Electrophoretic differences at 15 presumptive loci were used to assess allelic frequencies, heterozygosities, and polymorphism for male Yellow-headed Blackbirds (Xanthocephalus xanthocephalus) collected in east-central Alberta, north-central North Dakota, and east-central South Dakota. Five loci were polymorphic and mean heterozygosities ranged from 0.119 to 0.133. Significant differences were detected among these geographic populations of Yellow-headed Blackbirds, primarily due to differences in the allelic frequencies of isocitrate dehydrogenase and glucose-6-phosphate dehydrogenase. Differences detected were not sufficient to uniquely identify the geographic origin of Yellow-headed Blackbrids.
","language":"English","publisher":"Canadian Science Publishing","doi":"10.1139/z92-305","usgsCitation":"Twedt, D.J., Bleier, W.J., and Linz, G.M., 1992, Genetic variation in male Yellow-headed Blackbirds from the northern Great Plains: Canadian Journal of Zoology, v. 70, no. 11, p. 2280-2282, https://doi.org/10.1139/z92-305.","productDescription":"3 p.","startPage":"2280","endPage":"2282","costCenters":[{"id":455,"text":"National Wetlands Research Center","active":true,"usgs":true}],"links":[{"id":362889,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada, United States","volume":"70","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Twedt, Daniel J. 0000-0003-1223-5045 dtwedt@usgs.gov","orcid":"https://orcid.org/0000-0003-1223-5045","contributorId":398,"corporation":false,"usgs":true,"family":"Twedt","given":"Daniel","email":"dtwedt@usgs.gov","middleInitial":"J.","affiliations":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"preferred":true,"id":760734,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bleier, William J.","contributorId":66833,"corporation":false,"usgs":true,"family":"Bleier","given":"William","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":760735,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Linz, George M.","contributorId":32859,"corporation":false,"usgs":true,"family":"Linz","given":"George","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":760736,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70127577,"text":"70127577 - 1992 - Distribution of Yellowstone grizzly bears during the 1980s","interactions":[],"lastModifiedDate":"2023-02-14T16:57:08.018739","indexId":"70127577","displayToPublicDate":"1992-01-01T11:48:00","publicationYear":"1992","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":"Distribution of Yellowstone grizzly bears during the 1980s","docAbstract":"Grizzly bear (Ursus arctos horribilis) females with young occupied a greater proportion of area east of Yellowstone National Park during 1980-1989 compared to 1973-1979. Occupancy by all bears and females with young was lower in all peripheral areas compared to the Park, but greater east and south compared to north and south of the Park. Observed changes reflect not only a static or slightly increasing population trend, but may also reflect biases in data collection. These biases are discussed and distributions of all observations and females with young are presented. Methodological problems implicit in analyzing changes in distribution of grizzly bears are also discussed.
","language":"English","publisher":"University of Notre Dame","doi":"10.2307/2426467","usgsCitation":"Blanchard, B.M., Knight, R.R., and Mattson, D.J., 1992, Distribution of Yellowstone grizzly bears during the 1980s: American Midland Naturalist, v. 128, p. 332-335, https://doi.org/10.2307/2426467.","productDescription":"4 p.","startPage":"332","endPage":"335","numberOfPages":"4","costCenters":[],"links":[{"id":294643,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Idaho, Montana, Wyoming","otherGeospatial":"Yellowstone National Park","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -111.156,44.1324 ], [ -111.156,45.109 ], [ -109.8242,45.109 ], [ -109.8242,44.1324 ], [ -111.156,44.1324 ] ] ] } } ] }","volume":"128","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"542bc62de4b0abfb4c8097a3","contributors":{"authors":[{"text":"Blanchard, Bonnie M.","contributorId":33633,"corporation":false,"usgs":true,"family":"Blanchard","given":"Bonnie","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":502443,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Knight, Richard R.","contributorId":68660,"corporation":false,"usgs":true,"family":"Knight","given":"Richard","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":502445,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mattson, David J.","contributorId":191920,"corporation":false,"usgs":false,"family":"Mattson","given":"David","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":502444,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70243350,"text":"70243350 - 1992 - Source region of a granite batholith: Evidence from lower crustal xenoliths and inherited accessory minerals","interactions":[],"lastModifiedDate":"2023-05-09T15:29:36.780462","indexId":"70243350","displayToPublicDate":"1992-01-01T10:14:37","publicationYear":"1992","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5770,"text":"Earth and Environmental Science Transactions of The Royal Society of Edinburgh","active":true,"publicationSubtype":{"id":10}},"title":"Source region of a granite batholith: Evidence from lower crustal xenoliths and inherited accessory minerals","docAbstract":"Like many granites, the Late Cretaceous intrusives of the eastern Mojave Desert, California, have heretofore provided useful but poorly focused images of their source regions. New studies of lower crustal xenoliths and inherited accessory minerals are sharpening these images.
Xenoliths in Tertiary dykes in this region are the residues of an extensive partial melting event. Great diversity in their composition reflects initial heterogeneity (both igneous and sedimentary protoliths) and varying amounts of melt extraction (from <10% to >70%). Mineral assemblages and thermobarometry suggest that the melting event occurred at T ≥ 750°C at a depth of about 40 km. Present-day Sr, Nd, and Pb isotopic ratios indicate a Mojave Proterozoic heritage, but unrealistic model ages demonstrate the late Phanerozoic adjustment of parent/daughter ratios. A link between these xenoliths and the Late Cretaceous granites, though not fully documented, is probable; in any case, they provide invaluable clues concerning a crustal melting event, recording information about nature of source material (heterogeneous, supracrustal-rich), conditions of melting (moderately deep, moderately high T, accompanied by partial dehydration), and melt extraction (highly variable, locally extensive).
The Old Woman-Piute granites contain a large fraction of inherited zircon and monazite. A SHRIMP ion probe investigation shows that these zircons record a Proterozoic history similar to that which affected the Mojave region. Zonation patterns in zircons, and to a lesser extent monazites and xenotimes, document multiple phases of igneous, metamorphic, and sedimentary growth and degradation, commonly several in a single grain. Low Y in portions of the cores of inherited zircons and monazites and in monazites and outer portions of zircons from the xenoliths appear to indicate growth in equilibrium with abundant garnet.
","language":"English","publisher":"Cambridge University Press","doi":"10.1017/S0263593300007744","usgsCitation":"Miller, C., Hanchar, J.M., Wooden, J., Bennett, V.C., Harrison, T.M., Wark, D.A., and Foster, D.A., 1992, Source region of a granite batholith: Evidence from lower crustal xenoliths and inherited accessory minerals: Earth and Environmental Science Transactions of The Royal Society of Edinburgh, v. 83, no. 1-2, p. 49-62, https://doi.org/10.1017/S0263593300007744.","productDescription":"14 p.","startPage":"49","endPage":"62","costCenters":[],"links":[{"id":416862,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Mojave Desert","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -118.83356467988116,\n 34.8279676819143\n ],\n [\n -118.04513335337579,\n 34.41775123340372\n ],\n [\n -117.68170986448735,\n 34.37161513150107\n ],\n [\n -117.45255654829927,\n 34.25689606372363\n ],\n [\n -116.78161975031,\n 34.173673842669956\n ],\n [\n -116.06036390313116,\n 33.75633064149888\n ],\n [\n -115.67457589184934,\n 33.76097902741604\n ],\n [\n -115.08750717902925,\n 33.467639120929206\n ],\n [\n -114.46689168261973,\n 33.714483827633686\n ],\n [\n -114.50602959680751,\n 33.830674557637394\n ],\n [\n -114.47807394381609,\n 33.872464627919\n ],\n [\n -114.50602959680751,\n 33.95598340376327\n ],\n [\n -114.39979811544019,\n 34.016251590137855\n ],\n [\n -114.39420698484184,\n 34.090369120879245\n ],\n [\n -114.25442871988476,\n 34.14591472525245\n ],\n [\n -114.10346819373096,\n 34.25227509432112\n ],\n [\n -114.1481972385171,\n 34.349269472593306\n ],\n [\n -114.3215222870643,\n 34.464592814087354\n ],\n [\n -114.37184246244878,\n 34.48763839822264\n ],\n [\n -114.36625133185042,\n 34.53831627224551\n ],\n [\n -114.43893602962831,\n 34.67177373090276\n ],\n [\n -114.47248281321775,\n 34.736124658560016\n ],\n [\n -114.55075864159399,\n 34.78665097545071\n ],\n [\n -114.56753203338869,\n 34.83714635899972\n ],\n [\n -114.62344333937153,\n 34.89219692881092\n ],\n [\n -114.64021673116657,\n 35.00676718739375\n ],\n [\n -115.99886146654998,\n 36.084901936918754\n ],\n [\n -116.45174304501134,\n 35.89942757249506\n ],\n [\n -116.62506809355821,\n 36.02161826416021\n ],\n [\n -116.99967384364332,\n 35.98543332595766\n ],\n [\n -117.49169333629246,\n 35.86771765454857\n ],\n [\n -117.84393456398453,\n 36.301487877656825\n ],\n [\n -118.05639752671951,\n 36.21582758206627\n ],\n [\n -117.9557571759502,\n 35.67264984719334\n ],\n [\n -118.15144674689012,\n 35.59539813627521\n ],\n [\n -118.12908222449705,\n 35.28564569120178\n ],\n [\n -118.28004275065084,\n 35.14861175210852\n ],\n [\n -118.83356467988116,\n 34.8279676819143\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"83","issue":"1-2","noUsgsAuthors":false,"publicationDate":"2011-11-03","publicationStatus":"PW","contributors":{"authors":[{"text":"Miller, Calvin F.","contributorId":18437,"corporation":false,"usgs":true,"family":"Miller","given":"Calvin F.","affiliations":[],"preferred":false,"id":872127,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hanchar, John M.","contributorId":190636,"corporation":false,"usgs":false,"family":"Hanchar","given":"John","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":872128,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wooden, Joseph L.","contributorId":32209,"corporation":false,"usgs":true,"family":"Wooden","given":"Joseph