total amount of fresh water used during 1970 was estimated to be 256,000 million gallons (Mgal), of which 247,000 Mgal was used for cooling water at stream electric-generating plants. The quantity for domestic, commercial, industrial, and agricultural used was 9,000 Mgal, which was approximately 120 gallons a day per person. Public water systems providing 70 percent of these requirement and all the systems supplying water met the drinking water standards of the Connecticut General Assembly (1975).
\nTill is widespread and generally provides only small amounts of water. Wells in till normally yield only a few hundred gallons of water daily and may be inadequate during dry periods. The thickness of of till ranges from 0 to 15 feet; a median thickness of 26 feet is estimated from information provided in drillers' logs of 467 wells penetrating underlying bedrock. The till is generally used only as an emergency or secondary source of water.
\nBedrock aquifers underlie the entire area and include sedimentary and crystalline (igneous and metamorphic) rock types. These aquifers supply small and usually reliable quantities of water to wells and are the chief source of water for many rural homes and farms., About 90 percent of the wells tapping bedrock yield at least 2 gal/min. The median yields from wells tapping aquifers in sedimentary, igneous, and metamorphic rocks are 11, 8, and 6.5 gal/min, respectively.
\nThe quantity of water potentially available from stratified drift was estimated on the basis of hydraulic characteristics of the aquifers, mathematical modeling of the aquifer system, and evaluation of natural and induced recharge. Long-term yields estimated or ten areas underlain by significant thickness of stratified drift range from 0.4 to 4.4 million gallons per day (Mgal/d). A change in well spacing or numbering could increase the long-term yields, but detailed modeling verification studies are needed to confirm optimal well locations.
\nThe chemical and physical (turbidity, color, taste, and sediment load) quality of water is good. The water if generally low in dissolved solids and is classified as soft to hard. Surface water is less mineralized than ground water, especially during high flow, when it is primarily derived from surface runoff rather than groundwater runoff. A median dissolved-solids concentration of 42 milligrams per liter (mg/L) and median hardness of 18 mg/L were determined from water samples collected from 26 streams during the high-flow period. During the low-flow period, median dissolved-solids concentration of 61 mg/L and median hardness of 27 mg/L were determined from sample from the same streams.
\nThe quality of water in stratified-drift and crystalline-rock aquifers is generally better than that in the sedimentary-rock aquifers. Water from 32 wells tapping stratified drift had median dissolved-solids concentrations of 116 mg/L; and 33 wells tapping stratified drift and 42 tapping crystalline rock had median hardness of 73 mg/L and 68 mg/L, respectively. Water from 32 wells tapping sedimentary rock had median dissolved concentrations of 231 and 156 mg/L, respectively. Sedimentary rock generally yields the hardest water.
\nIron and manganese occur objectionable concentrations in places, particularly in water from streams draining swamps and in water from aquifers either rich in iron and manganese-nearing minerals or where the reducing environment for solution of these minerals is favorable. Concentrations of iron in excess of 0.3 mg/L were found in 35 percent of the high streamflow samples, and in 45 percent of the ground-water samples. Most of the high iron and manganese concentration in streams and aquifers are found east of the Connecticut River.
\nVicia menziesii Spreng., Hawai'i's first officially listed endangered plant species, formerly occurred across a large area in the upper montane-mesic forest habitat on the windward side of the island of Hawai'i. Until this species was ‘rediscovered’ in 1974, it had last been seen in 1915, and it was presumed to be extinct. The population is presently thought to number 150–300 plants, most of which are seedlings. These are located within a 200 ha area on the eastern flank of Mauna Loa volcano.
The primary factors responsible for the decline of V. menziesii are habitat loss and excessive predation on the plants by introduced ungulates. Continued logging and cattle grazing within its remnant range are major threats to its existence. Enhancing the survival of V. menziesii may best be accomplished by stabilizing its remaining habitat and allowing the population to reestablish itself naturally.
