The original range of the paddlefish was the Mississippi River drainage and adjacent Gul f Coast dra i nage. It was once found in some of the Great Lakes (Carlson and Bonislawsky 1981). The paddlefish is generally an inhabitant of large rivers, but it occurs in reservoirs and natural lakes connected to large rivers. Much of the original range has been reduced due to habitat alterations: (1) destruction of spawning areas; (2) blockage of movements by dams; (3) channelization and elimination of backwater areas; (4) dewatering of streams; and (5) pollution (Carlson and Bonislawsky 1981). Several States officially consider the paddlefish as rare or endangered (Miller 1972). An indexed bibliography of all known paddlefish work was prepared by Graham and Bonislawsky (1978) and recently updated to include more than 480 citations (Graham and Bonislawsky, in press).
","language":"English","publisher":"U.S. Fish and Wildlife Service","usgsCitation":"Hubert, W.A., Anderson, S.H., Southall, P.D., and Crance, J.H., 1984, Habitat Suitability Index Models and Instream Flow Suitability Curves: Paddlefish: FWS/OBS 82/10.80, vi, 32 p.","productDescription":"vi, 32 p.","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":167269,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a81e4b07f02db649e5c","contributors":{"authors":[{"text":"Hubert, Wayne A.","contributorId":9325,"corporation":false,"usgs":true,"family":"Hubert","given":"Wayne","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":216463,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Anderson, Stanley H.","contributorId":68361,"corporation":false,"usgs":true,"family":"Anderson","given":"Stanley","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":216466,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Southall, Peter D.","contributorId":39844,"corporation":false,"usgs":true,"family":"Southall","given":"Peter","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":216465,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Crance, Johnie H.","contributorId":9326,"corporation":false,"usgs":true,"family":"Crance","given":"Johnie","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":216464,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":36578,"text":"fwsobs82_10_56 - 1984 - Habitat Suitability Index Models: Walleye","interactions":[],"lastModifiedDate":"2022-02-09T15:19:36.985384","indexId":"fwsobs82_10_56","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"seriesTitle":{"id":20,"text":"FWS/OBS","active":false,"publicationSubtype":{"id":1}},"seriesNumber":"82/10.56","subseriesTitle":"Habitat Suitability Index","title":"Habitat Suitability Index Models: Walleye","docAbstract":"The wall eye is native to freshwater ri vers and 1akes of Canada and the United States, with rare occurrences in brackish water (Scott and Crossman 1973). In the United States, its native range occurs primarily in drainages east of the Rocky Mountains and west of the Appalachians; however, it has been widely introduced into reservoirs outside its native range (Colby et al. 1979). Walleye hybridize with sauger (S. canadense) and blue pike (S. v. glaucum) (Scott and Crossman 1973).
","language":"English","publisher":"U.S. Fish and Wildlife Service","usgsCitation":"McMahon, T., Terrell, J.W., and Nelson, P.C., 1984, Habitat Suitability Index Models: Walleye: FWS/OBS 82/10.56, viii, 43 p.","productDescription":"viii, 43 p.","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":165604,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6497a2","contributors":{"authors":[{"text":"McMahon, Thomas E.","contributorId":93548,"corporation":false,"usgs":true,"family":"McMahon","given":"Thomas E.","affiliations":[],"preferred":false,"id":216576,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Terrell, James W. 0000-0001-5394-5663","orcid":"https://orcid.org/0000-0001-5394-5663","contributorId":92726,"corporation":false,"usgs":true,"family":"Terrell","given":"James","email":"","middleInitial":"W.","affiliations":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"preferred":true,"id":216575,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Nelson, Patrick C.","contributorId":68799,"corporation":false,"usgs":true,"family":"Nelson","given":"Patrick","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":216574,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":11666,"text":"ofr84637 - 1984 - Mineral resource potential of national forest RARE II and wilderness areas in Montana","interactions":[],"lastModifiedDate":"2012-02-02T00:06:32","indexId":"ofr84637","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"84-637","title":"Mineral resource potential of national forest RARE II and wilderness areas in Montana","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr84637","usgsCitation":"Williams, C.E., and Pearson, R.C., 1984, Mineral resource potential of national forest RARE II and wilderness areas in Montana: U.S. Geological Survey Open-File Report 84-637, v, 141 p. :map ;28 cm., https://doi.org/10.3133/ofr84637.","productDescription":"v, 141 p. :map ;28 cm.","costCenters":[],"links":[{"id":143844,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1984/0637/report-thumb.jpg"},{"id":39522,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1984/0637/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":39523,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1984/0637/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b0be4b07f02db69d603","contributors":{"authors":[{"text":"Williams, C. E. (compiler)","contributorId":54205,"corporation":false,"usgs":true,"family":"Williams","given":"C.","suffix":"(compiler)","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":163543,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pearson, R. C.","contributorId":30978,"corporation":false,"usgs":true,"family":"Pearson","given":"R.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":163542,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5864,"text":"pp1272 - 1984 - High-temperature, large-volume, lavalike ash-flow tuffs without calderas in southwestern Idaho","interactions":[],"lastModifiedDate":"2012-02-02T00:05:51","indexId":"pp1272","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1272","title":"High-temperature, large-volume, lavalike ash-flow tuffs without calderas in southwestern Idaho","docAbstract":"Rhyolitic rocks were erupted from vents in and adjacent to the Owyhee Mountains and Owyhee Plateau of southwestern Idaho from 16 m.y. ago to about 10 m.y. ago. They were deposited on a highly irregular surface developed on a variety of basement rocks that include granitic rocks of Cretaceous age, quartz latite and rhyodacite tuffs and lava flows of Eocene age, andesitic and basaltic lava flows of Oligocene age, and latitic and basaltic lava flows of early Miocene age. \r\n\r\nThe rhyolitic rocks are principally welded tuffs that, regardless of their source, have one feature in common-namely internal characteristics indicating en-masse, viscous lavalike flowage. The flowage features commonly include considerable thicknesses of flow breccia at the bases of various cooling units. On the basis of the tabular nature of the rhyolitic deposits, their broad areal extents, and the local preservation of pyroclastic textures at the bases, tops, and distal ends of some of the deposits, we have concluded that the rocks were emplaced as ash flows at extremely high temperatures and that they coalesced to liquids before final emplacement and cooling. Temperatures of l090?C and higher are indicated by iron-titanium oxide compositions. \r\n\r\nRhyolites that are about 16 m.y. old are preserved mostly in the downdropped eastern and western flanks of the Silver City Range and they are inferred to have been erupted from the Silver City Range. They rarely contain more than about 2 percent phenocrysts that consist of quartz and subequal amounts of plagioclase and alkali feldspar; commonly, they contain biotite, and they are the only rhyolitic rocks in the area to do so. The several rhyolitic units that are 14 m.y. to about 10 m.y. old contain only pyroxene-principally ferriferous and intermediate pigeonites-as mafic constituents. The rhyolites of the Silver City Range comprise many cooling units, none of which can be traced for great distances. \r\n\r\nRocks erupted from the Owyhee Plateau include two sequences that were traced over areas having diameters of about 100 km. These two sheets are the herein-named Swisher Mountain Tuff, which is about 13.8 m.y. old, and the Little Jacks Tuff, which is about 10 m.y. old. The Swisher Mountain Tuff was erupted from the Juniper Mountain volcanic center, a gentle dome that is not bounded by arcuate faults indicative of cauldron subsidence. The tuff is 200 m thick over a considerable area in and adjacent to its source. It apparently thins gradually toward its distal edges, and it is inferred to be uniformly distributed around its source at Juniper Mountain. The unit contains vitrophyres at various intervals from base to top, and, although the vitrophyres are, in general, flow layered and commonly flow brecciated, they occasionally contain well-defined pumice clasts. The vitrophyres indicate compound cooling, and, near the distal edges of the sheet, some of them probably represent complete cooling breaks. \r\n\r\nThe Little Jacks Tuff onlaps the Swisher Mountain Tuff in expo sures east of Juniper Mountain, and it is inferred to have been erupted from a source on the part of the Owyhee Plateau that lies just east of the area studied. This inferred source area, like that at Juniper Mountain, is also expressed today as a gentle dome without structural features indicative of cauldron subsidence. The Little Jacks Tuff, in most exposures in the deep canyons of the Plateau, consists of at least four cooling units, and, in places in the eastern part of the studied area near the source area, it possibly comprises as many as six. Although there is no obvious evidence of erosion between the various cooling units, magnetic polarity measurements indicate that there were at least two magnetic reversals during the eruption interval of the Little Jacks Tuff. Like the Swisher Mountain Tuff, the Little Jacks has flattened pumice clasts in a few outcrops-principally at the bases of the various cooling units. \r\n\r\nThe two tuff sequences are calc-a","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/pp1272","usgsCitation":"Ekren, E.B., McIntyre, D.H., and Bennett, E.H., 1984, High-temperature, large-volume, lavalike ash-flow tuffs without calderas in southwestern Idaho: U.S. Geological Survey Professional Paper 1272, 76 p.; 2 plates in pocket, https://doi.org/10.3133/pp1272.","productDescription":"76 p.; 2 plates in pocket","costCenters":[],"links":[{"id":126352,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1272/report-thumb.jpg"},{"id":247321,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1272/plate-1.pdf","size":"4589","linkFileType":{"id":1,"text":"pdf"}},{"id":247322,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1272/plate-2.pdf","size":"4882","linkFileType":{"id":1,"text":"pdf"}},{"id":32655,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1272/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a58e4b07f02db62efd5","contributors":{"authors":[{"text":"Ekren, E. B.","contributorId":14371,"corporation":false,"usgs":true,"family":"Ekren","given":"E.","middleInitial":"B.","affiliations":[],"preferred":false,"id":151701,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McIntyre, David H.","contributorId":46490,"corporation":false,"usgs":true,"family":"McIntyre","given":"David","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":151702,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bennett, Earl H.","contributorId":97093,"corporation":false,"usgs":true,"family":"Bennett","given":"Earl","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":151703,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":19616,"text":"ofr84159 - 1984 - Reconnaissance geology of the Qufar Quadrangle, sheet 27/41 D, Kingdom of Saudi Arabia","interactions":[],"lastModifiedDate":"2015-09-07T14:38:30","indexId":"ofr84159","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"84-159","title":"Reconnaissance geology of the Qufar Quadrangle, sheet 27/41 D, Kingdom of Saudi Arabia","docAbstract":"The Qufar quadrangle, south of the city of Ha' il in the northern Arabian Shield is underlain by late Proterozoic granitic and dioritic rocks and two volcano-sedimentary sequences. Phanerozoic rocks include a few outcrops of the Cambrian and Ordovician Saq Sandstone and small remnants of Miocene basalt flows and plugs.
