{"pageNumber":"4862","pageRowStart":"121525","pageSize":"25","recordCount":165626,"records":[{"id":70012044,"text":"70012044 - 1981 - Geologic evidence for age of deposits at Hueyatlaco archeological site, Vasequillo, Mexico","interactions":[],"lastModifiedDate":"2025-07-10T16:09:41.203229","indexId":"70012044","displayToPublicDate":"2004-11-19T00:00:00","publicationYear":"1981","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":"Geologic evidence for age of deposits at Hueyatlaco archeological site, Vasequillo, Mexico","docAbstract":"<p><span>Direct tracing of beds during excavation in May 1973, confirmed that the artifact-bearing layers at Hueyatlaco underlie 10 m of fine-grained, water-laid deposits that constitute part of the wide-spread Valsequillo gravels. Dissection of these deposits by the adjacent Río Atoyac has reached a depth of 50 m. The stratigraphic section at Hueyatlaco includes four distinctive tephra units. The oldest one occupies a small channel in a series of cut-and-fill stream deposits that have yielded bifacial tools. It lies more than a meter above flat-lying, fine-grained beds from which edge-retouched tools have been recovered. The three other tephra units occur higher in the section.</span></p><p><span>Fission-track ages on zircon phenocrysts from two of the younger tephra layers (370,000 ± 200,000 and 600,000 ± 340,000 yr, 2σ) agree with concordant uranium-series dates for a camel pelvis that was found associated with bifacial tools at Hueyatlaco (245,000 ± 40,000 yr by&nbsp;<sup>230</sup>Th and &gt; 180,000 yr by&nbsp;<sup>231</sup>Pa). These dates are compatible with the depth of burial and subsequent dissection of the Hueyatlaco deposits, as well as with the degree of hydration of volcanic glass shards and with the extent of etching of heavy-mineral phenocrysts from within the tephra layers.</span></p><p><span>These findings suggest to us that further search for archaeological remains in deposits as old as those at Hueyatlaco would be warranted.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0033-5894(81)90124-1","issn":"00335894","usgsCitation":"Steen-McIntyre, V., Fryxell, R., and Malde, H., 1981, Geologic evidence for age of deposits at Hueyatlaco archeological site, Vasequillo, Mexico: Quaternary Research, v. 16, no. 1, p. 1-17, https://doi.org/10.1016/0033-5894(81)90124-1.","productDescription":"17 p.","startPage":"1","endPage":"17","costCenters":[],"links":[{"id":222690,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Mexico","otherGeospatial":"Vasequillo Reservoir","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -98.29516517583532,\n              18.987841319589492\n            ],\n            [\n              -98.29516517583532,\n              18.91375802729796\n            ],\n            [\n              -98.18568714858003,\n              18.91375802729796\n            ],\n            [\n              -98.18568714858003,\n              18.987841319589492\n            ],\n            [\n              -98.29516517583532,\n              18.987841319589492\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"16","issue":"1","noUsgsAuthors":false,"publicationDate":"2017-01-20","publicationStatus":"PW","scienceBaseUri":"505a1959e4b0c8380cd5596c","contributors":{"authors":[{"text":"Steen-McIntyre, V.","contributorId":75019,"corporation":false,"usgs":true,"family":"Steen-McIntyre","given":"V.","email":"","affiliations":[],"preferred":false,"id":362597,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fryxell, R.","contributorId":28369,"corporation":false,"usgs":true,"family":"Fryxell","given":"R.","email":"","affiliations":[],"preferred":false,"id":362595,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Malde, H.E.","contributorId":65863,"corporation":false,"usgs":true,"family":"Malde","given":"H.E.","affiliations":[],"preferred":false,"id":362596,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70012046,"text":"70012046 - 1981 - The sedimentary framework of the southern basin of Lake George, New York","interactions":[],"lastModifiedDate":"2025-07-10T16:02:22.249868","indexId":"70012046","displayToPublicDate":"2004-11-19T00:00:00","publicationYear":"1981","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":"The sedimentary framework of the southern basin of Lake George, New York","docAbstract":"<p>Information from 240 km of high-resolution seismic reflection profiles has been analyzed to