","language":"English","publisher":"Elsevier","doi":"10.1016/0006-3207(82)90034-9","usgsCitation":"Warshauer, F.R., and Jacobi, J., 1982, Distribution and status of Vicia menziesii Spreng. (Leguminosae): Hawai'i's first officially listed endangered plant species: Biological Conservation, v. 23, no. 2, p. 111-126, https://doi.org/10.1016/0006-3207(82)90034-9.","productDescription":"16 p.","startPage":"111","endPage":"126","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":197305,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Hawai'i","otherGeospatial":"Hawai'i, Mauna Loa Volcano","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -155.6622740700458,\n 19.363812612335536\n ],\n [\n -155.51105380670714,\n 19.235551369951082\n ],\n [\n -155.45509564758615,\n 19.244356822861917\n ],\n [\n -155.38581411724607,\n 19.350613895081167\n ],\n [\n -155.3178649240277,\n 19.438585143126204\n ],\n [\n -155.3585012062466,\n 19.472504188046685\n ],\n [\n -155.3798186001973,\n 19.501392590816337\n ],\n [\n -155.47774537865888,\n 19.54283215872283\n ],\n [\n -155.57100897719386,\n 19.504532323951167\n ],\n [\n -155.60498357380297,\n 19.481924885668775\n ],\n [\n -155.62896564199755,\n 19.397747263253564\n ],\n [\n -155.6622740700458,\n 19.363812612335536\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"23","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db64959a","contributors":{"authors":[{"text":"Warshauer, F. R.","contributorId":39873,"corporation":false,"usgs":true,"family":"Warshauer","given":"F.","middleInitial":"R.","affiliations":[],"preferred":false,"id":334559,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jacobi, J.D.","contributorId":13570,"corporation":false,"usgs":true,"family":"Jacobi","given":"J.D.","email":"","affiliations":[],"preferred":false,"id":334558,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5223719,"text":"5223719 - 1982 - Anarbylus switaki Murphy: An addition to the herpetofauna of the United States with comments on relationships with Coleonyx","interactions":[],"lastModifiedDate":"2024-12-10T16:54:33.202718","indexId":"5223719","displayToPublicDate":"2010-06-16T12:19:23","publicationYear":"1982","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2334,"text":"Journal of Herpetology","active":true,"publicationSubtype":{"id":10}},"title":"Anarbylus switaki Murphy: An addition to the herpetofauna of the United States with comments on relationships with Coleonyx","docAbstract":"Anarbys switaki, a species previously known only from Baja California Sur, Mexico, occurs in eastern San Diego and southwestern Imperial Counties in California. In California, specimens tend to have continuous transverse bars on the body, are lighter in color, and more slender in body form than in southern Baja California. California populations appear to be confined to extremely rocky habitats in desert foothill situations between 200 and 600 m. The species appears to be secretive, and occurs in low densities within rock crevices and subterranean cavities. The morphological gap between Anarbylus and Coleonyx species may not warrant generic recognition. Anarbylus is part of a diverse lizard fauna in southern California and occurs in sympatry with 15 lizard species in a small area of southern California.","language":"English","publisher":"Society for the Study of Amphibians and Reptiles","doi":"10.2307/1563903","usgsCitation":"Fritts, T.H., Snell, H., and Martin, R., 1982, Anarbylus switaki Murphy: An addition to the herpetofauna of the United States with comments on relationships with Coleonyx: Journal of Herpetology, v. 16, no. 1, p. 39-52, https://doi.org/10.2307/1563903.","productDescription":"14 p.","startPage":"39","endPage":"52","numberOfPages":"14","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":200341,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"16","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c40f","contributors":{"authors":[{"text":"Fritts, T. H.","contributorId":40147,"corporation":false,"usgs":true,"family":"Fritts","given":"T.","middleInitial":"H.","affiliations":[],"preferred":false,"id":339336,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Snell, H.L.","contributorId":49314,"corporation":false,"usgs":false,"family":"Snell","given":"H.L.","email":"","affiliations":[],"preferred":false,"id":339337,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Martin, R.L.","contributorId":85296,"corporation":false,"usgs":true,"family":"Martin","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":339338,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":7978,"text":"ofr82585 - 1982 - The Giles County, Virginia, seismogenic zone-- Seismological results and geological interpretations","interactions":[{"subject":{"id":7978,"text":"ofr82585 - 1982 - The Giles County, Virginia, seismogenic zone-- Seismological results and geological interpretations","indexId":"ofr82585","publicationYear":"1982","noYear":false,"title":"The Giles County, Virginia, seismogenic zone-- Seismological results and geological interpretations"},"predicate":"SUPERSEDED_BY","object":{"id":38521,"text":"pp1355 - 1988 - The Giles County, Virginia, seismic zone– Seismological results and geological interpretations","indexId":"pp1355","publicationYear":"1988","noYear":false,"title":"The Giles County, Virginia, seismic zone– Seismological results and geological interpretations"},"id":1}],"supersededBy":{"id":38521,"text":"pp1355 - 1988 - The Giles County, Virginia, seismic zone– Seismological results and geological interpretations","indexId":"pp1355","publicationYear":"1988","noYear":false,"title":"The Giles County, Virginia, seismic zone– Seismological results and geological interpretations"},"lastModifiedDate":"2026-01-21T17:27:41.443217","indexId":"ofr82585","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1982","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":"82-585","title":"The Giles County, Virginia, seismogenic zone-- Seismological results and geological interpretations","docAbstract":"This paper describes and interprets a newly-recognized 40-km-long seismogenic zone, which is inferred to have been the locus of a damaging earthquake in 1897. That shock was the second largest known to have occurred in the southeastern United States (MMI VIII, mb estimated at 5.8, felt over 725,000 km2). It struck Giles County in southwestern Virginia, and a recurrence would affect populous regions on and near the central Atlantic seaboard. This paper attempts to aid in evaluating that hazard by presenting and synthesizing new seismological data with geological inferences and deductions.