\nThe oldest rocks in the quadrangle comprise the Nuf formation, a layered sequence of submarine, tholeiitic metabasalt and meta-andesite, and interbedded metagraywacke and marble. The Nuf formation may correlate with rocks mapped as Halaban or Hulayfah group (approximately 780-720 Ma old) to the south of the quadrangle. Cogenetic subvolcanic rocks include gabbro and diorite. Voluminous plutonic rocks of approximately monzogranite composition intruded and dismembered the Nuf formation, gabbro, and diorite, which were simultaneously metamorphosed and internally deformed. Metamorphism of the Nuf formation was variable, but generally' upper greenstone-facies assemblages were produced.
\nFollowing a period of extensive erosion, the Hadn formation, dacitic to rhyolitic ignimbrite and flow breccia, and interbedded subgraywacke, arkose, and minor conglomerate was deposited. The Hadn formation may be a continental equivalent of the Murdama group, which is mapped to the south of the quadrangle and is approximately 650 to 610 Ma old.
\nNumerous plutons, predominantly monzogranite, but ranging from gabbro to alkali-feldspar granite, post-date the Hadn formation. Of these, the Malayhah granite is particularly noteworthy because it has a broad zone of cataclasis along the western and southern border. Country rock within several kilometers of the western contact is also highly sheared, predominantly along northerly trends. Locally, a melange of several rock types was produced. Contact metamorphism to garnet-amphibolite hornfels facies occurred at this time, and may be responsible for the formation of small sub-economic magnetite lenses interlayered with some of the marbles of the Nuf formation. In the northern part of the quadrangle, southeast dipping imbricate thrust faults probably closely post-date the emplacement of the Mulayhah granite. These thrusts were followed in time by predominantly northeast-trending high-angle faults.
\nThe last major plutonic event in the area is the intrusion of the alkalic granite complexes at Jabal Aja and Jabal Sal ma about 580 Ma ago. Of particular note is a per alkalic border facies of the Jabal Aja complex that is associated with pegmatites enriched in thorium, niobium, and rare-earth elements.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr84159","usgsCitation":"Kellogg, K., 1984, Reconnaissance geology of the Qufar Quadrangle, sheet 27/41 D, Kingdom of Saudi Arabia: U.S. Geological Survey Open-File Report 84-159, iii, 39 p. :maps ;28 cm., https://doi.org/10.3133/ofr84159.","productDescription":"iii, 39 p. :maps ;28 cm.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":49085,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1984/0159/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49086,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1984/0159/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49087,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1984/0159/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":152590,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1984/0159/report-thumb.jpg"}],"country":"Saudi Arabia","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n 40,\n 26\n ],\n [\n 40,\n 28\n ],\n [\n 42,\n 28\n ],\n [\n 42,\n 26\n ],\n [\n 40,\n 26\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6de4b07f02db63f234","contributors":{"authors":[{"text":"Kellogg, K.S.","contributorId":99145,"corporation":false,"usgs":true,"family":"Kellogg","given":"K.S.","email":"","affiliations":[],"preferred":false,"id":181220,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":58927,"text":"mf1611D - 1984 - Maps showing mines, quarries, prospects, and exposures in the Devils Fork Roadless Area, Scott County, Virginia","interactions":[],"lastModifiedDate":"2016-08-22T09:45:38","indexId":"mf1611D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"1611","chapter":"D","title":"Maps showing mines, quarries, prospects, and exposures in the Devils Fork Roadless Area, Scott County, Virginia","docAbstract":"The Wilderness Act (Public Law 88-577, September 3, 1964) and related acts require the U.S. Geological Survey and the U.S. Bureau of Mines to survey certain areas on Federal lands to determine their mineral resource potential. Results must be made available to the public and be submitted to the President and the Congress. This report presents the results of a survey of mines, quarries, prospects, and coal exposures in the vicinity of the Devils Fork Roadless Area in the Jefferson National Forest, Scott County, Virginia. Devils Fork Roadless Area was classified as a further planning area during the Second Roadless Area Review and Evaluation (RARE II) by the U.S. Forest Service, January 1979.
\nThe Devils Fork Roadless Area is in the Clinch Ranger district of the Jefferson National Forest, southwestern Virginia. It is located in Scott County, about 5 miles southeast of Big Stone Gap, Virginia, and is accessible from there via U.W. 23 to Duffield, Virginia, and then northeastward along State Route 653 (fig. 1). Access from the north is provided by State Routes 616, 619, and Forest Route 237. Southern access is provided by State Routes 619 and 649. The interior is accessible by foot along overgrown logging railroad grades and abandoned forest roads on the lower portions of Devil Fork, Straight Fork, and Roddy Branch.