L.","affiliations":[],"preferred":false,"id":872129,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bennett, Victoria C.","contributorId":190637,"corporation":false,"usgs":false,"family":"Bennett","given":"Victoria","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":872130,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Harrison, T. Mark","contributorId":304921,"corporation":false,"usgs":false,"family":"Harrison","given":"T.","email":"","middleInitial":"Mark","affiliations":[],"preferred":false,"id":872131,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Wark, David A.","contributorId":304922,"corporation":false,"usgs":false,"family":"Wark","given":"David","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":872132,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Foster, David A.","contributorId":304923,"corporation":false,"usgs":false,"family":"Foster","given":"David","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":872133,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":70017104,"text":"70017104 - 1992 - Widespread buried Precambrian layered sequences in the U.S. mid- continent: Evidence for large Proterozoic depositional basins","interactions":[],"lastModifiedDate":"2023-01-19T17:30:17.436221","indexId":"70017104","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","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":"Widespread buried Precambrian layered sequences in the U.S. mid- continent: Evidence for large Proterozoic depositional basins","docAbstract":"Large regions of the North American mid-continent are underlain by Precambrian layered rocks buried beneath Phanerozoic sedimentary strata. South of the Wichita Mountains, published seismic reflection profiles show a Precambrian layered assemblage extending for at least 40 km in both the north-south and east-west directions, and industry data show that it may continue 150 km to the southeast. Seismic reflection data in the Illinois region show a Precambrian layered assemblage extending 320 km in an east-west direction and 200 km in a north-south direction. In both cases, the layered rocks are as much as 12 km thick. Apparent sequence boundaries (onlap, downlap) within these assemblages suggest they are parts of large depositional basins with diffractions and dipping strat due to faulting. The layered sequences correlate with regions of relatively long-wavelength and low-amplitude magnetic anomalies; the extent of this magnetic signature suggests that about 200,000 km{2} of Illinois, Indiana, and western Ohio, about 50,000 km{2} of southernmost Oklahoma and north-central Texas, and about 32,000 km{2} of southern Missouri and northern Arkansas may be underlain by similar Precambrian strata.
Drill holes indicate that the top of the mid-continent Precambrian \"basement\" is composed largely of silicic igneous rocks. Such material may comprise a large part of the layered sequences. Alternatively, these igneous rocks could be intermixed with, or underlain by, nonvolcanic (meta?)sedimentary strata. The strong reflectivity of some layers suggest that minor mafic flows and/or sills may also be present. Analysis of U/Pb and Nd/Sm isotopes within the granites and rhyolites imply that the layered sequences postdate crustal formation at 1.7-2.0 Ga and predate or are contemporaneous with the 1.3-1.5 Ga crystallization ages of the granites and rhyolites. Though these layered rocks have a spatial association with igneous rocks and thus have likely been metamorphosed, the possibility tha they contain Precambrian hydrocarbons that escaped heating is as yet untested.
","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/BDFF89FC-1718-11D7-8645000102C1865D","usgsCitation":"Pratt, T.L., Hauser, E., and Nelson, K.D., 1992, Widespread buried Precambrian layered sequences in the U.S. mid- continent: Evidence for large Proterozoic depositional basins: American Association of Petroleum Geologists Bulletin, v. 76, no. 9, p. 1384-1401, https://doi.org/10.1306/BDFF89FC-1718-11D7-8645000102C1865D.","productDescription":"16 p.","startPage":"1384","endPage":"1401","numberOfPages":"18","costCenters":[],"links":[{"id":224818,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Mid-continent region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -82,\n 44\n ],\n [\n -105,\n 44\n ],\n [\n -105,\n 31\n ],\n [\n -82,\n 31\n ],\n [\n -82,\n 44\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"76","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bd0afe4b08c986b32efd4","contributors":{"authors":[{"text":"Pratt, T. L.","contributorId":53072,"corporation":false,"usgs":true,"family":"Pratt","given":"T.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":375420,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hauser, E.C.","contributorId":41150,"corporation":false,"usgs":true,"family":"Hauser","given":"E.C.","email":"","affiliations":[],"preferred":false,"id":375419,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Nelson, Kim","contributorId":92810,"corporation":false,"usgs":false,"family":"Nelson","given":"Kim","affiliations":[],"preferred":false,"id":375421,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70017141,"text":"70017141 - 1992 - Mapping thermal maturity in the Chainman shale, near Eureka, Nevada, with Landsat Thematic Mapper images","interactions":[],"lastModifiedDate":"2023-01-19T17:40:10.222065","indexId":"70017141","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","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":"Mapping thermal maturity in the Chainman shale, near Eureka, Nevada, with Landsat Thematic Mapper images","docAbstract":"The purpose of this study was to determine if there is a correlation between measurements of organic matter (OM) maturity and laboratory measurements of visible and near-infrared spectral reflectance, and if Landsat Thematic Mapper (TM) images could be used to map maturity. The maturity of Mississippian Chainman Shale samples collected in east-central Nevada and west-central Utah was determined by using vitrinite reflectance and Rock-Eval pyrolysis. To establish the relations between maturity and spectral reflectance in the visible and near-infrared (VNIR) wavelength region, VNIR reflectance spectra of fresh and weathered whole-rock sample surfaces were measured in the laboratory. The spectra were convolved digitally with the Landsat TM filter band passes to facilitate th analysis, especially the relative sensitivities of individual band passes and ratios of band passes to spectral reflectance variations related to OM maturity.
With increasing maturity, overall VNIR diffuse reflectance and mineral-absorption-feature intensities decrease, and the shape of the spectra changes from concave-downward to nearly flat. The spectral shape differences between mature and supermature samples remains distinctive in reflectance spectra of weathered surfaces. TM 4/TM 5 values correspond well to vitrinite reflectance and hydrogen index variations, and therefore this ratio was used to evaluate a TM image of the Eureka, Nevada, area for mapping thermal maturity differences in the Chainman Shale. First, the contribution of vegetation to the TM response was minimized using a linear regression technique, and then a TM 4/TM 5 density-sliced image was produced.
Field evaluation of the TM 4/TM 5 density-sliced image shows that all the high values in the Chainman Shale, which correspond to high maturity, are located in the Diamond Mountains; in contrast, Chainman Shale in the northwestern Pancake Range exhibits low to moderate values. These results are consistent with published local maturity determinations. Locally, the presence of limonitic arenaceous exposures and colluvium causes anomalously low TM 4/TM 5 values, but these areas can be identified in TM images because of their diagnostic VNIR reflectance spectra.
","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/BDFF895C-1718-11D7-8645000102C1865D","usgsCitation":"Rowan, L., Pawlewicz, M., and Jones, O.D., 1992, Mapping thermal maturity in the Chainman shale, near Eureka, Nevada, with Landsat Thematic Mapper images: American Association of Petroleum Geologists Bulletin, v. 76, no. 7, p. 1008-1023, https://doi.org/10.1306/BDFF895C-1718-11D7-8645000102C1865D.","productDescription":"16 p.","startPage":"1008","endPage":"1023","numberOfPages":"16","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":224679,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","city":"Eureka","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -115.75,\n 39.75\n ],\n [\n -116,\n 39.75\n ],\n [\n -116,\n 39.25\n ],\n [\n -115.75,\n 39.25\n ],\n [\n -115.75,\n 39.75\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"76","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a508be4b0c8380cd6b76b","contributors":{"authors":[{"text":"Rowan, Lawrence C.","contributorId":22860,"corporation":false,"usgs":true,"family":"Rowan","given":"Lawrence C.","affiliations":[],"preferred":false,"id":375540,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pawlewicz, Mark","contributorId":69212,"corporation":false,"usgs":true,"family":"Pawlewicz","given":"Mark","email":"","affiliations":[],"preferred":false,"id":375542,"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":375541,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70017263,"text":"70017263 - 1992 - Impact origin of the Avak Structure, Arctic Alaska, and genesis of the Barrow gas fields","interactions":[],"lastModifiedDate":"2023-01-19T17:47:56.045056","indexId":"70017263","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","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":"Impact origin of the Avak Structure, Arctic Alaska, and genesis of the Barrow gas fields","docAbstract":"Geophysical and subsurface geologic data suggest that the Avak structure, which underlies the Arctic Coastal Plain 12 km southeast of Barrow, Alaska, is a hypervelocity meteorite or comet impact structure. The structure is a roughly circular area of uplifted, chaotically deformed Upper Triassic to Lower Cretaceous sedimentary rocks 8 km in diameter that is bounded by a ring of anastomosing, inwardly dipping, listric normal faults 12 km in diameter. A zone of gently outward-dipping sedimentary country rocks forms a discontinuous ring of \"rim anticlines\" within the peripheral ring of normal faults. Beyond these anticlines, the sedimentary rocks are almost flat-lying. Basement consists of strongly deformed Ordovician and Silurian argillite. Density and acoustic impedance con rasts between the argillite and the overlying strata produce gravity and seismic-reflection signatures that define a ring of anticlines around the disturbed zone and a structural high surrounded by an annular structural low at its center.