show the bathymetric and subsurface configuration of southern Lake George in the southeastern corner of the Adirondack Mountains, New York. Three units have been identified and sampled in 13 piston cores as long as 7 m and 4 grab samples; they are glacial drift, glaciolacustrine nonorganic clay, and Holocene lake mud rich in organic material. Three deep bedrock basins controlled glacial, glaciolacustrine, and postglacial deposition within the lake. Glaciolacustrine clay is more than 30 m thick in these basins but is generally absent in water depths less than 20 m. An unconformity separates glaciolacustrine clay from overlying Holocene mud in water depths less than 30 m, but the contact is conformable and transitional in deeper water. The unconformity may have originated from subaqueous or subaerial erosion during a low stage of lake level which probably occurred between 10,000 and 700 yr B.P. Holocene lake mud is thin to absent in the shallower waters separating the three basins, but reaches 15-m thickness near the entrance to The Narrows. A new radiocarbon date of 6950 ?? 60 yr B.P. was obtained from a wood fragment which was found in the Holocene lake mud. We found no clear evidence of postglacial tectonic disturbances of the lake sediments although recent releveling profiles suggest that the Adirondack Mountains are undergoing contemporary uplift.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0033-5894(81)90113-7","issn":"00335894","usgsCitation":"Hutchinson, D.R., Ferrebee, W., Knebel, H., Wold, R.J., and Isachsen, Y., 1981, The sedimentary framework of the southern basin of Lake George, New York: Quaternary Research, v. 15, no. 1, p. 44-61, https://doi.org/10.1016/0033-5894(81)90113-7.","productDescription":"18 p.","startPage":"44","endPage":"61","costCenters":[],"links":[{"id":222692,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New York","otherGeospatial":"Lake George","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -73.58110291869816,\n              43.64789990422335\n            ],\n            [\n              -73.65171439763611,\n              43.59794917156913\n            ],\n            [\n              -73.73046377244945,\n              43.4200697402982\n            ],\n            [\n              -73.68460262645145,\n              43.41015708936362\n            ],\n            [\n              -73.6220769860821,\n              43.43945453274753\n            ],\n            [\n              -73.5869490296089,\n              43.54116883508024\n            ],\n            [\n              -73.46973033302903,\n              43.67093261922244\n            ],\n            [\n              -73.41074368762041,\n              43.816434774484236\n            ],\n            [\n              -73.43157011614562,\n              43.85257349011786\n            ],\n            [\n              -73.48697151047823,\n              43.78925842675548\n            ],\n            [\n              -73.58110291869816,\n              43.64789990422335\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"15","issue":"1","noUsgsAuthors":false,"publicationDate":"2017-01-20","publicationStatus":"PW","scienceBaseUri":"505bb004e4b08c986b324b89","contributors":{"authors":[{"text":"Hutchinson, D. R.","contributorId":31770,"corporation":false,"usgs":true,"family":"Hutchinson","given":"D.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":362600,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ferrebee, W.M.","contributorId":45312,"corporation":false,"usgs":true,"family":"Ferrebee","given":"W.M.","affiliations":[],"preferred":false,"id":362601,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Knebel, H.J.","contributorId":79092,"corporation":false,"usgs":true,"family":"Knebel","given":"H.J.","affiliations":[],"preferred":false,"id":362603,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wold, R. J.","contributorId":59503,"corporation":false,"usgs":true,"family":"Wold","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":362602,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Isachsen, Y.W.","contributorId":100528,"corporation":false,"usgs":true,"family":"Isachsen","given":"Y.W.","affiliations":[],"preferred":false,"id":362604,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":70012031,"text":"70012031 - 1981 - Obsidian hydration dating of volcanic