\nThe Devils Fork Roadless Area is located at the eastern edge of the Appalachian coal region and is within the Cumberland Mountain section of the Appalachian Plateau physiographic province. Most of the area is drained by Devil Fork and its tributaries. Clinch Rock Branch of Straight Creek, Roddy Branch of Valley Creek, and Stinking Creek, all tributary to the Clinch River, drain small fringe tracts. Altitudes range from about 1,550 ft on the lower part of Straight Fork to about 3,490 ft at Cox Place on Little Mountain. Vegetation varies from mixed hardwoods in the uplands to thickets of conifer, rhododendron, and laurel in moist protected areas, as in coves along drainage courses.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf1611D","usgsCitation":"Behum, P.T., 1984, Maps showing mines, quarries, prospects, and exposures in the Devils Fork Roadless Area, Scott County, Virginia: U.S. Geological Survey Miscellaneous Field Studies Map 1611, 27.59 x 37.04 inches, https://doi.org/10.3133/mf1611D.","productDescription":"27.59 x 37.04 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":183726,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/mf1611D.PNG"},{"id":327159,"rank":1,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1611-D/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Virginia","county":"Scott County","otherGeospatial":"Devils Fork Roadless Area, Jefferson National Forest","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -82.70083333333334,36.75138888888889 ], [ -82.70083333333334,36.8675 ], [ -82.58444444444444,36.8675 ], [ -82.58444444444444,36.75138888888889 ], [ -82.70083333333334,36.75138888888889 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a10e4b07f02db5ff6a3","contributors":{"authors":[{"text":"Behum, Paul T.","contributorId":86894,"corporation":false,"usgs":true,"family":"Behum","given":"Paul","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":261108,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":6975,"text":"ofr84479 - 1984 - Analyses of rock samples from the Circle Quadrangle, Alaska","interactions":[],"lastModifiedDate":"2012-02-02T00:05:42","indexId":"ofr84479","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"84-479","title":"Analyses of rock samples from the Circle Quadrangle, Alaska","docAbstract":"Suspendedsediment and reservoir sedimentation data have been analyzed to\r\ndetermine sediment yields and transport characteristics of Tennessee streams Data from\r\n31 reservoirs plus suspendedsediment data from TVA sampling efforts in the 1930?s and\r\n1960?s, and U.S. Geological Survey efforts from 1975-82 have been used.\r\nResults of the analyses show that the measured suspended-sediment is mostly silt\r\nand clay-size material even in the sand bed channels of western Tennessee. Samples of\r\nsuspended sediment rarely exceed 25 percent sand. Computed unmeasured load is less\r\nthan 10 percent of the total sediment load in western Tennessee. Unmeasured load has\r\nnot been computed for middle and eastern Tennessee streams because the bed material is\r\ngenerally coarse and quite variable. However, unmeasured load in these streams is\r\nbelieved to be less than 5 percent of total load. Transport curves show that when flow is\r\nless than about 1 cubic foot per second per square mile, western Tennessee streams have\r\nhigher concentrations than middle or eastern streams. When flow exceeds about 10 cubic\r\nfeet per second per square mile, however, concentrations in middle and eastern streams\r\ncan equal or exceed those in western streams. The more efficient sediment-delivery\r\nprocesses operating in middle and eastern Tennessee basins are responsible for the rapid\r\nincreases in suspended sediment concentrations with increasing flow.\r\nSediment yields for middle and eastern Tennessee basins generally are less than 800\r\ntons per square mile per year, however, heavily strip-mined basins can have yields from\r\n1,000 to 3,000 tons per square mile per year. Yields for the heavily agricultural and\r\nchannelized basins of western Tennessee generally range from 700 to 1,000 tons per\r\nsquare mile per year.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr84479","usgsCitation":"Foster, H., O’Leary, R.M., McDougal, C.M., and Menzie, W., 1984, Analyses of rock samples from the Circle Quadrangle, Alaska: U.S. Geological Survey Open-File Report 84-479, 116, 126 p. . :map ;28 cm., https://doi.org/10.3133/ofr84479.","productDescription":"116, 126 p. . :map ;28 cm.","costCenters":[],"links":[{"id":761,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/ofr84-749","linkFileType":{"id":5,"text":"html"}},{"id":139680,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1984/0479/report-thumb.jpg"},{"id":34251,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1984/0479/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":34252,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1984/0479/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abce4b07f02db672d1b","contributors":{"authors":[{"text":"Foster, H.L.","contributorId":34894,"corporation":false,"usgs":true,"family":"Foster","given":"H.L.","email":"","affiliations":[],"preferred":false,"id":153746,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"O’Leary, R. M.","contributorId":44894,"corporation":false,"usgs":true,"family":"O’Leary","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":153747,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McDougal, C. M.","contributorId":21129,"corporation":false,"usgs":true,"family":"McDougal","given":"C.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":153745,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Menzie, W. D.","contributorId":52916,"corporation":false,"usgs":true,"family":"Menzie","given":"W. D.","affiliations":[],"preferred":false,"id":153748,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70207376,"text":"70207376 - 1984 - Origin of Hawaiian tholeiite: A metasomatic model","interactions":[],"lastModifiedDate":"2020-06-03T15:04:42.86726","indexId":"70207376","displayToPublicDate":"1984-12-18T13:01:15","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2314,"text":"Journal of Geophysical Research B: Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Origin of Hawaiian tholeiite: A metasomatic model","docAbstract":"Two voluminous magma types generated in the mantle underlying the Pacific plate are mid‐ocean ridge tholeiite (MORB) erupted at the East Pacific Rise spreading center and Hawaiian tholeiite (HT) erupted above the Hawaiian hot spot or melting anomaly. MORB has low initial 87Sr/86Sr ratios and low amounts of all incompatible trace elements including rare earths; chondrite‐normalized patterns are depleted in light rare earths. HT, by contrast, has higher initial 87Sr/86Sr and higher amounts of incompatible trace elements; chondrite‐nor‐malized patterns are enriched in the middle and light rare earths. HT is generally poorer in CaO and Al2O3 and much richer in total iron and TiO2 compared with MORB having the same MgO content. Primary magma compositions for the two volcanic systems are calculated in Fe‐Mg equilibrium with residual olivine (Fo92). MORB is generated by partial melting of a trace element depleted Iherzolite source leaving a residual assemblage dominated by olivine and orthopyroxene. The percentage of partial melting for a primary magma containing 15% MgO is calculated to be 35–42% in a source mantle having a heavy rare earth content of 3×chondrite and 33–35% MgO. HT, represented by Kilauea tholeiite, is generated by partial melting of a mixture of unmelted and residual mantle for MORB which has been modified by metasomatic addition of a nephelinitic fluid, amphibole, and minor amounts of apatite and Fe‐bearing phases such as sulfide and magnetite/ilmenite. This model yields a picritic magma in equilbrium with magnesian dunite at high (>40%) degrees of partial melting. The source also has 35% MgO before partial melting. Melting in both systems in polyvariant and not controlled by lower‐temperature invariant equilibria. The low‐velocity zone is considered to be the source of metasomatic fluids that are driven upward into the lowermost lithosphere in response to a thermal plume. Picritic primary magmas are produced by shear melting, localized in the zone of thinned and metasomatized lithosphere beneath Hawaii. Melt extraction is rapid and episodic at intervals of months to decades; magma is not stored in the mantle but passes upward to a plexus of storage reservoirs located 2–6 km beneath the surface of Kilauea. Kilauea primary magmas fractionate olivine during upward transport to reach bulk compositions of 13–14% MgO in storage. Different magma batches erupted to the surface, distinguished by different major and minor element compositons compared at similar MgO content, represent combinations of differing degrees of metasomatic enrichment, differing degrees of partial melting, and some effects of premelting mantle heterogeneity.
","language":"English","publisher":"AGU","doi":"10.1029/JB089iB05p03233","usgsCitation":"Wright, T., 1984, Origin of Hawaiian tholeiite: A metasomatic model: Journal of Geophysical Research B: Solid Earth, v. 89, no. 5, p. 3233-3252, https://doi.org/10.1029/JB089iB05p03233.","productDescription":"20 p.","startPage":"3233","endPage":"3252","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":370418,"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 -160.48828125,\n 21.6778482933475\n ],\n [\n -156.181640625,\n 18.271086109608877\n ],\n [\n -154.0283203125,\n 19.68397023588844\n ],\n [\n -159.14794921875,\n 22.958393318086348\n ],\n [\n -160.48828125,\n 21.6778482933475\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"89","issue":"5","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","contributors":{"authors":[{"text":"Wright, Thomas L. twright@usgs.gov","contributorId":3890,"corporation":false,"usgs":true,"family":"Wright","given":"Thomas L.","email":"twright@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":777861,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70120857,"text":"70120857 - 1984 - A workshop model simulating fate and effect of drilling muds and cuttings on benthic communities","interactions":[],"lastModifiedDate":"2014-08-18T10:13:10","indexId":"70120857","displayToPublicDate":"1984-12-01T09:47:05","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":9,"text":"Other Report"},"seriesNumber":"WELUT-85/W02","title":"A workshop model simulating fate and effect of drilling muds and cuttings on benthic communities","docAbstract":"Oil and gas exploration and production at marine sites has generated concern over potential environmental impacts resulting from the discharge of spent drilling muds and cuttings. This concern has led to a broad array of publicly and privately sponsored research. This report described a cooperative modeling effort designed to focus information resulting from this research through construction of explicit equations that simulate the potential impacts of discharge drilling fluids (muds) and cuttings on marine communities. The model is the result of collaboration among more than 30 scientists. The principal cooperating organizations were the E.S. Environmental Protection Agency, the U.S. Minerals Management Service, the Offshore Operators Committee, and the Alaska Oil and Gas Association.
\nThe overall simulation model can be conceptualized as three connected submodels: Discharge and Plume Fate, Sediment Redistribution, and Benthic Community Effects. On each day of simulation, these submodels are executed in sequence, with flows of information between submodels. The Benthic Community Effects submodel can be further divided into sections that calculate mortality due to burial, mortality due to toxicity, mortality due to resuspension disturbance, and growth of the community.
\nThe model represents a series of seven discrete 1-m2 plots at specified distances along a transect in one direction away from a discharge point. It consists of coupled difference equations for which parameter values can easily be set to evaluate different conditions or to examine the sensitivity of output to various assumptions. Sets of parameter values were developed to represent four general cases or scenarios: (1) a shallow (5 m), cold environment with ice cover during a substantial fraction of the year, such as might be encountered in the Beaufort Sea, Alaska; (2) a shallow (20 m), temperate environment, such as might be encountered in the Gulf of Mexico; (3) a deeper (80 m), temperate environment, such as might be encountered in the Gulf of Mexico; and (4) a very deep (1,000 m) environment, such as might be encountered on the Atlantic slope.