In the adjacent Barrow gas fields, the tops of the informally named Neocomian \"pebble shale\" unit and the gas-producing Lower Jurassic Barrow sand (local usage) lie at average subsea depths of 488 m and 670 m, respectively. In the Avak 1 well, drilled on the central high, the pebble shale and the Barrow sand lie near the surface, documenting more than 500 m of relative uplift at the high. The cores in this well have steep dips (30-90 degrees), mixed breccia with Franklinian argillite clasts 10 and 90 m above basement, quartz grains with shock mosaicism and multiple sets of shock lamellae, oriented concussion fractures in sand-size quartz grains, and shatter cones resembling those found in the peripheral zones of well-documented impact structures. In addition, above-background levels o fractured quartz grains in Barrow sand were found as far as 19 km beyond the rim of the Avak structure.
Data concerning the age of the Avak structure are not definitive. If submarine landslide deposits in the upper part of the Aptian and Albian Torok Formation, in the subsurface 200 km to the east, were triggered by the Avak event, then the Avak meteorite struck a submerged marine shelf about 100 + or - 5 Ma. However, the impact features found at Avak (shatter cones, concussion fractures, shock lamellae and shock mosaicism in quartz grains, and widespread cataclasis) characterize the distal zones of meteorite impact structures. Fused rocks, plastic deformation, and shock-metamorphic minerals found in more proximal zones of impact structures are apparently missing. These observations, and the lack of Avak ejecta in cuttings and cores from the Torok Formation and Nanushuk Group (Albian to middle Cenomanian) in surrounding test wells, indicate that the impact event postdated these beds. In this case, the Avak meteorite struck a Late Cretaceous or Tertiary marine shelf or coastal plain between the Cenomanian (ca. 95 Ma), and deposition of the basal beds of the overlying late Pliocene and Quaternary Gubik Formation (ca. 3 Ma).
","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/BDFF889E-1718-11D7-8645000102C1865D","usgsCitation":"Kirschner, C., Grantz, A., and Mullen, M.W., 1992, Impact origin of the Avak Structure, Arctic Alaska, and genesis of the Barrow gas fields: American Association of Petroleum Geologists Bulletin, v. 76, no. 5, p. 651-679, https://doi.org/10.1306/BDFF889E-1718-11D7-8645000102C1865D.","productDescription":"29 p.","startPage":"651","endPage":"679","numberOfPages":"29","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":225163,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Avak structure, Barrow gas fields","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -160.10286874793076,\n 71.39378563719981\n ],\n [\n -160.10286874793076,\n 69.48627430745987\n ],\n [\n -146.27334730998183,\n 69.48627430745987\n ],\n [\n -146.27334730998183,\n 71.39378563719981\n ],\n [\n -160.10286874793076,\n 71.39378563719981\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"76","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a38d9e4b0c8380cd616ea","contributors":{"authors":[{"text":"Kirschner, C.E.","contributorId":81107,"corporation":false,"usgs":true,"family":"Kirschner","given":"C.E.","email":"","affiliations":[],"preferred":false,"id":375927,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Grantz, Arthur agrantz@usgs.gov","contributorId":2585,"corporation":false,"usgs":true,"family":"Grantz","given":"Arthur","email":"agrantz@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":375926,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mullen, M. W.","contributorId":15587,"corporation":false,"usgs":true,"family":"Mullen","given":"M.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":375925,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70017129,"text":"70017129 - 1992 - Lithofacies analysis of colluvial sediments - an aid in interpreting the recent history of Quaternary normal faults in the Basin and Range Province, western United States","interactions":[],"lastModifiedDate":"2024-05-17T11:04:56.354433","indexId":"70017129","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","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":"Lithofacies analysis of colluvial sediments - an aid in interpreting the recent history of Quaternary normal faults in the Basin and Range Province, western United States","docAbstract":"Inferring the frequency and magnitude of past earthquakes from the stratigraphy in exposures of normal-faulted sediments is difficult because colluvial lithofacies assemblages adjacent to faults are complex. Similarities in facies assemblages adjacent to young fault scarps in arid to semiarid areas, such as the Basin and Range province, allow lithofacies to be grouped into two genetic architectural elements: debris and wash elements. Upper and lower facies associations can commonly be recognized within each element. A lithofacies code scheme, similar to those used in the analysis of fluvial and glacial lithofacies sequences, provides a concise way of illustrating lithofacies relations in fault exposures. The source lithology of colluvial lithofacies is shown in the code, and soil-horizon symbols can be included. The architecture of lithofacies assemblages near fault scarps in semiarid areas is explained by a model of colluvial sedimentation in response to a single surface faulting event. Analysis of lithofacies assemblages exposed in three trenches across normal faults in the eastern Basin and Range shows how the model can be used to interpret fault histories. Similar facies analysis methods may be useful in interpreting colluvial sequences formed by non-tectonic processes.
The Uncompahgre caldera, and the Lake City caldera nested within it, each have fossil hydrothermal systems and associated mineral deposits that formed during multiple episodes of mineralization during Oligocene and Miocene time. New lead isotopic analyses for 51 ore samples, mainly galena, combined with previously obtained data for ore minerals and rocks, suggest likely lead source rocks and fluid-migration paths. Most values of 206Pb/204Pb, 207Pb/204Pb, and 208Pb/204Pb in galena from veins match the respective lead isotopic ratios for their host rocks; for example, all have 206Pb/204Pb typically in the range 18.4-19.0. The source for most vein lead is therefore probably the host unit for the vein. Some mixing of lead from other sources also occurred. Ratios of 206Pb/204Pb > 19.0 probably indicate a component of more-radiogenic lead from a Middle Proterozoic source. Lower lead isotopic ratios, 206Pb/204Pb < 18.5, suggest mixing with less-radiogenic lead from either Miocene rhyolitic volcanic and intrusive rocks or early Oligocene intermediate-composition volcanic rocks. Hydrothermal flow in the Uncompahgre caldera was predominantly west to east down the topographic slope. Discharge was mainly in closed topographic lows marked by lacustrine deposits. Hydrothermal circulation in the Lake City caldera was controlled by local topography and post-caldera intrusions and was isolated from flow in the Uncompahgre caldera and Eureka graben. Richer ore deposits may be associated with ring fault-related conduits that extend through the volcanic cover to more-radiogenic Middle Proterozoic basement at depth. As in the rest of the San Juan Mountains, lead originally came from a predominantly ∼1450 Ma source. Enough variation in 207Pb/204Pb was produced by orogenic events at ca. 1450 Ma, ca. 1760 Ma, and earlier to explain most of the 207Pb/204Pb variation present today in Tertiary volcanic rocks and hydrothermal veins.
A Late Pleistocene volcanic ash couplet consisting of a Glacier Peak ash layer and an underlying Mount Saint Helens J ash layer has been identified at three sites in the Colville Valley area of northeastern Washington. This ash couplet has been reported as far east as northwestern Montana and therefore appears to have widespread distribution south of the International Boundary. Because areas covered by the Cordilleran Ice Sheet, as well as by local mountain glaciers and icefields, were undergoing extensive deglaciation when these ash layers were deposited, about 11 200 BP, the ash couplet is an important time-stratigraphic marker, and its identification at a site provides information about the extent of deglaciation at that time.The ash couplet is easily recognized in the study area. Distinguishing characteristics include (i) the medium-sand-size (0.2–0.4 mm) rounded glass fragments and abundant mafic crystals in the fine-sand fraction of the Glacier Peak ash, a white layer 5–10 mm thick; (ii) the fine sandy silt and mafic-crystal-poor Mount Saint Helens J ash, also a white layer 5–10 mm thick, below the Glacier Peak ash; and (iii) the stratigraphic position of the couplet beneath the much younger Mazama ash.The presence of the Glacier Peak and Mount Saint Helens J ash couplet in the Colville Valley, about 50 km north (upglacier) from the Late Wisconsin terminal moraine near the town of Springdale, indicates that the active margin of the Colville sublobe of the Cordilleran Ice Sheet had retreated at least that distance by 11 200 BP.