A five-station, 60-km aperture seismic network has been in operation in the Giles County locale since early 1978. For the subsequent 3-year monitoring period, 10 microearthquakes (M < 2) have been detected. Eight of those 10 events, plus an additional 4 relocated felt earthquakes (3.2 < M < 4.1; 1959-1976) have a tabular distribution centered at Pearisburg, Virginia. That distribution is about 40 km long, 10 km wide, strikes N. 43° E., and has a nearly vertical extent of from 5 km to 25 km in depth. Thus, a Giles County seismogenic zone is defined presently by 12 earthquakes that span 4 orders of magnitude (0 < M < 4) and 2 decades of time (1959-1980). We conclude that the 1897 earthquake occurred on that seismogenic zone. From the orientation of the tabular zone, from evidence that greatest horizontal compressive stress trends east-northeasterly at seismogenic depths in and near Giles County and from sparse P-wave first-motion data, we infer that the monitored microseismicity probably occurs by right-reverse motion on the seismogenic zone, with the southeast side dropping down with respect to the northwest side.
In the Giles County locale, the upper 3-6 km of the crust are Paleozoic sedimentary rocks that have moved some tens of kilometers northwest on nearly horizontal detachment faults. The above-mentioned reliable hypocenters for the region lie below the deepest likely detachment, indicating that Giles County seismicity probably has no simple relationship to surface geology.
Since Precambrian time, three deformational episodes could have formed steep faults under today's surface structures, at the observed hypocentral depths. These episodes were as follows: (1) As the Iapetus Ocean (Atlantic's predecessor) opened in late Precambrian or early Paleozoic time, northeast-striking normal faults formed, probably at the inferred Iapetan continental edge in central Virginia and at least as far northwest of that locus as Giles County. (2) In late Paleozoic time, detachment faults loaded the crust with several kilometers of overthrust sedimentary rocks, perhaps forming northeast-striking thrust-load faults in a brittle analogue of isostatic depression caused by thrust masses and much lighter continental glaciers. (3) As the Atlantic Ocean opened in Mesozoic time, other northeast-striking normal faults formed on the present continental margin and inland of it.
The N. 43° E.-striking seismogenic zone seems most likely to have resulted from compressional reactivation of an Iapetan normal fault, which also may have been reactivated by late Paleozoic compression and Mesozoic extension. First, the seismogenic zone probably does not occur on a thrust-load fault. The zone underlies detached structures of southern Appalachian orientations (east-northeast), but those structures are not known to be displaced where they cross the zone. Thus, if the zone occurs on a thrust-load fault, the fault and its coeval causative central Appalachian detachments would pre-date the southern Appalachian structures. That deduction contradicts stratigraphic and structural estimates of relative ages of southern and central Appalachian detachments. Second, the zone probably does not result from a Mesozoic normal fault, because known locations of Mesozoic normal faults and grabens are well to the southeast of Giles County.