\nThe focus of the modeling effort was on the connection of a reasonable representation of physical fate to the biological responses of populations, rather than on highly detailed representations of individual processes. For example, the calculations of physical fate are not as detailed as those in the recently published model of Brandsma et al. (1983). The value of the model described herein is in the broad scope of processes that are explicitly represented and linked together. The model cannot be considered to produce reliable predictions of the quantitative impacts of discharged drilling fluids and cuttings on biological populations at a particular site. Limitations of the model in predicting integrated fate and effects can be traced to three general areas: level of refinement of the algorithms used in the model; lack of understanding of the processes determining fate and effects; and parameter and data values.
\nDespite the limitations, several qualitative conclusions concerning both potential impacts and the importance of various remaining data gaps can be drawn from the modeling effort. These include:
\n(1) Simple, unequivocal conclusions about fate and effects across geographical regions and drilling operations are difficult, if not misleading, due to the large amount of variability in characteristics of discharged materials (e.g., oil content and toxicity), discharge conditions (e.g., duration of drilling operations), physical environments (e.g., water depth, current direction, and sediment disturbance regimes), and biological communities (e.g., intrinsic growth rates). Different combinations of these characteristics can result in substantial differences in simulated environmental fate and biological effects. For examples, simulated recovery in some high-energy environments occurs within months after the cessation of discharge operations, even at heavily impacted sites, whereas simulated recover in some low-energy environments takes years at heavily impacted sites.
\n<2) Considerable difficulties remain in the reliable extrapolation of results from laboratory toxicity experiments to predictions of population effects in the field.
\n(3) The volume of material discharged and duration of operations in the production drilling operations simulated by the model are sufficient to produce substantial simulated biological impacts at some plots, both in terms of differences from a control plot during the period of discharge operations, and in terms of the recovery period following the perturbations.
\nEvaluation of the significance of potential effects involves the following factors:
\n• Definition of a specific spatial and temporal reference frame (e.g., What is the natural variation? Is 1 year to be considered a \"long\" or \"short\" time? Is 50 m to be considered a \"large\" or \"trivial\" distance?
\n• Consideration of rare or unique resources and particularly sensitive biotic assemblages.
\n• Consideration of the potential for long term, cumulative effects.
\nSome of these aspects are clearly beyond the scope of this modeling efforts (e.g., the model does not simulate the long term fate of resuspended material). The model does, however, contain an internal \"reference frame\" by comparison to simulated behavior at a control plot. The model, in general, simulates substantial \"natural\" variation at the reference or control plots, both over time, due to sediment disturbance events in medium to high energy environments, and over space, due to geographically varying conditions, such as water depth and current regime.
","language":"English","publisher":"U.S. Fish and Wildlife Service, Western Energy and Land Use Team","publisherLocation":"Fort Collins, CO","usgsCitation":"Auble, G.T., Andrews, A.K., Hamilton, D.B., Roelle, J.E., and Shoemaker, T.G., 1984, A workshop model simulating fate and effect of drilling muds and cuttings on benthic communities, 189 p.","productDescription":"189 p.","numberOfPages":"189","costCenters":[],"links":[{"id":292380,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53f25fc2e4b03334187188f7","contributors":{"authors":[{"text":"Auble, Gregor T. 0000-0002-0843-2751 aubleg@usgs.gov","orcid":"https://orcid.org/0000-0002-0843-2751","contributorId":2187,"corporation":false,"usgs":true,"family":"Auble","given":"Gregor","email":"aubleg@usgs.gov","middleInitial":"T.","affiliations":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"preferred":true,"id":498496,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Andrews, Austin K.","contributorId":85516,"corporation":false,"usgs":true,"family":"Andrews","given":"Austin","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":498499,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hamilton, David B. hamiltond@usgs.gov","contributorId":193,"corporation":false,"usgs":true,"family":"Hamilton","given":"David","email":"hamiltond@usgs.gov","middleInitial":"B.","affiliations":[],"preferred":true,"id":498495,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Roelle, James E. roelleb@usgs.gov","contributorId":2330,"corporation":false,"usgs":true,"family":"Roelle","given":"James","email":"roelleb@usgs.gov","middleInitial":"E.","affiliations":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"preferred":true,"id":498497,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Shoemaker, Thomas G.","contributorId":19491,"corporation":false,"usgs":true,"family":"Shoemaker","given":"Thomas","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":498498,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70207797,"text":"70207797 - 1984 - Middle Cretaceous black shales at Site 530 in the southeastern Angola Basin","interactions":[],"lastModifiedDate":"2020-06-24T14:26:20.080547","indexId":"70207797","displayToPublicDate":"1984-01-13T10:36:31","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1996,"text":"Initial Reports of the D.S.D.P.","active":true,"publicationSubtype":{"id":10}},"title":"Middle Cretaceous black shales at Site 530 in the southeastern Angola Basin","docAbstract":"The middle Cretaceous black shale interval at Site 530 is 170 m thick and late Albian to Coniacian in age. The organic-carbon-rich sediments occur as 260 separate beds (average 4 cm, maximum 60 cm thick) and make up less than 10% of the recovered section. Associated lithologies are greenish, grayish, and reddish mudstones, marlstones, and rare limestones. Organic-carbon contents of the black shales average about 5% (maximum 16%), and of the interbedded sediments, less than 0.5%. Careful study of the sedimentary and biogenic structures and composition and review of paleoceanographic conditions in the Angola Basin indicate that a complex interplay of processes controlled black shale accumulation. Relatively low oxygen concentrations in sediment and bottom waters occurred periodically, and conditions locally may have been anoxic or near anoxic both in the basin and on the continental margin. Pelagic, hemipelagic, and turbiditic depositional processes all operated to varying degrees at different times.
","language":"English","publisher":"Texas A&M D.S.D.P.","doi":"10.2973/dsdp.proc.75.120.1984","usgsCitation":"Stow, D., and Dean, W.E., 1984, Middle Cretaceous black shales at Site 530 in the southeastern Angola Basin: Initial Reports of the D.S.D.P., v. 75, no. 2, p. 809-817, https://doi.org/10.2973/dsdp.proc.75.120.1984.","productDescription":"9 p.","startPage":"809","endPage":"817","costCenters":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"links":[{"id":488865,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.2973/dsdp.proc.75.120.1984","text":"Publisher Index Page"},{"id":371186,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"otherGeospatial":"Drilling Site 530, 531, 532","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n 1.2744140625,\n -22.87744046489713\n ],\n [\n 14.5458984375,\n -22.87744046489713\n ],\n [\n 14.5458984375,\n -10.660607953624762\n ],\n [\n 1.2744140625,\n -10.660607953624762\n ],\n [\n 1.2744140625,\n -22.87744046489713\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"75","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Stow, D.A.","contributorId":44336,"corporation":false,"usgs":true,"family":"Stow","given":"D.A.","email":"","affiliations":[],"preferred":false,"id":779365,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dean, Walter E. dean@usgs.gov","contributorId":1801,"corporation":false,"usgs":true,"family":"Dean","given":"Walter","email":"dean@usgs.gov","middleInitial":"E.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"preferred":true,"id":779366,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":85492,"text":"85492 - 1984 - Species composition of fish communities in northern Wisconsin lakes: Relation to pH","interactions":[],"lastModifiedDate":"2012-02-02T00:15:15","indexId":"85492","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"title":"Species composition of fish communities in northern Wisconsin lakes: Relation to pH","docAbstract":"Fish communities in circumneutral Wisconsin lakes contained significantly more species than did those in acidic lakes (pH 5.1-6.0). Common, as well as rare, species occurred with lower frequency in acidic lakes than in circumneutral lakes. Certain taxa, such as minnows and darters, were either absent or rare in the acidic lakes, probably because of pH-related stress. The differences in species composition and richness of fish communities between acidic and circumneutral lakes did not appear to be related to differences in physical habitat characteristics, past fish migrations or productivity between the two lake groups.","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Early Biotic Responses to Advancing Lake Acidification. ACID-PRECIP.-SER. vol. 6","largerWorkSubtype":{"id":4,"text":"Other Government Series"},"language":"English","publisher":"Butterworth Publishers","publisherLocation":"Boston, MA","isbn":"0250405717","usgsCitation":"Wiener, J., Rago, P., and Eilers, J., 1984, Species composition of fish communities in northern Wisconsin lakes: Relation to pH, chap. of Early Biotic Responses to Advancing Lake Acidification. ACID-PRECIP.