","language":"English","publisher":"Canadian Science Publishing","doi":"10.1139/e92-187","issn":"00084077","usgsCitation":"Carrara, P., and Trimble, D., 1992, A glacier peak and Mount Saint Helens J volcanic ash couplet and the timing of deglaciation in the Colville Valley area, Washington: Canadian Journal of Earth Sciences, v. 29, no. 11, p. 2397-2405, https://doi.org/10.1139/e92-187.","productDescription":"9 p.","startPage":"2397","endPage":"2405","costCenters":[],"links":[{"id":225031,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Washington","otherGeospatial":"Colville Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -117.83272354754718,\n 48.14814340011884\n ],\n [\n -117.83272354754718,\n 48.05560883696705\n ],\n [\n -117.60501566141664,\n 48.05560883696705\n ],\n [\n -117.60501566141664,\n 48.14814340011884\n ],\n [\n -117.83272354754718,\n 48.14814340011884\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"29","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e409e4b0c8380cd4637a","contributors":{"authors":[{"text":"Carrara, P. E.","contributorId":33727,"corporation":false,"usgs":true,"family":"Carrara","given":"P. E.","affiliations":[],"preferred":false,"id":374616,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Trimble, D.A.","contributorId":9664,"corporation":false,"usgs":true,"family":"Trimble","given":"D.A.","email":"","affiliations":[],"preferred":false,"id":374615,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70016799,"text":"70016799 - 1992 - The southern Washington Cascades conductor: A previously unrecognized thick sedimentary sequence?","interactions":[],"lastModifiedDate":"2023-01-19T17:06:55.497097","indexId":"70016799","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","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":"The southern Washington Cascades conductor: A previously unrecognized thick sedimentary sequence?","docAbstract":"Geophysical studies in the southern Washington Cascades have outlined a possible, previously unrecognized sequence of sedimentary rocks. These postulated sedimentary units are interpreted to correspond to at least the upper section of a low-resistivity (high-conductivity) assemblage of rocks at depths of 1-10 km and with thicknesses up to 15 km that called the southern Washington Cascades conductor. Structure on the upper surface of this conductive assemblage correlates in some places with anticlines that bring Tertiary marine rocks near the surface. The geometry of the conductive rocks consists of a east-dipping, low-angle wedge that thickens to the north and with an undulating upper surface corresponding to the anticlines. Geothermal fluids may be a contributing factor to low resistivities in the deeper parts of the conductive section. -from Authors","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/BDFF8A56-1718-11D7-8645000102C1865D","usgsCitation":"Stanley, W.D., Gwilliam, W.J., Latham, G., and Westhusing, K., 1992, The southern Washington Cascades conductor: A previously unrecognized thick sedimentary sequence?: American Association of Petroleum Geologists Bulletin, v. 76, no. 10, p. 1569-1585, https://doi.org/10.1306/BDFF8A56-1718-11D7-8645000102C1865D.","productDescription":"17 p.","startPage":"1569","endPage":"1585","numberOfPages":"17","costCenters":[],"links":[{"id":224558,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Washington","otherGeospatial":"southern Washington Cascades","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -123.0476092389447,\n 47.09217717972356\n ],\n [\n -123.0476092389447,\n 46.10926604734689\n ],\n [\n -120.81643027066724,\n 46.10926604734689\n ],\n [\n -120.81643027066724,\n 47.09217717972356\n ],\n [\n -123.0476092389447,\n 47.09217717972356\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"76","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb052e4b08c986b324da8","contributors":{"authors":[{"text":"Stanley, W. D.","contributorId":86756,"corporation":false,"usgs":true,"family":"Stanley","given":"W.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":374528,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gwilliam, W. J.","contributorId":36127,"corporation":false,"usgs":true,"family":"Gwilliam","given":"W.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":374526,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Latham, Gary","contributorId":105739,"corporation":false,"usgs":true,"family":"Latham","given":"Gary","email":"","affiliations":[],"preferred":false,"id":374525,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Westhusing, Keith","contributorId":104920,"corporation":false,"usgs":true,"family":"Westhusing","given":"Keith","email":"","affiliations":[],"preferred":false,"id":374527,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70016729,"text":"70016729 - 1992 - Jurassic ash-flow sheets, calderas, and related intrusions of the Cordilleran volcanic arc in southeastern Arizona: Implications for regional tectonics and ore deposits","interactions":[],"lastModifiedDate":"2023-12-26T22:51:57.177714","indexId":"70016729","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Jurassic ash-flow sheets, calderas, and related intrusions of the Cordilleran volcanic arc in southeastern Arizona: Implications for regional tectonics and ore deposits","docAbstract":"Volcanologic, petrologic, and paleomagnetic studies of widespread Jurassic ash-flow sheets in the Huachuca-southern Dragoon Mountains area have led to identification of four large source calderas and associated comagmatic intracaldera intrusions. Stratigraphic, facies, and contact features of the caldera-related tuffs also provide constraints on the locations, lateral displacements, and very existence for some major northwest-trending faults and inferred regional thrusts in south-eastern Arizona. For example, the intricate Cochise thrust system, as mapped by others in the southern Dragoon Mountains, consists instead of primary depositional contacts within caldera-fill megabreccia, and the inferred regional thrusts do not exist, at least as previously interpreted. Silicic alkalic compositions of the Jurassic caldera-related, ash-flow tuffs; bimodal associated mafic magmatism; and interstratified coarse sedimentary deposits provide evidence for synvolcanic extension and rifting within the Cordilleran magmatic arc. Gold-copper mineralization is associated with subvolcanic intrusions at several of the Jurassic calderas.
In conjunction with the U.S. Geological Survey's exploration program in the National Petroleum Reserve, Alaska (NPRA) several high-resolution temperature logs were made in each of 21 drillholes between 1977 and 1984. These time-series of shallow (average 600-m depth) temperature profiles were extrapolated to infinite time to yield equilibrium temperature profiles (±0.1 °C). Thermal gradients are inversely correlated with elevation, and vary from 22 °C/km in the foothills of the Brooks Range to as high as 53 °C/km on the coastal plain to the north. Shallow temperature data were supplemented with 24 equilibrium temperatures (±3-5 °C) estimated from series of bottom-hole temperatures (BHTs) measured near the bottom of petroleum exploration wells. A total of 601 thermal conductivity measurements were made on drill cuttings and cores. Near-surface heat flow (±20%) is inversely correlated with elevation and ranges from a low of 27 mW/m2 in the foothills of the Brooks Range in the south, to a high of 90 mW/m2 near the north coast. Subsurface temperatures and thermal gradients estimated from corrected BHTs are similarly much higher on the coastal plain than in the foothills province to the south. Significant east-west variation in heat flow and subsurface temperature is also observed; higher heat flow and temperature coincide with higher basement topography. The observed thermal pattern is consistent with forced convection by a topographically driven ground-water flow system; alternative explanations are largely unsatisfactory. Average ground-water (Darcy) velocity in the postulated flow system is estimated to be of the order of 0.1 m/yr; the effective basin-scale permeability is estimated to be of the order of 10-14 m2. Organic maturation data collected in other studies indicate that systematic variations in thermal state may have persisted for tens of millions of years. The ground-water flow system thought to be responsible for present heat-flow variations conceivably has existed for the same period of time, possibly providing the driving mechanism for petroleum migration and accumulation at Prudhoe Bay.
The eastern margin of the Yucca Flat basin, in southern Nevada, is bounded by north-northwest-striking tilted fault blocks of the Halfpint Range whose strikes curve as much as 90° clockwise into east-northeast strikes in the French Peak-Massachusetts Mountain (FPMM) area. This pattern of arcuate structures has been attributed to clockwise drag along a postulated northwest-trending, right-lateral shear zone. The flexure model implies that rocks within the FPMM area were rotated strongly clockwise about a vertical axis. Directions of remanent magnetization of the middle Miocene Ammonia Tanks and Rainier Mesa Members of the Timber Mountain Tuff and of the Topopah Spring Member of the Paintbrush Tuff indicate no systematic vertical-axis rotation in the FPMM area and disprove the flexure model. After tilt correction, declinations of 29 site means obtained from the three ash-flow sheets in the FPMM area are not systematically different than declinations of 17 site means from the Halfpint Range or declinations of 16 site means from little-deformed mesa areas to the west. The paleomagnetic data thus indicate that structures in the FPMM area initiated with arcuate trends and were not originally straight elements that were rotated by right-lateral drag. The structures probably formed under the influence of spatially variable stress fields. The FPMM area lies in an accommodation zone between domains of oppositely tilted extensional fault blocks. Interaction between stress fields associated with propagating normal-fault zones may have been responsible for the arcuate structures in the FPMM area.