Not yet known is where else in the East reactivated Iapetan normal faults might generate shocks similar to that of 1897. However, our analysis enables us to suggest specific geological and geophysical investigations that may produce results useful in answering that question. Such investigations can concentrate on defining the area of probable occurrence of other Iapetan normal faults, and on determining whether the one inferred to underlie Giles County is uniquely active or is typical of others that might exist elsewhere.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr82585","usgsCitation":"Bollinger, G.A., and Wheeler, R.L., 1982, The Giles County, Virginia, seismogenic zone-- Seismological results and geological interpretations: U.S. Geological Survey Open-File Report 82-585, iv, 136 p., https://doi.org/10.3133/ofr82585.","productDescription":"iv, 136 p.","costCenters":[],"links":[{"id":412470,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1982/0585/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":140332,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1982/0585/report-thumb.jpg"}],"country":"United States","state":"Virginia","county":"Giles County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-80.4761,37.4269],[-80.4506,37.3704],[-80.4417,37.3506],[-80.428,37.3194],[-80.4481,37.3088],[-80.4756,37.2905],[-80.4912,37.2822],[-80.5049,37.273],[-80.5147,37.2688],[-80.5302,37.2633],[-80.5551,37.2608],[-80.5787,37.2542],[-80.6075,37.2467],[-80.6219,37.2425],[-80.6724,37.2239],[-80.6828,37.2197],[-80.7051,37.209],[-80.7218,37.2039],[-80.7794,37.1888],[-80.804,37.1786],[-80.8286,37.1615],[-80.856,37.1476],[-80.8678,37.157],[-80.8824,37.1686],[-80.8624,37.1797],[-80.8725,37.1928],[-80.8947,37.1798],[-81.0099,37.2746],[-80.9785,37.294],[-80.9777,37.2934],[-80.9772,37.2932],[-80.9756,37.2931],[-80.9686,37.2927],[-80.9651,37.2932],[-80.9595,37.294],[-80.9566,37.2948],[-80.949,37.2971],[-80.9394,37.2999],[-80.9347,37.3015],[-80.9209,37.307],[-80.9111,37.3107],[-80.8985,37.3171],[-80.8916,37.3218],[-80.8859,37.3264],[-80.8813,37.33],[-80.8795,37.3312],[-80.8767,37.3332],[-80.8735,37.3352],[-80.8709,37.3368],[-80.8646,37.3401],[-80.8627,37.3411],[-80.859,37.3434],[-80.8544,37.3453],[-80.8516,37.3476],[-80.8504,37.3495],[-80.8532,37.3533],[-80.8705,37.371],[-80.8736,37.3737],[-80.8782,37.3777],[-80.8817,37.3817],[-80.8824,37.3848],[-80.8808,37.3889],[-80.8778,37.3926],[-80.8643,37.4096],[-80.8655,37.4132],[-80.8661,37.4159],[-80.8662,37.4184],[-80.8661,37.4189],[-80.8633,37.423],[-80.8627,37.4239],[-80.8575,37.4304],[-80.853,37.4278],[-80.8484,37.4256],[-80.8451,37.4257],[-80.842,37.4257],[-80.8367,37.4248],[-80.8321,37.4222],[-80.8244,37.4168],[-80.8157,37.4115],[-80.8097,37.4062],[-80.8051,37.4012],[-80.8021,37.3981],[-80.8004,37.3963],[-80.7986,37.3954],[-80.7968,37.395],[-80.7963,37.3948],[-80.7939,37.3946],[-80.7934,37.3945],[-80.7899,37.3945],[-80.7864,37.3936],[-80.7834,37.3923],[-80.7793,37.3878],[-80.7757,37.382],[-80.7709,37.3729],[-80.7629,37.3748],[-80.7531,37.3776],[-80.7507,37.3784],[-80.7423,37.3812],[-80.7307,37.3849],[-80.7248,37.3874],[-80.7198,37.3895],[-80.7052,37.3958],[-80.7048,37.396],[-80.684,37.4056],[-80.6696,37.4116],[-80.6518,37.4199],[-80.6363,37.4282],[-80.6276,37.4328],[-80.6219,37.4361],[-80.6176,37.4385],[-80.613,37.4404],[-80.6077,37.4427],[-80.6052,37.4439],[-80.603,37.445],[-80.5986,37.4473],[-80.5899,37.4523],[-80.5807,37.4583],[-80.5732,37.4628],[-80.5673,37.4661],[-80.5563,37.4707],[-80.55,37.4729],[-80.5407,37.4752],[-80.5309,37.4768],[-80.5182,37.4796],[-80.5156,37.48],[-80.5124,37.4806],[-80.5083,37.481],[-80.5054,37.4802],[-80.5026,37.4789],[-80.5002,37.4761],[-80.4984,37.473],[-80.4954,37.4666],[-80.4932,37.4596],[-80.4931,37.4528],[-80.4937,37.4487],[-80.4939,37.4467],[-80.4942,37.4446],[-80.4936,37.4419],[-80.4919,37.4396],[-80.4905,37.4379],[-80.4901,37.4374],[-80.4884,37.4356],[-80.486,37.4333],[-80.4831,37.4319],[-80.4802,37.4283],[-80.4761,37.4269]]]},\"properties\":{\"name\":\"Giles\",\"state\":\"VA\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c56e","contributors":{"authors":[{"text":"Bollinger, G. A.","contributorId":55809,"corporation":false,"usgs":true,"family":"Bollinger","given":"G.