events","interactions":[],"lastModifiedDate":"2025-07-10T16:18:43.958814","indexId":"70012031","displayToPublicDate":"2004-11-19T00:00:00","publicationYear":"1981","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":"Obsidian hydration dating of volcanic events","docAbstract":"<p>Obsidian hydration dating of volcanic events had been compared with ages of the same events determined by the <sup>14</sup>C and K-Ar methods at several localities. The localities, ranging in age from 1200 to over 1 million yr, include Newberry Craters, Oregon; Coso Hot Springs, California; Salton Sea, California; Yellowstone National Park, Wyoming; and Mineral Range, Utah. In most cases the agreement is quite good. A number of factors including volcanic glass composition and exposure-temperature history must be known in order to relate hydration thickness to age. The effect of composition can be determined from chemical analysis or the refractive index of the glass. Exposure-temperature history requires a number of considerations enumerated in this paper.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0033-5894(81)90126-5","issn":"00335894","usgsCitation":"Friedman, I., and Obradovich, J., 1981, Obsidian hydration dating of volcanic events: Quaternary Research, v. 16, no. 1, p. 37-47, https://doi.org/10.1016/0033-5894(81)90126-5.","productDescription":"11 p.","startPage":"37","endPage":"47","costCenters":[],"links":[{"id":222511,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, Oregon, Utah, Wyoming","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -124.6475160525464,\n              46.20771992929792\n            ],\n            [\n              -125.1003791369465,\n              40.17349401689333\n            ],\n            [\n              -122.29600040357937,\n              34.82675722442707\n            ],\n            [\n              -116.74416409105484,\n              32.3984406460912\n            ],\n            [\n              -114.57430674803186,\n              32.944375104035416\n            ],\n            [\n              -114.78200635517106,\n              36.4861323329432\n            ],\n            [\n              -108.61253629515322,\n              37.15955344593477\n            ],\n            [\n              -108.66922526809813,\n              40.843670668884684\n            ],\n            [\n              -104.26862126283552,\n              41.09844303976675\n            ],\n            [\n              -103.98990367317387,\n              44.97956854547027\n            ],\n            [\n              -111.0309803408683,\n              44.86850389437278\n            ],\n            [\n              -111.21537759882554,\n              42.146710134492714\n            ],\n            [\n              -114.11252686220469,\n              41.93536025488858\n            ],\n            [\n              -114.8348805138175,\n              35.70503682526824\n            ],\n            [\n              -119.66879055671411,\n              39.084468849710476\n            ],\n            [\n              -120.27217606595909,\n              41.93688186236618\n            ],\n            [\n              -117.01575185687031,\n              41.93878648474629\n            ],\n            [\n              -116.56102846133165,\n              45.94050702489267\n            ],\n            [\n              -124.6475160525464,\n              46.20771992929792\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"16","issue":"1","noUsgsAuthors":false,"publicationDate":"2017-01-20","publicationStatus":"PW","scienceBaseUri":"505a6b03e4b0c8380cd74492","contributors":{"authors":[{"text":"Friedman, I.","contributorId":95596,"corporation":false,"usgs":true,"family":"Friedman","given":"I.","email":"","affiliations":[],"preferred":false,"id":362568,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Obradovich, J.","contributorId":53953,"corporation":false,"usgs":true,"family":"Obradovich","given":"J.","email":"","affiliations":[],"preferred":false,"id":362567,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70011738,"text":"70011738 - 1981 - Canyon Creek: A late Pleistocene vertebrate locality in interior Alaska","interactions":[],"lastModifiedDate":"2025-07-10T16:29:25.653401","indexId":"70011738","displayToPublicDate":"2004-11-19T00:00:00","publicationYear":"1981","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":"Canyon Creek: A late Pleistocene vertebrate locality in interior Alaska","docAbstract":"<p><span>The Canyon Creek vertebrate-fossil