The upper Middle Jurassic-Lower Cretaceous Gravina belt lies along the eastern margin of the Alexander terrane in southeastern Alaska. This group of turbidites and mafic to intermediate volcanic rocks was deformed during mid to Late Cretaceous time during the closing of a basin of unknown size between the Alexander terrane on the west and the Stikine terrane to the east. Therefore structures of Gravina belt rocks largely reflect the final accretion and subsequent transport of the Alexander terrane. Six geologic transects across the central Gravina belt (southern Mitkof Island to northern Douglas Island) define a structural history that includes (1) syndepositional soft-sediment folding and faulting, possibly in conjunction with block tilting and extension; (2) tight to isoclinal folding or thrust faulting, with formation of a slaty cleavage (S1) striking ∼330°; (3) local coaxial refolding with formation of crenulation cleavage (S2); (4) development of domainal crenulation folds and cleavage (S3) oriented at a large angle to the margin of the belt; (5) intrusion of tonalitic plutons around 90 Ma; and (6) right-lateral strike-slip displacement on faults oriented ∼330°. Finite strain measurements on sedimentary rocks suggest the belt was at least twice its present width, normal to the foliation, before deformation. Subhorizontal margin-parallel fold axes, margin-parallel slaty cleavage, and margin-perpendicular stretching lineations suggest orthogonal contraction of the Gravina basin, assuming that oblique plate convergence was not decoupled along strike-slip faults. After contractional deformation, strike-slip faults indicate dextral displacement (probably of the order of several tens of kilometers) of the Alexander terrane with respect to the terranes to the east. Domainal crenulation folds and cleavages at a high angle to the margin of the belt suggest that the change in convergence directions occurred while the rocks (presently at the surface) could still plastically deform. This kinematic interpretation of structures is consistent with changes in plate motions [Engebretson et al., 1985]. Before 100 Ma, the convergence directions between the Kula and North America plates were at a high angle to the continental margin, whereas after 100 Ma, convergence directions were at a small angle to the continental margin. In addition, after 100 Ma, the Kula-North America, and not the Farallon-North America, convergence direction is most compatible with a N-S principal paleostress orientation derived from inversion of strike-slip fault data. This relationship suggests that it may have been the Kula plate that drove northward transport of the Alexander terrane along the margin of North America.
","language":"English","publisher":"Wiley","doi":"10.1029/92TC01107","usgsCitation":"Haeussler, P.J., 1992, Structural evolution of an arc-basin: The Gravina Belt in central southeastern Alaska: Tectonics, v. 11, no. 6, p. 1245-1265, https://doi.org/10.1029/92TC01107.","productDescription":"21 p.","startPage":"1245","endPage":"1265","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"links":[{"id":337548,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Alexander terrane","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -135.92998305119977,\n 58.76028709475264\n ],\n [\n -135.92998305119977,\n 56.61312544505941\n ],\n [\n -133.71072320749985,\n 56.61312544505941\n ],\n [\n -133.71072320749985,\n 58.76028709475264\n ],\n [\n -135.92998305119977,\n 58.76028709475264\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"11","issue":"6","noUsgsAuthors":false,"publicationDate":"2010-07-26","publicationStatus":"PW","scienceBaseUri":"58c90130e4b0849ce97abd57","contributors":{"authors":[{"text":"Haeussler, Peter J. 0000-0002-1503-6247 pheuslr@usgs.gov","orcid":"https://orcid.org/0000-0002-1503-6247","contributorId":503,"corporation":false,"usgs":true,"family":"Haeussler","given":"Peter","email":"pheuslr@usgs.gov","middleInitial":"J.","affiliations":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":119,"text":"Alaska Science Center Geology Minerals","active":true,"usgs":true}],"preferred":true,"id":684323,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70162563,"text":"70162563 - 1992 - The ten-year eruption of Kilauea Volcano","interactions":[],"lastModifiedDate":"2016-02-09T15:30:47","indexId":"70162563","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1437,"text":"Earthquakes & Volcanoes (USGS)","active":true,"publicationSubtype":{"id":10}},"title":"The ten-year eruption of Kilauea Volcano","docAbstract":"The Pu'u 'O' o-Kupaianaha eruption now ranks as the longest-lived historic eruption on the East Rift Zone and the most destructive in Kilauea's recent history.
\nAbout 1 km3 of lava erupted during the first 0 years of the eruption. Lava flows have destroyed 181 houses and severed the coastal highway along the volcano's south flank, severely restricting transportation on this part of the island of Hawaii. the eruption consisted of many distinct episodes characterized by activity at different vents and by different eruptive styles. the following summarizes the first 10 years of the eruption, starting with the initial outbreak in 1983.
","language":"English","publisher":"U.S Geological Survey","usgsCitation":"Clague, D., and Heliker, C., 1992, The ten-year eruption of Kilauea Volcano: Earthquakes & Volcanoes (USGS), v. 23, no. 6, p. 244-254.","productDescription":"11 p.","startPage":"244","endPage":"254","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":314890,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Hawaii","otherGeospatial":"Kīlauea","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -155.26290893554688,\n 19.433571773164164\n ],\n [\n -155.2972412109375,\n 19.420620739866035\n ],\n [\n -155.30548095703125,\n 19.40119225476861\n ],\n [\n -155.28488159179688,\n 19.35908924593432\n ],\n [\n -155.19149780273438,\n 19.2573494756706\n ],\n [\n -155.1331329345703,\n 19.2748506284423\n ],\n [\n -155.0562286376953,\n 19.31567937987149\n ],\n [\n -155.1496124267578,\n 19.43616185591159\n ],\n [\n -155.2306365966797,\n 19.419325579756944\n ],\n [\n -155.25604248046875,\n 19.430981649106492\n ],\n [\n -155.26290893554688,\n 19.433571773164164\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"23","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"56a8a6d2e4b0b28f1184dc21","contributors":{"authors":[{"text":"Clague, D.A.","contributorId":36129,"corporation":false,"usgs":true,"family":"Clague","given":"D.A.","email":"","affiliations":[],"preferred":false,"id":589853,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Heliker, C.","contributorId":80314,"corporation":false,"usgs":true,"family":"Heliker","given":"C.","affiliations":[],"preferred":false,"id":589854,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70162371,"text":"70162371 - 1992 - Preliminary damage and intensity survey","interactions":[],"lastModifiedDate":"2016-02-04T16:46:23","indexId":"70162371","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1437,"text":"Earthquakes & Volcanoes (USGS)","active":true,"publicationSubtype":{"id":10}},"title":"Preliminary damage and intensity survey","docAbstract":"A major earthquake struck the Mojave Desert region in southern California at about 5 a.m. local time on June 28th, 1992. Seismologists located the epicenter of the magnitude 7.6 (Ms) earthquake 5-10km southwest of Landers, a small community about 150km east of Los Angeles. the earthquake shook a wide area of southern California, southern Nevada, western Arizona, and extreme northwest Mexico. High-rise buildings swayed in cities as far north as Boise, Idaho, and as far east as Albuquerque, New Mexico, and Denver, Colorado. Standing waves called seiches disturbed the surface of lakes and bays as far away as Washington State and the Gulf Coast of Texas. In United States, the Landers shock was felt over a contiguous land area approximately 103.600km2. Approximately 3 hrs after the Landers earthquake, a magntude 6.7 (Ms) aftershock struck an area near Big Bear Lake, California, less than 50 km from the main-shcok epicenter. Within its epicentral area this afterhoskc caused consideralbe damage.
","language":"English","publisher":"U.S Geological Survey","usgsCitation":"Brewer, L.R., 1992, Preliminary damage and intensity survey: Earthquakes & Volcanoes (USGS), v. 23, no. 5, p. 219-226.","productDescription":"8 p.","startPage":"219","endPage":"226","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":314651,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.05657958984375,\n 34.40237742424137\n ],\n [\n -115.96343994140625,\n 34.40917568058836\n ],\n [\n -115.93597412109374,\n 33.667211101197545\n ],\n [\n -116.96319580078125,\n 33.74946419232578\n ],\n [\n -117.05932617187499,\n 34.384246040152206\n ],\n [\n -117.05657958984375,\n 34.40237742424137\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"23","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"56a20f4ee4b0961cf2811c1b","contributors":{"authors":[{"text":"Brewer, L. R.","contributorId":89506,"corporation":false,"usgs":true,"family":"Brewer","given":"L.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":589315,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70168821,"text":"70168821 - 1992 - The 1992 Landers earthquake and surface faulting","interactions":[],"lastModifiedDate":"2016-09-19T14:46:50","indexId":"70168821","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1437,"text":"Earthquakes & Volcanoes (USGS)","active":true,"publicationSubtype":{"id":10}},"title":"The 1992 Landers earthquake and surface faulting","docAbstract":"Faulting associated with the June 28, 992, earthquake near Landers, California, broke the surface of the ground over a length of more than 70 km, the longest surface rupture in the United States since the great San Francisco quake of 1906. the strongest shaking associated with this magnitude 7.6 (MS) earthquake, the largest in the contiguous 48 states in the last 40 years, occurred in a sparsely populated sections of the Mojave Desert more than 200 km east of Los Angeles. the earthquake began with a sudden slip on the Johnson Valley fault about 10 km southwest of Landers. The initial fault movement probably occurred at a depth of less than 10 km. Surface faulting then propagated over 70 km to the north and northeast. The faulting linked preexisting faults-some previously known and mapped and others previously unknown-into a complex, coherent rupture zone.