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":156924,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wheeler, Russell L. wheeler@usgs.gov","contributorId":858,"corporation":false,"usgs":true,"family":"Wheeler","given":"Russell","email":"wheeler@usgs.gov","middleInitial":"L.","affiliations":[],"preferred":false,"id":156925,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":4301,"text":"cir861 - 1982 - Geological studies of the COST nos. G-1 and G-2 wells, United States North Atlantic outer continental shelf","interactions":[],"lastModifiedDate":"2018-10-23T17:49:36","indexId":"cir861","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1982","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":"861","title":"Geological studies of the COST nos. G-1 and G-2 wells, United States North Atlantic outer continental shelf","docAbstract":"The COST Nos. G-1 and G-2 wells (fig. 1) are the second and third deep stratigraphic test wells drilled in the North Atlantic Outer Continental Shelf of the United States. COST No. G-1 was drilled in the Georges Bank basin to a total depth of 16,071 ft (4,898 m). G-1 bottomed in phyllite, slate, and metaquartzite overlain by weakly metamorphosed dolomite, all of Cambrian age. From approximately 15,600 to 12,400 ft (4,755 to 3,780 m) the strata are Upper Triassic(?), Lower Jurassic(?), and Middle Jurassic, predominantly red shales, sandstones, and conglomerates. Thin, gray Middle Jurassic beds of shale, sandstone, limestone, and dolomite occur from 12,400 to 9,900 ft (3,780 to 3,018 m). From 9,900 to 1,030 ft (3,018 to 314 m) are coarse-grained unconsolidated sands and loosely cemented sandstones, with beds of gray shale, lignite, and coal. The microfossils indicate the rocks are Upper Jurassic from 10,100 ft (3,078 m) up to 5,400 ft (1,646 m) and Cretaceous from that depth to 1,030 ft (314 m). No younger or shallower rocks were recovered in the drilling at the COST No. G-1 site, but an Eocene limestone is inferred to be disconformable over Santonian strata. The Jurassic strata of the COST No. G-1 well were deposited in shallow marine, marginal marine, and nonmarine environments, which changed to a dominantly shallow marine but still nearshore environment in the Cretaceous. \r\n\r\nThe COST No. G-2 well was drilled 42 statute miles {68 km) east of the G-1 site, still within the Georges Bank basin, to a depth of 21,874 ft (6,667 m). The bottom 40 ft (12 m) of salt and anhydrite is overlain by approximately 7,000 ft {2,134 m) of Upper Triassic{?), Lower Jurassic{?) and Middle Jurassic dolomite, limestone, and interbedded anhydrite from 21,830 to 13,615 ft (6,654 to 4,153 m). From 13,500 to 9,700 ft (4,115 to 2,957 m) are Middle Jurassic limestones with interbedded sandstone. From 9,700 to 4,000 ft (2,957 to 1,219 m) are Upper Jurassic and Cretaceous interbedded sandstones and limestones overlain by Upper Cretaceous unconsolidated sands, sandstones, and calcareous shales. Pliocene, Miocene, Eocene, and Paleocene strata are disconformable over Santonian rocks; uppermost Cretaceous rocks are missing at this site, as at G-1. The sedimentary rocks in the COST No. G-2 well were deposited in somewhat deeper water, farther away from sources of terrigenous material than those at G-l, but still in marginal marine to shallow marine environments. \r\n\r\nData from geophysical logs and examination of conventional cores, wellcuttings, and sidewall cores show that below 10,000 ft {3,048 m), the strata in both wells have moderate porosities {< 20 percent) and low to moderate permeabilities {< 100 mD) and are thus considered adequate to poor reservoir rocks. Above 10,000 ft (3,000 m) the porosities range from 16 to 39 percent, and the permeabilities are highly variable, ranging from 0.01 to 7,100 mD. \r\n\r\nMeasurements of vitrinite reflectance, color alteration of visible organic matter, and various organic geochemical properties suggest that the Tertiary and Cretaceous strata of the COST Nos. G-1 and G-2 are not prospective for oil and gas. These sediments have not been buried deeply enough for hydrocarbon generation, and the kerogen and extractable organic matter in them are thermally immature. However, the Jurassic rocks at the G-1 site do contain small amounts of thermally mature gas-prone kerogens. The Jurassic rocks at COST No. G-2 are also gas-prone and are slightly richer in organic carbon and total extractable hydrocarbons than the G-1 rocks, but both sites have only poor to fair oil and gas source-rock potential.