locality is an extensive road cut near Fairbanks that exposes sediments that range in age from early Wisconsin to late Holocene. Tanana River gravel at the base of the section evidently formed during the Delta Glaciation of the north-central Alaska Range. Younger layers and lenses of fluvial sand are interbedded with arkosic gravel from Canyon Creek that contains tephra as well as fossil bones of an interstadial fauna about 40,000 years old. Solifluction deposits containing ventifacts, wedge casts, and rodent burrows formed during a subsequent period of periglacial activity that took place during the maximum phase of Donnelly Glaciation about 25,000–17,000 years ago. Overlying sheets of eolian sand are separated by a 9500-year-old paleosol that may correlate with a phase of early Holocene spruce expansion through central Alaska. The Pleistocene fauna from Canyon Creek consists of rodents (indicated by burrows),&nbsp;</span><i>Mammuthus primigenius</i><span>&nbsp;(woolly mammoth),&nbsp;</span><i>Equus lambei</i><span>&nbsp;(Yukon wild ass),&nbsp;</span><i>Camelops hesternus</i><span>&nbsp;(western camel),&nbsp;</span><i>Bison</i><span>&nbsp;sp. cf.&nbsp;</span><i>B. crassicornis</i><span>&nbsp;(large-horned bison),&nbsp;</span><i>Ovis</i><span>&nbsp;sp. cf.</span><i>O. dalli</i><span>&nbsp;(mountain sheep),&nbsp;</span><i>Canis</i><span>&nbsp;sp. cf.&nbsp;</span><i>C. lupus</i><span>&nbsp;(wolf),&nbsp;</span><i>Lepus</i><span>&nbsp;sp. cf.&nbsp;</span><i>L. othus</i><span>&nbsp;or&nbsp;</span><i>L. arcticus</i><span>&nbsp;(tundra hare), and&nbsp;</span><i>Rangifer</i><span>&nbsp;sp. (caribou). This assemblage suggests an open landscape in which trees and tall shrubs were either absent or confined to sheltered and moist sites.&nbsp;</span><i>Camelops</i><span>&nbsp;evidently was present in eastern Beringia during the middle Wisconsin interstadial interval but may have disappeared during the following glacial episode. The stratigraphic section at Canyon Creek appears to demonstrate that the Delta Glaciation of the north-central Alaska Range is at least in part of early Wisconsin age and was separated from the succeeding Donnelly Glaciation by an interstadial rather than interglacial episode.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0033-5894(81)90043-0","issn":"00335894","usgsCitation":"Weber, F.R., Hamilton, T.D., Hopkins, D., Repenning, C., and Haas, H., 1981, Canyon Creek: A late Pleistocene vertebrate locality in interior Alaska: Quaternary Research, v. 16, no. 2, p. 167-180, https://doi.org/10.1016/0033-5894(81)90043-0.","productDescription":"14 p.","startPage":"167","endPage":"180","costCenters":[],"links":[{"id":220787,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"north-central Alaska Range","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -150.32186007264718,\n              65.94098893598314\n            ],\n            [\n              -150.32186007264718,\n              64.33338352969466\n            ],\n            [\n              -145.35284620275706,\n              64.33338352969466\n            ],\n            [\n              -145.35284620275706,\n              65.94098893598314\n            ],\n            [\n              -150.32186007264718,\n              65.94098893598314\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"16","issue":"2","noUsgsAuthors":false,"publicationDate":"2017-01-20","publicationStatus":"PW","scienceBaseUri":"5059f347e4b0c8380cd4b6eb","contributors":{"authors":[{"text":"Weber, F. R.","contributorId":105303,"corporation":false,"usgs":true,"family":"Weber","given":"F.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":361847,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hamilton, T. D.","contributorId":36921,"corporation":false,"usgs":true,"family":"Hamilton","given":"T.