","language":"English","publisher":"U.S Geological Survey","usgsCitation":"Rymer, M.J., 1992, The 1992 Landers earthquake and surface faulting: Earthquakes & Volcanoes (USGS), v. 23, no. 5, p. 209-218.","productDescription":"10 p.","startPage":"209","endPage":"218","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":318547,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Landers","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.1746826171875,\n 34.768691457552706\n ],\n [\n -116.15295410156249,\n 34.76192255039478\n ],\n [\n -115.96343994140625,\n 33.51849923765608\n ],\n [\n -117.158203125,\n 33.53681606773302\n ],\n [\n -117.1746826171875,\n 34.768691457552706\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"23","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"56d96e5fe4b015c306f764ce","contributors":{"authors":[{"text":"Rymer, Michael J. mrymer@usgs.gov","contributorId":1522,"corporation":false,"usgs":true,"family":"Rymer","given":"Michael","email":"mrymer@usgs.gov","middleInitial":"J.","affiliations":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"preferred":true,"id":621852,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":26300,"text":"wri924018 - 1992 - Hydrology of the Cave Springs area near Chattanooga, Hamilton County, Tennessee","interactions":[],"lastModifiedDate":"2026-04-06T19:36:13.528626","indexId":"wri924018","displayToPublicDate":"1992-01-01T00:00:00","publicationYear":"1992","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":"92-4018","title":"Hydrology of the Cave Springs area near Chattanooga, Hamilton County, Tennessee","docAbstract":"The hydrology of Cave Springs, the second largest spring in East Tennessee was investigated from July 1987 to September 1989. Wells near the spring supply about 5 million gallons per day of potable water to people in Hamilton County near Chattanooga. Discharge from the spring averaged about 13.5 cubic feet per second (8.72 million gallons per day) during the study period. Withdrawals by the Hixson Utility District from wells upgradient from the outflow averaged 8.6 cubic feet per second (5.54 million gallons per day). Aquifer tests using wells intersecting a large solution cavity supplying water to the spring showed a drawdown of less than 3 feet with a discharge of 9,000 gallons per minute or 20 cubic feet per second.
Temperature and specific conductance of ground water near the spring outflow were monitored hourly. Temperatures ranged from 13.5 to 18.2 degrees celsius, and fluctuated seasonally in response to climate. Specific-conductance values ranged from 122 to 405 microsiemens per centimeter at 25 degrees Celsius, but were generally between 163 to 185 microsiemens per centimeter.
The drainage area of the basin recharging the spring system was estimated to be 1O square miles. A potentiometric map of the recharge basin was developed from water levels measured at domestic and test wells in August 1989. Aquifer tests at five test wells in the study area indicated that specific-capacity values for these wells ranged from 4.1 to 261 gallons per minute per foot of drawdown. Water-quality characteristics of ground water in the area were used in conjunction with potentiometric-surface maps to delineate the approximate area contributing recharge to Cave Springs.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri924018","collaboration":"Prepared in cooperation with the Hixson Utility District","usgsCitation":"Bradfield, A.D., 1992, Hydrology of the Cave Springs area near Chattanooga, Hamilton County, Tennessee: U.S. Geological Survey Water-Resources Investigations Report 92-4018, iv, 28 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri924018.","productDescription":"iv, 28 p.","costCenters":[],"links":[{"id":502216,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/wri92-4018/pdf/wrir_92-4018_a.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122969,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_92_4018.jpg"},{"id":1998,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wri92-4018/index.html","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Tennessee","county":"Hamilton County","otherGeospatial":"Cave Springs","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a13e4b07f02db601f5b","contributors":{"authors":[{"text":"Bradfield, Arthur D.","contributorId":88383,"corporation":false,"usgs":true,"family":"Bradfield","given":"Arthur","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":196137,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":27105,"text":"wri904108 - 1991 - Hydrogeology of the surficial aquifer system, Dade County, Florida","interactions":[],"lastModifiedDate":"2021-10-14T12:09:26.947959","indexId":"wri904108","displayToPublicDate":"2021-10-13T11:05:00","publicationYear":"1991","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":"90-4108","title":"Hydrogeology of the surficial aquifer system, Dade County, Florida","docAbstract":"An investigation of the surficial aquifer system in Dade County, begun in 1983, is part of a regional study of the aquifer system in southeastern Florida. Test drilling for lithologic samples, flow measurements during drilling, aquifer testing, and analyses of earlier data permitted delineation of the hydraulic conductivity distribution (on hydrogeologic sections), the aquifers in the system, the generalized transmissivity distribution, and interpretation of the ground-water flow system. \r\n\r\nThe surficial aquifer system, in which an unconfined ground-water flow system exists, is composed of the sediments from land surface downward to the top of a regionally extensive zone of sediments of low permeability called the intermediate confining unit. The aquifer system units, which vary in composition from clay-size sediments to cavernous limestone, are hydro stratigraphically divided into the Biscayne aquifer at the top; an intervening semiconfining unit that consists principally of clayey sand; a predominantly gray limestone aquifer in the Tamiami Formation in western and west-central Dade County; and sand or clayey sand near the base of the surficial aquifer system. The base of the surficial aquifer system ranges from a depth of about 175 to 210 feet below land surface in westernmost Dade County to greater than 270 feet in northeastern Dade County. Test drilling and aquifer-test data indicate a complex hydraulic conductivity distribution. Hydraulic conductivities of the very highly permeable zone of the Biscayne aquifer commonly exceed 10,000 feet per day; in the gray limestone aquifer, they range from 210 to 780 feet per day. \r\n\r\nTransmissivities of the surficial aquifer system vary locally but have a recognizable areal trend. Estimated values generally are about 300,000 feet squared per day or greater in nearly all of central and eastern Dade County. Transmissivity is lower to the west, decreasing to less than 75,000 feet squared per day in western Dade County. High transmissivity usually is associated with thick sections of the Fort Thompson Formation within the Biscayne aquifer. The gray limestone aquifer of the Tamiami Formation has transmissivities that range from 5,800 to 39,000 feet squared per day in western Dade County. The transition from high transmissivity to relatively low transmissivity is often only a few miles wide and coincides with the decrease in thickness of the very highly permeable Fort Thompson Formation, which marks the western boundary of the Biscayne aquifer. \r\n\r\nMore effective drainage as a result of extensive canal systems and large-scale pumping from municipal well fields has greatly altered the predevelopment flow system in eastern Dade County by: (1) eliminating or greatly reducing a seasonal and coastal ground-water ridge; (2) reducing deep circulation; (3) reducing or eliminating seasonal westward movement of ground water; (4) causing accelerated stormwater runoff and short ground-water flow paths; and (5) generally lowering the water table and inducing saltwater intrusion. Under predevelopment conditions in western Dade County, water entered the gray limestone aquifer by lateral movement from Broward and Collier Counties, and by downward seepage from The Everglades and the Biscayne aquifer, and moved southward and southeastward into Dade County to coastal discharge areas. Circulation in the Biscayne aquifer inland also was primarily to the south and southeast. In eastern Dade County, the seasonal ground-water ridge that formed under predevelopment conditions supported both easterly and westerly ground-water flow away from the ridge axis. This seasonal flow created a zone of lower dissolved solids.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri904108","usgsCitation":"Fish, J., and Stewart, M., 1991, Hydrogeology of the surficial aquifer system, Dade County, Florida: U.S. Geological Survey Water-Resources Investigations Report 90-4108, v, 50 p., https://doi.org/10.3133/wri904108.","productDescription":"v, 50 p.","costCenters":[{"id":27821,"text":"Caribbean-Florida Water Science Center","active":true,"usgs":true}],"links":[{"id":2216,"rank":100,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1990/4108/wri904108.pdf","text":"Report","size":"3.01 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 90-4108"},{"id":389208,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1990/4108/wri904108_plates.pdf","text":"Plates 1-11","size":"11.5 MB","linkFileType":{"id":1,"text":"pdf"}},{"id":159040,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1990/4108/coverthb.jpg"}],"country":"United States","state":"Florida","county":"Dade County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -80.79345703124999,\n 25.28443774698303\n ],\n [\n -79.73876953124997,\n 25.28443774698303\n ],\n [\n -79.72778320312499,\n 26.401710528707707\n ],\n [\n -80.2001953125,\n 26.362342068998764\n ],\n [\n -80.74951171874999,\n 26.43122806450644\n ],\n [\n -80.79345703124999,\n 25.28443774698303\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
We monitored lead exposure in Eastern Prairie Population Canada geese during summer-winter, 1986-1987 and 1987-1988 at 5 areas. Blood lead concentrations in geese trapped during summer at Cape Churchill Manitoba were below levels indicative of recent lead exposure (0.18 ppm). Geese exposed to lead (≥0.18 ppm blood lead) increased to 7.6% at Oak Hammock Wildlife Management Area (WMA), southern Manitoba, where lead shot was still in use, and to 10.0% at Roseau River WMA, northern Minnesota, when fall-staging geese were close to a source of lead shot in Manitoba. Proportion of birds exposed to lead dropped to <2% at Lac Qui Parle WMA, Minnesota, a steel shot zone since 1980. On the wintering grounds at Swan Lake National Wildlife Refuge in Missouri, 4.9% of all geese showed exposure to lead before the hunting season. Lead exposure rose to 10.0% after hunting ended and then decreased to 5.2% in late winter. Incidence of lead shot in gizzards and concentrations of lead in livers supported blood assay data. Soil samples indicated that lead shot continues to be available to geese at Swan Lake, even though the area was established as a non-toxic shot zone in 1978. Steel shot zones have reduced lead exposure in the Eastern Prairie Population, but lead shot persists in the environment and continues to account for lead exposure and mortality in Eastern Prairie Population Canada geese.