-SER. vol. 6, v. 6, 133-146.","productDescription":"133-146","costCenters":[{"id":606,"text":"Upper Midwest Environmental Sciences Center","active":true,"usgs":true}],"links":[{"id":200419,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"6","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e4e4b07f02db5e6292","contributors":{"editors":[{"text":"Hendrey, G.R.","contributorId":113957,"corporation":false,"usgs":true,"family":"Hendrey","given":"G.R.","email":"","affiliations":[],"preferred":false,"id":504521,"contributorType":{"id":2,"text":"Editors"},"rank":1}],"authors":[{"text":"Wiener, J.G.","contributorId":44107,"corporation":false,"usgs":true,"family":"Wiener","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":296069,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rago, P.J.","contributorId":50099,"corporation":false,"usgs":true,"family":"Rago","given":"P.J.","email":"","affiliations":[],"preferred":false,"id":296070,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Eilers, J.M.","contributorId":29103,"corporation":false,"usgs":true,"family":"Eilers","given":"J.M.","email":"","affiliations":[],"preferred":false,"id":296068,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70014030,"text":"70014030 - 1984 - Mineral resources of the Atlantic Exclusive Economic Zone","interactions":[],"lastModifiedDate":"2018-03-13T16:55:58","indexId":"70014030","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Mineral resources of the Atlantic Exclusive Economic Zone","docAbstract":"Potential mineral resources of the Atlantic Exclusive Economic Zone (including the Gulf of Mexico and US Caribbean areas) include petroleum, sand and gravel, phosphorite, placer deposits of heavy mineral sands, ferromanganese nodules, and fresh water. Although major efforts have been made to search for petroleum, the oil and gas resources of the region are well known only in the western Gulf Shelf and more exploration is under way. Heavy-mineral placer deposits, which may be sources of titanium, gold, rare earths, etc. , have been sampled, but the extent and, therefore, economic value of the deposits have not been identified. Sand and gravel, phosphorite, and ferromanganese nodules all are represented by fairly well established deposits, and only modified market conditions would be necessary to cause detailed exploration and mining.","largerWorkTitle":"Oceans Conference Record (IEEE)","conferenceTitle":"Oceans '84 Conference & Exposition, Conference Record: Industry, Government, Education, Designs for the Future.","conferenceLocation":"Washington, DC, USA","language":"English","publisher":"IEEE","publisherLocation":"New York, NY, USA","issn":"01977385","usgsCitation":"Dillon, W.P., 1984, Mineral resources of the Atlantic Exclusive Economic Zone, in Oceans Conference Record (IEEE), Washington, DC, USA, p. 431-437.","productDescription":"7 p.","startPage":"431","endPage":"437","costCenters":[],"links":[{"id":225995,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a4acbe4b0c8380cd6905b","contributors":{"authors":[{"text":"Dillon, William P. bdillon@usgs.gov","contributorId":79820,"corporation":false,"usgs":true,"family":"Dillon","given":"William","email":"bdillon@usgs.gov","middleInitial":"P.","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":367416,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012858,"text":"70012858 - 1984 - Sedimentary fluorite in a lacustrine zeolitic tuff of the Gila Conglomerate near Buckhorn, Grant County, New Mexico","interactions":[],"lastModifiedDate":"2024-05-21T23:31:22.564103","indexId":"70012858","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2450,"text":"Journal of Sedimentary Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Sedimentary fluorite in a lacustrine zeolitic tuff of the Gila Conglomerate near Buckhorn, Grant County, New Mexico","docAbstract":"Fluorite makes up 20-30% of a zeolitic tuff in a Pliocene or Pleistocene lacustrine facies of the Gila Conglomerate that has not been subjected to hydrothermal activity. The light gray zeolitic tuff is 40 cm thick and crops out over a 0.6-km 2 area about 2.5 km east of Buckhorn, New Mexico. This tuff is overlain by zeolitic mudstone that contains abundant and conspicuous Magadi-type chert. The fluorite occurs as prolate pellets and, rarely, as ooids that are mostly 0.14.3 mm in size. Broken pellets and ooids are extremely rare. Studies by X-ray diffraction and scanning electron microscopy show that the pellets and ooids consist mainly of submicrometer-size fluorite and quartz and that both minerals have poorly defined morphology. These pellets and ooids are embedded in a matrix that consists chiefly of micrometer-size mordenite and smectite and that has a vague vitroclastic texture. The pellets and ooids probably are the result of primary precipitation of fluorite and magadiite where dilute, calcium-bearing water from springs or streams mixed with the saline, alkaline lake water that had a high fluorine content. The pellets and ooids were then transported basinward and were incorporated with reworked vitric ash. During diagenesis, the magadiite of the pellets and ooids was converted to quartz, and the glass of the ash was altered to mordenite and smectite.
A sequential-scanning, inductively-coupled argon plasma emission spectrometer is used for the determination of the rare-earth elements, plus yttrium and scandium, in manganese nodules. Wavelength selection is optimized to minimize spectral interferences from manganese nodule components. Samples are decomposed with mixed acids in a sealed polycarbonate vessel, and elements are quantified without further treatment. Results for U.S. Geological Survey manganese nodule standards A-1 and P-1 had average relative standard deviations of 6.8% and 8.1%, respectively, and results were in good agreement with those obtained by other methods.
","language":"English","publisher":"Elsevier","doi":"10.1016/S0003-2670(00)84307-X","usgsCitation":"Fries, T.L., Lamothe, P.J., and Pesek, J.J., 1984, Determination of rare-earth elements, yttrium and scandium in manganese nodules by inductively-coupled argon-plastma emission spectrometry: Analytica Chimica Acta, v. 159, no. C, p. 329-336, https://doi.org/10.1016/S0003-2670(00)84307-X.","productDescription":"8 p.","startPage":"329","endPage":"336","numberOfPages":"8","costCenters":[],"links":[{"id":220129,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"159","issue":"C","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059ffc0e4b0c8380cd4f398","contributors":{"authors":[{"text":"Fries, Terry L.","contributorId":76349,"corporation":false,"usgs":true,"family":"Fries","given":"Terry","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":365439,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lamothe, Paul J","contributorId":118580,"corporation":false,"usgs":true,"family":"Lamothe","given":"Paul","email":"","middleInitial":"J","affiliations":[],"preferred":false,"id":365437,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pesek, J. J.","contributorId":78872,"corporation":false,"usgs":false,"family":"Pesek","given":"J.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":365438,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70013921,"text":"70013921 - 1984 - Laboratory studies of volcanic jets","interactions":[],"lastModifiedDate":"2024-06-27T16:07:41.067511","indexId":"70013921","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":6453,"text":"Journal of Geophysical Research Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Laboratory studies of volcanic jets","docAbstract":"The study of the fluid dynamics of violent volcanic eruptions by laboratory experiment is described, and the important fluid-dynamic processes that can be examined in laboratory models are discussed in detail. In preliminary experiments, pure gases are erupted from small reservoirs. The gases used are Freon 12 and Freon 22, two gases of high molecular weight and high density that are good analogs of heavy and particulate-laden volcanic gases; nitrogen, a moderate molecular weight, moderate density gas for which the thermodynamic properties are well known; and helium, a low molecular weight, lowdensity gas that is used as a basis for comparison with the behavior of the heavier gases and as an analog of steam, the gas that dominates many volcanic eruptions. Transient jets erupt from the reservoir into the laboratory upon rupture of a thin diaphragm at the exit of a convergent nozzle. The gas accelerates from rest in the reservoir to high velocity in the jet. Reservoir pressures and geometries are such that the fluid velocity in the jets is initially supersonic and later decays to subsonic. The measured reservoir pressure decreases as the fluid expands through repetitively reflecting rarefaction waves, but for the conditions of these experiments, a simple steady-discharge model is sufficient to explain the pressure decay and to predict the duration of the flow. Density variations in the flow field have been visualized with schlieren and shadowgraph photography. The observed structure of the jet is correlated with the measured pressure history. The starting vortex generated when the diaphragm ruptures becomes the head of the jet. Though the exit velocity is sonic, the flow head in the helium jet decelerates to about one-third of sonic velocity in the first few nozzle diameters, the nitrogen head decelerates to about three-fourths of sonic velocity, while Freon maintains nearly sonic velocity. The impulsive acceleration of reservoir fluid into the surrounding atmosphere produces a compression wave. The strength of this wave depends primarily on the sound speed of the fluid in the reservoir but also, secondarily with opposite effect, on the density: helium produces a relatively strong atmospheric shock while the Freons do not produce any optically observable wave front. Well-formed N waves are detected with a microphone far from the reservoir. Barrel shocks, Mach disks, and other familiar features of steady underexpanded supersonic jets form inside the jet almost immediately after passage of the flow head. These features are maintained until the pressure in the reservoir decays to sonic conditions. At low pressures the jets are relatively structureless. Gas-particle jets from volcanic eruptions may behave as pseudogases if particle concentrations and mass and momentum exchange between the components are sufficiently small. The sound speed of volcanic pseudogases can be as large as 1000 m s−1 or as small as a few tens of meters per second depending on the mass loading and initial temperature. Fluids of high sound speed produce stronger atmospheric shock waves than do those of low sound speed. Therefore eruption of a hot gas lightly laden with particulates should produce a stronger shock than eruption of a cooler or heavily laden fluid. An empirical expression suggests that the initial velocity of the head of supersonic volcanic jets is controlled by the sound speed and the ratio of the density of the erupting fluid to that of the atmosphere. The duration of gas or pseudogas eruptions is controlled by the sound speed of the fluid and the ratio of reservoir volume to vent area.