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/cir861","usgsCitation":"Wenkam, C.R., 1982, Geological studies of the COST nos. G-1 and G-2 wells, United States North Atlantic outer continental shelf: U.S. Geological Survey Circular 861, vi, 193 p. :ill., maps ;26 cm., https://doi.org/10.3133/cir861.","productDescription":"vi, 193 p. :ill., maps ;26 cm.","costCenters":[],"links":[{"id":31412,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1982/0861/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124681,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1982/0861/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adee4b07f02db687461","contributors":{"editors":[{"text":"Scholle, Peter A.","contributorId":60194,"corporation":false,"usgs":true,"family":"Scholle","given":"Peter A.","affiliations":[],"preferred":false,"id":749517,"contributorType":{"id":2,"text":"Editors"},"rank":1}],"authors":[{"text":"Wenkam, Chiye R.","contributorId":105286,"corporation":false,"usgs":true,"family":"Wenkam","given":"Chiye","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":148769,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":9966,"text":"ofr82493 - 1982 - The geology of the Kutztown and Hamburg 7 1/2-minute quadrangles, eastern Pennsylvania","interactions":[],"lastModifiedDate":"2026-01-21T17:27:28.454679","indexId":"ofr82493","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1982","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":"82-493","title":"The geology of the Kutztown and Hamburg 7 1/2-minute quadrangles, eastern Pennsylvania","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr82493","usgsCitation":"Lash, G.G., 1982, The geology of the Kutztown and Hamburg 7 1/2-minute quadrangles, eastern Pennsylvania: U.S. Geological Survey Open-File Report 82-493, 3 Plates: 9.08 x 11.46 inches or smaller, https://doi.org/10.3133/ofr82493.","productDescription":"3 Plates: 9.08 x 11.46 inches or smaller","costCenters":[],"links":[{"id":426552,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1982/0493/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":426551,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1982/0493/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":426550,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1982/0493/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":142425,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1982/0493/report-thumb.jpg"}],"scale":"24000","country":"United States","state":"Pennsylvania","city":"Kutztown","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -75.79625118853856,\n 40.531669801963176\n ],\n [\n -75.79625118853856,\n 40.50144072971335\n ],\n [\n -75.74910540374503,\n 40.50144072971335\n ],\n [\n -75.74910540374503,\n 40.531669801963176\n ],\n [\n -75.79625118853856,\n 40.531669801963176\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d649","contributors":{"authors":[{"text":"Lash, G. G.","contributorId":60648,"corporation":false,"usgs":true,"family":"Lash","given":"G.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":160585,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":59546,"text":"mf1415B - 1982 - Geochemical survey of the Cohutta Wilderness and the Hemp Top Roadless Area, northern Georgia and southeastern Tennessee","interactions":[],"lastModifiedDate":"2018-09-14T12:52:09","indexId":"mf1415B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1982","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1415","chapter":"B","title":"Geochemical survey of the Cohutta Wilderness and the Hemp Top Roadless Area, northern Georgia and southeastern Tennessee","docAbstract":"The contiguous Cohutta Wilderness and Hemp Top Roadless Area are in the western part of the Blue Ridge physiographic province of northern Georgia and southeastern Tennessee (fig. 1). All of the study area is in Georgia except an irregular strip of land about 1 mi at its widest on the northern end of the Cohutta Wilderness in Tennessee. The area of the Cohutta Wilderness is 34,650 acres; that of the Hemp Top Roadless Area is 2,800 acres. The areas are in rugged mountainous terrain- a strongly dissected upland ranging in altitude from about 980 to 4,200 ft above sea level. Local altitude differences of 1,450-2,000 ft and slopes steeper than 25° are common. The north end of the Cohutta Wilderness is about 6 mi south of the Ocoee River gorge, 10 mi west-southwest of the major copper-and sulfur-mining district at Ducktown, Tenn., and approximately 22 mi southeast of Cleveland, Tenn., in Bradley County, west of the area shown in figure 1. The eastern, central, and northwestern parts of the wilderness are drained by Jacks River and it tributaries; the southwestern part, by the Conasauga River and its tributaries; and the Hemp Top Roadless Area, by Tumbling Creek and some of its western tributaries. All drainage ultimately goes to the Ocoee River and from these into the Hiwassee River.