","language":"English","publisher":"The Wildlife Society","usgsCitation":"DeStefano, S., Brand, C.J., Rusch, D., Finley, D.L., and Gillespie, M.M., 1991, Lead exposure in Canada geese of the eastern prairie population: Wildlife Society Bulletin, v. 19, no. 1, p. 23-32.","productDescription":"10 p.","startPage":"23","endPage":"32","numberOfPages":"10","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":456,"text":"National Wildlife Health Center","active":true,"usgs":true}],"links":[{"id":258883,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":258865,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://www.jstor.org/stable/3782411","linkFileType":{"id":5,"text":"html"}}],"country":"United States, Canada","state":"Minnesota, Manitoba","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -96.15234375,\n 43.45291889355465\n ],\n [\n -90.52734374999999,\n 43.644025847699496\n ],\n [\n -92.197265625,\n 46.37725420510028\n ],\n [\n -88.9453125,\n 48.69096039092549\n ],\n [\n -94.39453125,\n 49.49667452747045\n ],\n [\n -95.00976562499999,\n 51.83577752045248\n ],\n [\n -95.2734375,\n 55.7765730186677\n ],\n [\n -93.603515625,\n 58.722598828043374\n ],\n [\n -94.482421875,\n 59.93300042374631\n ],\n [\n -102.39257812499999,\n 59.977005492196\n ],\n [\n -103.095703125,\n 56.31653672211301\n ],\n [\n -102.83203125,\n 51.069016659603896\n ],\n [\n -100.81054687499999,\n 48.574789910928864\n ],\n [\n -97.822265625,\n 48.40003249610685\n ],\n [\n -96.767578125,\n 46.92025531537451\n ],\n [\n -96.15234375,\n 43.45291889355465\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"19","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a45b8e4b0c8380cd67491","contributors":{"authors":[{"text":"DeStefano, S.","contributorId":84309,"corporation":false,"usgs":true,"family":"DeStefano","given":"S.","email":"","affiliations":[],"preferred":false,"id":354845,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brand, C. J.","contributorId":8788,"corporation":false,"usgs":true,"family":"Brand","given":"C.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":354843,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rusch, D. H.","contributorId":19897,"corporation":false,"usgs":true,"family":"Rusch","given":"D. H.","affiliations":[],"preferred":false,"id":354844,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Finley, Daniel L.","contributorId":103155,"corporation":false,"usgs":true,"family":"Finley","given":"Daniel","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":354846,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Gillespie, Murray M.","contributorId":108064,"corporation":false,"usgs":true,"family":"Gillespie","given":"Murray","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":354847,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":5222592,"text":"5222592 - 1991 - Gray wolf density and its association with weights and hematology of pups from 1970 to 1988","interactions":[],"lastModifiedDate":"2020-02-24T11:59:59","indexId":"5222592","displayToPublicDate":"2010-06-16T12:18:12","publicationYear":"1991","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2507,"text":"Journal of Wildlife Diseases","active":true,"publicationSubtype":{"id":10}},"title":"Gray wolf density and its association with weights and hematology of pups from 1970 to 1988","docAbstract":"We examined weights and hematologic profiles of gray wolf (Canis lupus) pups and the associated wolf density in the east-central Superior National Forest of northeastern Minnesota (USA) during 1970 to 1988. We collected weight and hematologic data from 117 pups (57 females, 60 males) during 1 September to 22 November each year. The wolf density (wolves/800 km2) trend was divided into three phases: high (72 ± 7), 1970 to 1975; medium (44 ± 2), 1976 to 1983; and low (27 ± 2), 1984 to 1988. Wolf numbers declined (P = 0.0001) 39 and 63% from 1970 to 1975 to 1976 to 1983 and from 1970 to 1975 to 1984 to 1988, respectively. Weight was similar between male and female pups and did not vary as wolf density changed. Mean hemoglobin (P = 0.04), red (P = 0.0001) and white blood cells (P = 0.002), mean corpuscular volume, mean corpuscular hemoglobin concentration and mean corpuscular hemoglobin (P = 0.0001) did differ among the multi-annual phases of changing wolf density. Weight and hematologic data also were compared to values from captive wolf pups. The high, but declining wolf density was associated with macrocytic, normochromic anemia in wolf pups, whereas the lowest density coincided with a hypochromic anemia. Although hematologic values show promise for assessing wolf pup condition and wolf population status, they must be used cautiously until data are available from other populations.
","language":"English","publisher":"Wildlife Disease Association","doi":"10.7589/0090-3558-27.4.630","usgsCitation":"DelGiudice, G.D., Mech, L.D., and Seal, U., 1991, Gray wolf density and its association with weights and hematology of pups from 1970 to 1988: Journal of Wildlife Diseases, v. 27, no. 4, p. 630-636, https://doi.org/10.7589/0090-3558-27.4.630.","productDescription":"7 p.","startPage":"630","endPage":"636","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":193977,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Minnesota","otherGeospatial":"Superior National Forest","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.04394531249999,\n 47.824220149350246\n ],\n [\n -90.0604248046875,\n 48.085418575511966\n ],\n [\n -90.736083984375,\n 48.100094697973795\n ],\n [\n -90.90087890624999,\n 48.246625590713826\n ],\n [\n -91.318359375,\n 48.07807894349862\n ],\n [\n -91.549072265625,\n 48.05605376398125\n ],\n [\n -91.746826171875,\n 48.19538740833338\n ],\n [\n -92.054443359375,\n 48.330691283387175\n ],\n [\n -92.296142578125,\n 48.35989909002194\n ],\n [\n -92.296142578125,\n 48.23565029755308\n ],\n [\n -92.3675537109375,\n 48.228332127214934\n ],\n [\n -92.493896484375,\n 48.43284538647477\n ],\n [\n -92.7191162109375,\n 48.46563710044979\n ],\n [\n -92.61474609375,\n 48.5275192374508\n ],\n [\n -92.9498291015625,\n 48.60748989475176\n ],\n [\n -92.94433593749999,\n 48.1367666796927\n ],\n [\n -92.68615722656249,\n 47.868459093342956\n ],\n [\n -93.4002685546875,\n 47.468949677672484\n ],\n [\n -92.49938964843749,\n 47.17477833929903\n ],\n [\n -91.0711669921875,\n 47.431803338643334\n ],\n [\n -90.47241210937499,\n 47.73193447949174\n ],\n [\n -90.04394531249999,\n 47.824220149350246\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"27","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abae4b07f02db671f80","contributors":{"authors":[{"text":"DelGiudice, Glenn D.","contributorId":64582,"corporation":false,"usgs":true,"family":"DelGiudice","given":"Glenn","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":336628,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mech, L. David 0000-0003-3944-7769 david_mech@usgs.gov","orcid":"https://orcid.org/0000-0003-3944-7769","contributorId":2518,"corporation":false,"usgs":true,"family":"Mech","given":"L.","email":"david_mech@usgs.gov","middleInitial":"David","affiliations":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true}],"preferred":true,"id":336630,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Seal, U.S.","contributorId":40564,"corporation":false,"usgs":false,"family":"Seal","given":"U.S.","email":"","affiliations":[],"preferred":false,"id":336629,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70016665,"text":"70016665 - 1991 - Sedimentary facies and depositional environments of early Mesozoic Newark Supergroup basins, eastern North America","interactions":[],"lastModifiedDate":"2025-06-05T17:13:29.047401","indexId":"70016665","displayToPublicDate":"2003-04-22T00:00:00","publicationYear":"1991","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2996,"text":"Palaeogeography, Palaeoclimatology, Palaeoecology","printIssn":"0031-0182","active":true,"publicationSubtype":{"id":10}},"title":"Sedimentary facies and depositional environments of early Mesozoic Newark Supergroup basins, eastern North America","docAbstract":"The early Mesozoic Newark Supergroup consists of continental sedimentary rocks and basalt flows that occupy a NE-trending belt of elongate basins exposed in eastern North America. The basins were filled over a period of 30–40 m.y. spanning the Late Triassic to Early Jurassic, prior to the opening of the north Atlantic Ocean. The sedimentary rocks are here divided into four principal lithofacies. The alluvial-fan facies includes deposits dominated by: (1) debris flows; (2) shallow braided streams; (3) deeper braided streams (with trough crossbeds); or (4) intense bioturbation or hyperconcentrated flows (tabular, unstratified muddy sandstone). The fluvial facies include deposits of: (1) shallow, ephemeral braided streams; (2) deeper, flashflooding, braided streams (with poor sorting and crossbeds); (3) perennial braided rivers; (4) meandering rivers; (5) meandering streams (with high suspended loads); (6) overbank areas or local flood-plain lakes; or (7) local streams and/or colluvium. The lacustrine facies includes deposits of: (1) deep perennial lakes; (2) shallow perennial lakes; (3) shallow ephemeral lakes; (4) playa dry mudflats; (5) salt-encrusted saline mudflats; or (6) vegetated mudflats. The lake margin clastic facies includes deposits of: (1) birdfoot deltas; (2) stacked Gilbert-type deltas; (3) sheet deltas; (4) wave-reworked alluvial fans; or (5) wave-sorted sand sheets.