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/JB089iB10p08253","issn":"01480227","usgsCitation":"Kieffer, S.W., and Sturtevant, B., 1984, Laboratory studies of volcanic jets: Journal of Geophysical Research Solid Earth, v. 89, no. B10, p. 8253-8268, https://doi.org/10.1029/JB089iB10p08253.","productDescription":"16 p.","startPage":"8253","endPage":"8268","numberOfPages":"16","costCenters":[],"links":[{"id":480209,"rank":2,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://resolver.caltech.edu/CaltechAUTHORS:20141029-163731844","text":"External Repository"},{"id":225286,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"89","issue":"B10","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","scienceBaseUri":"505a4118e4b0c8380cd652b9","contributors":{"authors":[{"text":"Kieffer, S. W.","contributorId":19186,"corporation":false,"usgs":true,"family":"Kieffer","given":"S.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":367168,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sturtevant, B.","contributorId":48318,"corporation":false,"usgs":true,"family":"Sturtevant","given":"B.","email":"","affiliations":[],"preferred":false,"id":367169,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70014010,"text":"70014010 - 1984 - The group separation of the rare-earth elements and yttrium from geologic materials by cation-exchange chromatography","interactions":[],"lastModifiedDate":"2013-01-21T08:43:04","indexId":"70014010","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1213,"text":"Chemical Geology","active":true,"publicationSubtype":{"id":10}},"title":"The group separation of the rare-earth elements and yttrium from geologic materials by cation-exchange chromatography","docAbstract":"Demand is increasing for the determination of the rare-earth elements (REE) and yttrium in geologic materials. Due to their low natural abundance in many materials and the interferences that occur in many methods of determination, a separation procedure utilizing gradient strong-acid cation-exchange chromatography is often used to preconcentrate and isolate these elements from the host-rock matrix. Two separate gradient strong-acid cation-exchange procedures were characterized and the major elements as well as those elements thought to provide the greatest interference for the determination of the REE in geologic materials were tested for separation from the REE. Simultaneous inductively coupled argon plasma-atomic emission spectroscopy (ICAP-AES) measurements were used to construct the chromatograms for the elution studies, allowing the elution patterns of all the elements of interest to be determined in a single fraction of eluent. As a rock matrix, U.S. Geological Survey standard reference BCR-1 basalt was digested using both an acid decomposition procedure and a lithium metaborate fusion. Hydrochloric and nitric acids were tested as eluents and chromatograms were plotted using the ICAP-AES data; and we observed substantial differences in the elution patterns of the REE and as well as in the solution patterns of Ba, Ca, Fe and Sr. The nitric acid elution required substantially less eluent to elute the REE and Y as a group when compared to the hydrochloric acid elution, and provided a clearer separation of the REE from interfering and matrix elements. ?? 1984.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Chemical Geology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Elsevier","doi":"10.1016/0009-2541(84)90121-9","issn":"00092541","usgsCitation":"Crock, J., Lichte, F., and Wildeman, T., 1984, The group separation of the rare-earth elements and yttrium from geologic materials by cation-exchange chromatography: Chemical Geology, v. 45, no. 1-2, p. 149-163, https://doi.org/10.1016/0009-2541(84)90121-9.","startPage":"149","endPage":"163","numberOfPages":"15","costCenters":[],"links":[{"id":266109,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/0009-2541(84)90121-9"},{"id":225677,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"45","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505baca7e4b08c986b32363e","contributors":{"authors":[{"text":"Crock, J.G.","contributorId":58236,"corporation":false,"usgs":true,"family":"Crock","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":367363,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lichte, F.E.","contributorId":99108,"corporation":false,"usgs":true,"family":"Lichte","given":"F.E.","affiliations":[],"preferred":false,"id":367364,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wildeman, T.R.","contributorId":30248,"corporation":false,"usgs":true,"family":"Wildeman","given":"T.R.","email":"","affiliations":[],"preferred":false,"id":367362,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70013341,"text":"70013341 - 1984 - Deformation, geochemistry, and origin of massive sulfide deposits, Gossan lead district, Virginia","interactions":[],"lastModifiedDate":"2024-01-08T23:55:15.12474","indexId":"70013341","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Deformation, geochemistry, and origin of massive sulfide deposits, Gossan lead district, Virginia","docAbstract":"The Gossan Lead district is a 28-km-long, northeast-trending belt of discontinuous massive sulfide deposits in the Blue Ridge province of southwestern Virginia. The deposits, hosted by the Ashe Formation of late Proterozoic age, consist of strata-bound lenses and layers of massive pyrrhotite, minor chalcopyrite, sphalerite, and pyrite, and rare arsenopyrite and galena. Deposits were mined principally in the Iron Ridge and Betty Baker segments, respectively, at the southwestern and northeastern ends of the belt. Detailed mapping of the Gossan Howard, Huey, and Bumbarger pits in the Iron Ridge segment indicates that the deposits occur at one horizon and have been variously folded and brecciated after sulfide deposition. The Gossan Howard consists of a single, gently dipping lens of sulfide. The Huey deposit is complexly folded and locally contains tectonically thickened ore. The Bumbarger deposit is a lens as much as 40 m thick--the thickest known in the district. This deposit contains abundant coarse breccia fragments of wall rock around which the massive sulfide has flowed (during deformation and metamorphism), probably thickening the original deposit significantly. In the northeastern part of the district, drill holes intersect several sulfide layers that possibly are structurally repeated.The Ashe Formation in the district is a sequence of metasedimentary rocks and local conformable lenses of amphibolite and actinolite-chlorite schist. The metasedimentary rocks include metapelite, quartz-feldspar granofels (metagraywacke), and minor quartzite and carbonaceous schist, and are interpreted as marine turbidites. The amphibolites and other mafic rocks have chemical compositions similar to low Ti tholeiitic basalt, with a high Y/Nb (>10) and high average contents of Co (40 ppm), Cr (403 ppm), Ni (211 ppm), and V (247 ppm). Immobile trace element signatures (Ti-Y-Zr; Th-Hf-Ta; Ti-Cr) suggest a magmatic affinity with midocean ridge basalt (MORB); rare earth elements (REE) have low abundance levels (10X-15X chondrite), broadly flat patterns [(La/Yb) N = 0.7-1.1], and a slight depletion in the light elements similar to midocean ridge basalts. An amphibolite from a much higher stratigraphic level, south of the district, differs significantly from the mafic rocks closer to the sulfide zone in having the chemical signature of a transitional, slightly alkalic tholeiite with high TiO 2 (3.87 wt %), Fe 2 O 3 (16.4 wt %), and P 2 O 5 (0.56 wt %), low Y/Nb (3.3), and a highly fractionated rare earth element distribution [(La/Yb) N = 3.9] similar to continental basalt.Some silicate wall rocks of the deposits are mineralogically and chemically unusual, and differ substantially from the clastic metasediments of the Ashe Formation. Such rocks are composed mainly or wholly of plagioclase feldspar, biotite, chlorite, muscovite, or spessartine-rich garnet. The unusual lithologies form local strata-bound lenses in the footwall and/or hanging wall of the deposits, typically within 10 m of massive sulfide. The plagioclase rocks (3.4-7.6 wt % Na 2 O) consist largely of granoblastic albite-oligoclase (Ab (sub 78-90) ) with minor quartz and biotite; rare earth elements are highly fractionated [(La/Yb) N = 6.8-7.1] and their patterns resemble those of the quartz-feldspar granofels (metagraywacke) from the district.The biotite schists, locally monomineralic, have FeO/(FeO + MgO) = 0.5 and contain high phosphorus (1 wt % P 2 O 5 ) and fluorine (0.5 wt % F), present in fluorapatite. The chlorite schist is essentially all ripidolite; rare earth elements are highly fractionated, and have a large negative Eu anomaly. The spessartine-rich rocks (6.3-8.9 wt % MnO) are in places interlayered with the other unusual wall rocks and consist of abundant Mn-rich garnet (Sp 50 Al 23 Gr 19 Py 8 ) and minor quartz, plagioclase, pyrrhotite, and biotite. The distinctive mineralogy and chemistry of these rocks suggest that they represent metamorphosed alteration zones and/or intermixed chemical and clastic sediments.The sulfide deposits are interpreted as syngenetic in origin but modified in form by deformation which accompanied metamorphism. The great length of the mineralized district parallel to the regional strike and the flyschoid (turbidite) nature of the host rocks suggest that sedimentation and initial sulfide deposition took place in a deep, elongate marine basin or graben overlying a crustal rift zone. A rift underlying the sedimentary pile is consistent with the occurrence of mafic metavolcanic rocks of midocean ridge basalt affinity and could also have served as the feeder system for a line of hydrothermal vents on the sea floor that generated the sulfide deposits.