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf1415B","usgsCitation":"Gair, J.E., 1982, Geochemical survey of the Cohutta Wilderness and the Hemp Top Roadless Area, northern Georgia and southeastern Tennessee: U.S. Geological Survey Miscellaneous Field Studies Map 1415, 2 Plates: 52.33 x 39.84 inches and 48.70 x 31.49 inches, https://doi.org/10.3133/mf1415B.","productDescription":"2 Plates: 52.33 x 39.84 inches and 48.70 x 31.49 inches","costCenters":[],"links":[{"id":183161,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/1415-B/report-thumb.jpg"},{"id":357341,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1415-B/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":357342,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1415-B/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"0","country":"United States","state":"Georgia, Tennessee","otherGeospatial":"Cohutta Wilderness, Hemp Top Roadless Area","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -84.66666666666667,34.833333333333336 ], [ -84.66666666666667,35.016666666666666 ], [ -84.45083333333334,35.016666666666666 ], [ -84.45083333333334,34.833333333333336 ], [ -84.66666666666667,34.833333333333336 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b20e4b07f02db6aba72","contributors":{"authors":[{"text":"Gair, Jacob E.","contributorId":18381,"corporation":false,"usgs":true,"family":"Gair","given":"Jacob","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":262200,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":56201,"text":"wdrNY811 - 1982 - Water resources data, New York, water year 1981; Volume 1. Eastern New York excluding Long Island","interactions":[],"lastModifiedDate":"2024-07-22T21:02:49.725547","indexId":"wdrNY811","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1982","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":340,"text":"Water Data Report","code":"WDR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"NY-81-1","title":"Water resources data, New York, water year 1981; Volume 1. Eastern New York excluding Long Island","docAbstract":"Water resources data for the 1981 water year for New York consist of records of stage, discharge, and water quality of streams; stage, contents, and water quality of lakes and reservoirs; and water levels of ground-water wells. This volume contains records for water discharge at 105 gaging stations; stage only at 6 gaging stations; and stage and contents at 4 gaging stations and 19 other lakes and reservoirs; water quality at 29 gaging stations, 5 precipitation stations and 4 partial-record stations; and water levels at 23 observation wells. Also included are data for 50 crest-stage and 14 low-flow partial-record stations. Additional water data were collected at various sites not involved in the systematic data-collection program and are published as miscellaneous measurements and analyses. These data together with the data in Volumes 2 and 3 represent that part of the National Water Data System operated by the U.S. Geological Survey and cooperating State, local, and Federal agencies in New York.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wdrNY811","collaboration":"Prepared in cooperation with the State of New York and with other agencies","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1982, Water resources data, New York, water year 1981; Volume 1. Eastern New York excluding Long Island: U.S. Geological Survey Water Data Report NY-81-1, viii, 318 p., https://doi.org/10.3133/wdrNY811.","productDescription":"viii, 318 p.","costCenters":[],"links":[{"id":431318,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wdr/1981/ny-81-1/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":180910,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wdr/1981/ny-81-1/report-thumb.jpg"}],"country":"United States","state":"New York","otherGeospatial":"eastern New York excluding Long Island","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -73.50726953585145,\n 44.98041799746011\n ],\n [\n -76.02932029130172,\n 44.98041799746011\n ],\n [\n -76.02932029130172,\n 41.044913356229046\n ],\n [\n -73.50726953585145,\n 41.044913356229046\n ],\n [\n -73.50726953585145,\n 44.98041799746011\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f5e4b07f02db5f0f16","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":532449,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}