Coal deposits are present in the lake margin clastic and the lacustrine facies of Carnian age (Late Triassic) only in basins of south-central Virginia and North and South Carolina. Eolian deposits are known only from the basins in Nova Scotia and Connecticut. Evaporites (and their pseudomorphs) occur mainly in the northern basins as deposits of saline soils and less commonly of saline lakes, and some evaporite and alkaline minerals present in the Mesozoic rocks may be a result of later diagenesis. These relationships suggest climatic variations across paleolatitudes, more humid to the south where coal beds are preserved, and more arid in the north where evaporites and eolian deposits are common. Fluctuations in paleoclimate that caused lake levels to rise and fall in hydrologically closed basins are preserved as lacustrine cycles of various scales, including major shifts in the Late Triassic from a wet Carnian to an arid Norian. In contrast, fluvial deposits were mainly formed in response to the tectonic evolution of the basins, but to some extent also reflect climatic changes.
The Newark Supergroup illustrates the complexity of rift-basin sedimentation and the problems that may arise from using a single modern analog for sedimentary deposition spanning millions of years. It also shows that a tremendous wealth of depositional, climatic, and tectonic information is preserved in ancient rift-basin deposits which can be recovered if the depositional processes of modern rift-basin deposits are understood.
No abstract available.
","language":"English","publisher":"National Science Foundation, Office of Polar Programs","publisherLocation":"Arlington, VA","usgsCitation":"ten Brink, U., Beaudoin, B.C., Stern, T., and Bannister, S., 1991, Seismic investigation of the boundary between East and West Antarctica: Antarctic Journal of the United States, v. 26, no. 5, p. 33-36.","productDescription":"4 p.","startPage":"33","endPage":"36","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":296702,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":346126,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://www.coldregions.org/vufind/Record/175327"}],"otherGeospatial":"Antarctica","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n 162,\n -83\n ],\n [\n 170,\n -83\n ],\n [\n 170,\n -82\n ],\n [\n 162,\n -82\n ],\n [\n 162,\n -83\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"26","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"549165d2e4b0d0759afaad99","contributors":{"authors":[{"text":"ten Brink, Uri S. 0000-0001-6858-3001 utenbrink@usgs.gov","orcid":"https://orcid.org/0000-0001-6858-3001","contributorId":127560,"corporation":false,"usgs":true,"family":"ten Brink","given":"Uri S.","email":"utenbrink@usgs.gov","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true},{"id":186,"text":"Coastal and Marine Geology Program","active":true,"usgs":true}],"preferred":false,"id":536777,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Beaudoin, Bruce C.","contributorId":58140,"corporation":false,"usgs":true,"family":"Beaudoin","given":"Bruce","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":536778,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Stern, T.","contributorId":49137,"corporation":false,"usgs":true,"family":"Stern","given":"T.","affiliations":[],"preferred":false,"id":536779,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bannister, Stephen","contributorId":8497,"corporation":false,"usgs":true,"family":"Bannister","given":"Stephen","email":"","affiliations":[],"preferred":false,"id":536780,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":19458,"text":"ofr9166 - 1991 - Regional stratigraphy and subsurface geology of Cenozoic deposits, Gulf Coastal Plain, south-central United States","interactions":[{"subject":{"id":19458,"text":"ofr9166 - 1991 - Regional stratigraphy and subsurface geology of Cenozoic deposits, Gulf Coastal Plain, south-central United States","indexId":"ofr9166","publicationYear":"1991","noYear":false,"title":"Regional stratigraphy and subsurface geology of Cenozoic deposits, Gulf Coastal Plain, south-central United States"},"predicate":"SUPERSEDED_BY","object":{"id":38232,"text":"pp1416G - 1996 - Regional stratigraphy and subsurface geology of Cenozoic deposits, Gulf Coastal Plain, south-central United States","indexId":"pp1416G","publicationYear":"1996","noYear":false,"chapter":"G","title":"Regional stratigraphy and subsurface geology of Cenozoic deposits, Gulf Coastal Plain, south-central United States"},"id":1}],"supersededBy":{"id":38232,"text":"pp1416G - 1996 - Regional stratigraphy and subsurface geology of Cenozoic deposits, Gulf Coastal Plain, south-central United States","indexId":"pp1416G","publicationYear":"1996","noYear":false,"title":"Regional stratigraphy and subsurface geology of Cenozoic deposits, Gulf Coastal Plain, south-central United States"},"lastModifiedDate":"2015-11-02T11:48:46","indexId":"ofr9166","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1991","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":"91-66","title":"Regional stratigraphy and subsurface geology of Cenozoic deposits, Gulf Coastal Plain, south-central United States","docAbstract":"The Gulf Coast Regional Aquifer-System Analysis includes all major aquifer systems in Cenozoic deposits in the Gulf Coastal Plain in the States of Arkansas, Illinois, Kentucky, Louisiana, Mississippi, Missouri, Tennessee, Texas, and small areas in Alabama and Florida (western panhandle area), an area of about 290,000 square miles. The Gulf Coast geosyncline and the Mississippi embayment were the major depocenters for the Tertiary and Quaternary deposits that form the framework for the aquifer systems.
\nFoiiDation of the Gulf Coast geosyncline and the Mississippi embayment began with downwarping and downfaulting at the end of the Paleozoic Era. Sedimentation caused the geosyncline to continue to subside throughout Mesozoic and Cenozoic time. During the Late Cretaceous, at the close of the Mesozoic Era, the sea advanced northward and eventually inundated the Mississippi embayment. Marine cycles persisted throughout the Paleocene and Eocene Epochs of the Tertiary Period, as the sea alternately advanced and retreated over the Mississippi embayment. The resulting sediments form a series of dense marine clays separated by terrigenous sands. The Gulf Coast geosyncline remained submerged during marine regressions in the embayment. After withdrawal of the last Tertiary sea from the Mississippi embayment at the end of the Eocene Epoch, deposition continued along the Gulf Coastal Plain under a shifting variety of nonmarine, marine, near-marine, and deltaic environments. Deposition resumed in the Mississippi embayment during the Quaternary with glacially related terraces and aggradation of streams. Fluvial deposition continues.
\nStructural features in the Gulf Coastal Plain and Mississippi embayment significantly affected Cenozoic deposition. The Desha basin, for example, is a pronounced Tertiary synclinal depocenter in southeastern Arkansas. Three large uplifts are approximately aligned along the latitude of the northern boundary of Louisiana. These are, from west to east, the Sabine, Monroe, and Jackson uplifts. A belt of three major fault zones, the Luling-Mexia-Talco, Arkansas, and Pickens-Gilbertown, generally follows the strike of sediments across the Coastal Plain and more or less forms the northern updip extent of the Gulf Coast geosyncline. An alternating series of gentle synclines and anticlines is oriented perpendicular to the coastline along the Gulf Coast in Texas. Beginning at the southwestern end, these are the Rio Grande embayment, San Marcos arch, Houston embayment, and Sabine arch. The Wiggins anticline is oriented approximately along strike of the sediments in southern Mississippi. Salt domes are numerous in the Gulf Coastal Plain and may penetrate thousands of feet of sediments. Although the degree of salt intrusion can be very great, disruption of adjacent strata is limited to the vicinity of the dome.
\nThe physiography of the Gulf Coastal Plain is a direct result of the nature of the strata at land surface and physical forces that act upon them. Different terrains typify the lithologies that underlie them. The sands and clays that are the predominant rock types each produce characteristic geomorphologic patterns; sands tend to produce ridges, and clays produce topographic lows.
\nAlthough Cenozoic deposits are not uniformly differentiated, interstate correlations of major Paleocene and Eocene units are generally established throughout the area. Younger deposits are not as well differentiated. Some stratigraphic designations made at surface exposures cannot be extended into the sub-surface, and the scarcity of distinct geologic horizons has hampered differentiation on a regional scale. The complexities of facies development in Oligocene and younger coastal deposits preclude the development of extensive recognizable horizons needed for stratigraphic applications. Coastal deposits are a heterogeneous assemblage of deltaic, lagoonal, lacustrine, palustrine, eolian, and fluvial clastic facies and local calcareous reef facies. Even major time boundaries, as between geologic series, are not fully resolved. Surficial Quaternary deposits overlie the truncated subcrops of Tertiary strata and generally are distinguishable, although some contacts between Pleistocene and underlying Pliocene deposits have been a ?lstoncal source of controversy. Glacially related terraces are characteristic of the Pleistocene Epoch, and alluvium of aggrading streams typifies the Holocene.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr9166","usgsCitation":"Hosman, R., 1991, Regional stratigraphy and subsurface geology of Cenozoic deposits, Gulf Coastal Plain, south-central United States: U.S. Geological Survey Open-File Report 91-66, vi, 43 p.; 31 Figures: 17.07 x 21.75 inches or smaller; 1 Table, https://doi.org/10.3133/ofr9166.","productDescription":"vi, 43 p.; 31 Figures: 17.07 x 21.75 inches or smaller; 1 Table","numberOfPages":"49","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":151336,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr9166.PNG"},{"id":310853,"rank":19,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1991/0066/figure-21.pdf","text":"Figure 21","linkFileType":{"id":1,"text":"pdf"}},{"id":310854,"rank":20,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1991/0066/figure-22.pdf","text":"Figure 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