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.79.7.1483","issn":"03610128","usgsCitation":"Gair, J., and Slack, J.F., 1984, Deformation, geochemistry, and origin of massive sulfide deposits, Gossan lead district, Virginia: Economic Geology, v. 79, no. 7, p. 1483-1520, https://doi.org/10.2113/gsecongeo.79.7.1483.","productDescription":"38 p.","startPage":"1483","endPage":"1520","numberOfPages":"38","costCenters":[],"links":[{"id":219973,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"79","issue":"7","noUsgsAuthors":false,"publicationDate":"1984-11-01","publicationStatus":"PW","scienceBaseUri":"5059fe4de4b0c8380cd4ec63","contributors":{"authors":[{"text":"Gair, J. E.","contributorId":50891,"corporation":false,"usgs":true,"family":"Gair","given":"J. E.","affiliations":[],"preferred":false,"id":365846,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Slack, J. F.","contributorId":75917,"corporation":false,"usgs":true,"family":"Slack","given":"J.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":365847,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70013920,"text":"70013920 - 1984 - Determination of carrier yields for neutron activation analysis using energy dispersive X-ray spectrometry","interactions":[],"lastModifiedDate":"2012-03-12T17:19:29","indexId":"70013920","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2440,"text":"Journal of Radioanalytical and Nuclear Chemistry Articles","active":true,"publicationSubtype":{"id":10}},"title":"Determination of carrier yields for neutron activation analysis using energy dispersive X-ray spectrometry","docAbstract":"A new method is described for determining carrier yield in the radiochemical neutron activation analysis of rare-earth elements in silicate rocks by group separation. The method involves the determination of the rare-earth elements present in the carrier by means of energy-dispersive X-ray fluorescence analysis, eliminating the need to re-irradiate samples in a nuclear reactor after the gamma ray analysis is complete. Results from the analysis of USGS standards AGV-1 and BCR-1 compare favorably with those obtained using the conventional method. ?? 1984 Akade??miai Kiado??.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Journal of Radioanalytical and Nuclear Chemistry Articles","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisherLocation":"Kluwer Academic Publishers","doi":"10.1007/BF02132917","issn":"02365731","usgsCitation":"Johnson, R.G., and Wandless, G., 1984, Determination of carrier yields for neutron activation analysis using energy dispersive X-ray spectrometry: Journal of Radioanalytical and Nuclear Chemistry Articles, v. 81, no. 1, p. 21-28, https://doi.org/10.1007/BF02132917.","startPage":"21","endPage":"28","numberOfPages":"8","costCenters":[],"links":[{"id":205617,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF02132917"},{"id":225285,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"81","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059ff9ae4b0c8380cd4f2a0","contributors":{"authors":[{"text":"Johnson, R. G.","contributorId":39350,"corporation":false,"usgs":true,"family":"Johnson","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":367166,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wandless, G.A.","contributorId":107716,"corporation":false,"usgs":true,"family":"Wandless","given":"G.A.","affiliations":[],"preferred":false,"id":367167,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70013958,"text":"70013958 - 1984 - Nivation landforms in the western Great Basin and their paleoclimatic significance","interactions":[],"lastModifiedDate":"2013-01-26T15:43:35","indexId":"70013958","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3218,"text":"Quaternary Research","active":true,"publicationSubtype":{"id":10}},"title":"Nivation landforms in the western Great Basin and their paleoclimatic significance","docAbstract":"More than 10,000 nivation landforms occur in the higher mountain ranges of the western Great Basin. They range from small, subtle hollows with head scarps a few meters high and a few tens of meters long to broad, clearly defined terraces as much as 220 m wide bounded by bold, steeply sloping head scarps as much as 30 m high and 1600 m long. Distribution of these nivation hollows is strongly influenced by elevation, slope orientation, local relief, and substrate lithology. About 95% occur between 2200 and 3000 m elevation, and nearly 80% are situated on north-northwest-to east-northeast-facing slopes. They occur mainly in areas of moderately sloping terrain and moderate local relief, and they are preferentially developed on relatively incompetent substrates including terrigenous sedimentary deposits, volcanic and metavolcanic rocks of intermediate composition, and deeply weathered granitoid rocks. Nearly all of these nivation hollows are relict. They are most abundant near areas of late Pleistocene glaciation but rarely occur within such areas. Most are veneered with colluvium and are well vegetated, and many hollows in the Mono Basin area are veneered with volcanic ash at least 700 yr old. Distribution of nivation hollows suggests that (1) the full-glacial nivation threshold altitude (NTA) rose from north to south at 190 m per degree of latitude, subparallel to, and approximately 740 m lower than, the full-glacial equilibrium-line altitude (ELA) and about 1370 m lower than the estimated modern ELA; (2) the difference between the full-glacial and modern ELAs indicates an approximate 7??C full-glacial mean-annual-temperature depression throughout the Great Basin; and (3) the full-glacial mean annual temperature at the NTA is estimated to have been approximately 0?? to 1??C, assuming little change in accumulation-season precipitation. ?? 1984.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Quaternary Research","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Elsevier","publisherLocation":"Amsterdam, Netherlands","doi":"10.1016/0033-5894(84)90022-X","issn":"00335894","usgsCitation":"Dohrenwend, J.C., 1984, Nivation landforms in the western Great Basin and their paleoclimatic significance: Quaternary Research, v. 22, no. 3, p. 275-288, https://doi.org/10.1016/0033-5894(84)90022-X.","startPage":"275","endPage":"288","numberOfPages":"14","costCenters":[],"links":[{"id":266552,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/0033-5894(84)90022-X"},{"id":225926,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"22","issue":"3","noUsgsAuthors":false,"publicationDate":"2017-01-20","publicationStatus":"PW","scienceBaseUri":"505a6706e4b0c8380cd7312c","contributors":{"authors":[{"text":"Dohrenwend, J. C.","contributorId":40960,"corporation":false,"usgs":true,"family":"Dohrenwend","given":"J.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":367250,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1007752,"text":"1007752 - 1984 - Post-fire recovery of California coastal sage scrub","interactions":[],"lastModifiedDate":"2023-02-15T15:29:56.003181","indexId":"1007752","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":737,"text":"American Midland Naturalist","active":true,"publicationSubtype":{"id":10}},"title":"Post-fire recovery of California coastal sage scrub","docAbstract":"Postfire regeneration of the shrub and herb vegetation on eight coastal slopes of California coastal sage scrub was studied in the first two growing seasons after fire. All shrub species resprouted with the exception of the suffrutescent Lotus scoparius, though it is not known if this species was alive prior to the fire. It was estimated that 70% of the prefire shrub populations resprouted and these sprouts covered one third of the ground surface by the end of the second season. In contrast to chaparral, seedling establishment from soil-stored seed was low (∼ 102-103/ha) in the 1st postfire year. Resprouts of most major species (Artemisia californica, Encelia californica, Haplopappus squarrosus, Eriogonum cinereum) flowered and set seed in the 1st year. Seedling densities were ∼ 104-106/ha in the 2nd year. Herbs dominated the first postfire season vegetation in number of species, cover and biomass. The magnitude of the postfire herb flora was comparable to that in chaparral after fire and included many of the same species. On several slopes, \"pyrophyte endemic\" annuals (Lupinus succulentus, Lotus salsuginosus, Phacelia parryi) dominated the first season and were rare or absent in the 2nd year. One major distinction between these coastal sage sites and chaparral was that resprouting perennial herbs dominated some slopes in the first postfire season and most slopes in the second season in coastal sage. Seedling recruitment of perennial herbs was rare; 26 of the 28 species were present only as resprouts. Total herb cover was markedly lower in the 2nd year despite the fact that it was a wetter year. Between the 1st and 2nd years, shrub cover ∼ doubled, largely from resprouts, annual herb cover declined markedly and perennial herb cover remained relatively constant. The perennial bunchgrass Stipa lepida was an important component of the herb flora on all slopes and was the only species (herb or shrub) to exceed 1/m2 on all eight slopes.
","language":"English","publisher":"University of Notre Dame","doi":"10.2307/2425548","usgsCitation":"Keeley, J.E., and Keeley, S.C., 1984, Post-fire recovery of California coastal sage scrub: American Midland Naturalist, v. 111, p. 105-117, https://doi.org/10.2307/2425548.","productDescription":"13 p.","startPage":"105","endPage":"117","numberOfPages":"13","costCenters":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"links":[{"id":130185,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Santa Monica Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -119.15076393254975,\n 34.2720286815771\n ],\n [\n -119.15076393254975,\n 33.98965067077958\n ],\n [\n -118.12202439621663,\n 33.98965067077958\n ],\n [\n -118.12202439621663,\n 34.2720286815771\n ],\n [\n -119.15076393254975,\n 34.2720286815771\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"111","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db683a7e","contributors":{"authors":[{"text":"Keeley, Jon E. 0000-0002-4564-6521 jon_keeley@usgs.gov","orcid":"https://orcid.org/0000-0002-4564-6521","contributorId":1268,"corporation":false,"usgs":true,"family":"Keeley","given":"Jon","email":"jon_keeley@usgs.gov","middleInitial":"E.","affiliations":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"preferred":true,"id":315968,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Keeley, Sterling C.","contributorId":112968,"corporation":false,"usgs":true,"family":"Keeley","given":"Sterling","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":315967,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70013910,"text":"70013910 - 1984 - Seismicity at Old Faithful Geyser: an isolated source of geothermal noise and possible analogue of volcanic seismicity","interactions":[],"lastModifiedDate":"2012-03-12T17:19:33","indexId":"70013910","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","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":"Seismicity at Old Faithful Geyser: an isolated source of geothermal noise and possible analogue of volcanic seismicity","docAbstract":"Old Faithful Geyser in Yellowstone National Park, U.S.A., is a relatively isolated source of seismic noise and exhibits seismic behavior similar to that observed at many volcanoes, including \"bubblequakes\" that resemble B-type \"earthquakes\", harmonic tremor before and during eruptions, and periods of seismic quiet prior to eruptions. Although Old Faithful differs from volcanoes in that the conduit is continuously open, that rock-fracturing is not a process responsible for seismicity, and that the erupting fluid is inviscid H2O rather than viscous magma, there are also remarkable similarities in the problems of heat and mass recharge to the system, in the eruption dynamics, and in the seismicity. Water rises irregularly into the immediate reservoir of Old Faithful as recharge occurs, a fact that suggests that there are two enlarged storage regions: one between 18 and 22 m (the base of the immediate reservoir) and one between about 10 and 12 m depth. Transport of heat from hot water or steam entering at the base of the recharging water column into cooler overlying water occurs by migration of steam bubbles upward and their collapse in the cooler water, and by episodes of convective overturn. An eruption occurs when the temperature of the near-surface water exceeds the boiling point if the entire water column is sufficiently close to the boiling curve that the propagation of pressure-release waves (rarefactions) down the column can bring the liquid water onto the boiling curve. The process of conversion of the liquid water in the conduit at the onset of an eruption into a two-phase liquid-vapor mixture takes on the order of 30 s. The seismicity is directly related to the sequence of filling and heating during the recharge cycle, and to the fluid mechanics of the eruption. Short (0.2-0.3 s), monochromatic, high-frequency events (20-60 Hz) resembling unsustained harmonic tremor and, in some instances, B-type volcanic earthquakes, occur when exploding or imploding bubbles of steam cause transient vibrations of the fluid column. The frequency of the events is determined by the length of the water column and the speed of sound of the fluid in the conduit when these events occur; damping is controlled by the characteristic and hydraulic impedances, which depend on the above parameters, as well as on the recharge rate of the fluid. Two periods of reduced seismicity (of a few tens of seconds to nearly a minute in duration) occur during the recharge cycle, apparently when the water rises rapidly through the narrow regions of the conduit, causing a sudden pressure increase that temporarily suppresses steam bubble formation. A period of decreased seismicity also precedes preplay or an eruption; this appears to be the time when rising steam bubbles move into a zone of boiling that is acoustically decoupled from the wall of the conduit because of the acoustic impedance mismatch between boiling water (??c ??? 103 g cm-2 s-1) and rock (??c ??? 3 ?? 105 g cm2 s-1). Sustained harmonic tremor occurs during the first one to one-and-a-half minutes of an eruption of Old Faithful, but is not detectable in the succeeding minutes of the eruption. The eruption tremor is caused by hydraulic transients propagating within a sublayer of unvesiculated water that underlies the erupting two-phase liquid-vapor mixture. The resonant frequencies of the fluid column decrease to about 1 Hz when all of the water in the conduit has been converted to a water-steam mixture. Surges are observed in the flow at this frequency, but the resonance has not been detected seismically, possibly because the two-phase erupting fluid is seismically decoupled from the rock on which seismometers are placed. If Old Faithful is an analogue for volcanic seismicity, this study shows that because the frequency of tremor depends on the acoustic properties of the fluid and on conduit dimensions, both properties must be considered in analysis of tremor in volcanic regions. Because magma sound","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Journal of Volcanology and Geothermal Research","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","issn":"03770273","usgsCitation":"Kieffer, S.W., 1984, Seismicity at Old Faithful Geyser: an isolated source of geothermal noise and possible analogue of volcanic seismicity: Journal of Volcanology and Geothermal Research, v. 22, no. 1-2, p. 59-95.","startPage":"59","endPage":"95","numberOfPages":"37","costCenters":[],"links":[{"id":226119,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"22","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b8b93e4b08c986b31793c","contributors":{"authors":[{"text":"Kieffer, S. W.","contributorId":19186,"corporation":false,"usgs":true,"family":"Kieffer","given":"S.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":367147,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70013969,"text":"70013969 - 1984 - Straczekite, a new calcium barium potassium vanadate mineral from Wilson Springs, Arkansas","interactions":[],"lastModifiedDate":"2019-11-05T07:57:54","indexId":"70013969","displayToPublicDate":"1984-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2748,"text":"Mineralogical Magazine","active":true,"publicationSubtype":{"id":10}},"title":"Straczekite, a new calcium barium potassium vanadate mineral from Wilson Springs, Arkansas","docAbstract":"Straczekite occurs as a rare secondary mineral in fibrous seams, along with other V minerals (A.M. 64-713), in ore from the vanadium mine in Wilson Springs (formerly Potash Sulfur Springs), Garland County, Arkansas. It forms soft, thin laths of dark greenish black crystals up to 0.5 mm in length. Indexed XRD data are tabulated; strongest lines 3.486(100), 10.449(50), 1.8306(50), 1.9437(15) A; a 11.679, b 3.6608, c 10.636 A, beta 100.53o; space group C2/m, C2 or Cm. Chemical analysis gave V2O5 66.4, V2O4 15.3, Fe2O3 0.9, Na2O 0.4, K2O 1.8, CaO 2.5, BaO 5.5, H2O 7.2, = 100.0, leading to the formula (Ca0.39Ba0.31K0.33Na0.11)- 196(V4+1.59V5+6.31Fe3+0.10)O20.02(H2O)2.9; Dcalc. 3.21 g/cm3. A possible layer structure is discussed. The name is for J. A. Straczek, Chief Geologist at Union Carbide Corp.-R.A.H.","language":"English","publisher":"Cambridge University Press","doi":"10.1180/minmag.1984.048.347.16","issn":"0026461X","usgsCitation":"Evans, H.T., Nord, G., Marinenko, J., and Milton, C., 1984, Straczekite, a new calcium barium potassium vanadate mineral from Wilson Springs, Arkansas: Mineralogical Magazine, v. 48, no. 2, p. 289-293, https://doi.org/10.1180/minmag.1984.048.347.16.","productDescription":"5 p.","startPage":"289","endPage":"293","numberOfPages":"5","costCenters":[],"links":[{"id":226122,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arkansas","county":"Garland County ","city":"Wilson Springs","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.53485107421875,\n 36.146746777814364\n ],\n [\n -92.449951171875,\n 36.146746777814364\n ],\n [\n -92.449951171875,\n 36.4433803110554\n ],\n [\n -93.53485107421875,\n 36.4433803110554\n ],\n [\n -93.53485107421875,\n 36.146746777814364\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"48","issue":"2","noUsgsAuthors":false,"publicationDate":"2018-07-05","publicationStatus":"PW","scienceBaseUri":"505b988ce4b08c986b31c08f","contributors":{"authors":[{"text":"Evans, H. T. Jr.","contributorId":41859,"corporation":false,"usgs":true,"family":"Evans","given":"H.","suffix":"Jr.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":367277,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nord, G.","contributorId":7854,"corporation":false,"usgs":true,"family":"Nord","given":"G.","email":"","affiliations":[],"preferred":false,"id":367275,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Marinenko, J.","contributorId":104221,"corporation":false,"usgs":true,"family":"Marinenko","given":"J.","email":"","affiliations":[],"preferred":false,"id":367278,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Milton, C.","contributorId":37472,"corporation":false,"usgs":true,"family":"Milton","given":"C.","affiliations":[],"preferred":false,"id":367276,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ]}