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":361844,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hopkins, D.M.","contributorId":103646,"corporation":false,"usgs":true,"family":"Hopkins","given":"D.M.","email":"","affiliations":[],"preferred":false,"id":361846,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Repenning, C.A.","contributorId":56700,"corporation":false,"usgs":true,"family":"Repenning","given":"C.A.","affiliations":[],"preferred":false,"id":361845,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Haas, H.","contributorId":27192,"corporation":false,"usgs":true,"family":"Haas","given":"H.","email":"","affiliations":[],"preferred":false,"id":361843,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":70012109,"text":"70012109 - 1981 - Dated wood from Alaska and the Yukon: Implications for forest refugia in Beringia","interactions":[],"lastModifiedDate":"2025-07-11T13:25:38.335813","indexId":"70012109","displayToPublicDate":"2004-11-19T00:00:00","publicationYear":"1981","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":"Dated wood from Alaska and the Yukon: Implications for forest refugia in Beringia","docAbstract":"<p>Postulations on the existence of forest refugia in parts of Beringia during the last glacial have been, in large part, based on ambiguous evidence. Existing data on radiocarbon-dated and identified fossil wood and macrofossils from Alaska and northwest Canada are synthesized here and are augmented by results of palynological studies in an effort to show the persistence of some, and total extinction of other, tree and large shrub species. Possible dispersal routes taken by species that reinvaded Beringia in postglacial times are also reconstructed from the fossil record. Macrofossil and pollen evidence, when combined with climatic factors, makes cottonwood a good candidate for survival during the last glacial. Larch and aspen are also candidates, though the evidence for them is less positive. Pollen and macrofossils of alder are very scarce in deposits of the last glacial age, and if it survived at all, it was probably in very isolated vegetatively reproducing clones. Shrub birch may have been present in Beringia, but tree birch probably was reintroduced during the Holocene. Spruce also appears to have been absent in Alaska from about 30,000 to 11,500 yr ago and probably reinvaded Beringia from a refugium south of the Laurentide ice sheet.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0033-5894(81)90028-4","issn":"00335894","usgsCitation":"Hopkins, D., Smith, P., and Matthews, J., 1981, Dated wood from Alaska and the Yukon: Implications for forest refugia in Beringia: Quaternary Research, v. 15, no. 3, p. 217-249, https://doi.org/10.1016/0033-5894(81)90028-4.","productDescription":"33 p.","startPage":"217","endPage":"249","costCenters":[],"links":[{"id":221989,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.er.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada, Russia, United States","state":"Alaska","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -179.99,\n              70.56085858763808\n            ],\n            [\n              -179.99,\n              61.24556255904437\n            ],\n            [\n              -139.71319537741883,\n              61.24556255904437\n            ],\n            [\n              -139.71319537741883,\n              70.56085858763808\n            ],\n            [\n              -179.99,\n              70.56085858763808\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"15","issue":"3","noUsgsAuthors":false,"publicationDate":"2017-01-20","publicationStatus":"PW","scienceBaseUri":"5059fddde4b0c8380cd4e996","contributors":{"authors":[{"text":"Hopkins, D.M.","contributorId":103646,"corporation":false,"usgs":true,"family":"Hopkins","given":"D.M.","email":"","affiliations":[],"preferred":false,"id":362755,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Smith, P.A.","contributorId":86795,"corporation":false,"usgs":true,"family":"Smith","given":"P.A.","email":"","affiliations":[],"preferred":false,"id":362754,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Matthews, J.V. Jr.","contributorId":72931,"corporation":false,"usgs":true,"family":"Matthews","given":"J.V.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":362753,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70011753,"text":"70011753 - 1981 - The terminal Eocene event and the Polish connection","interactions":[],"lastModifiedDate":"2025-06-16T23:14:42.593139","indexId":"70011753","displayToPublicDate":"2003-04-15T00:00:00","publicationYear":"1981","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":"The terminal Eocene event and the Polish connection","docAbstract":"<p><span>The Eocene/Oligocene boundary in Europe is marked by major discontinuities in all environments: the “Grande Coupure” in continental mammals; the elimination of semitropical elements from high-latitude floras; the virtually complete replacement of the shallow-marine malacofauna; and an extraordinary downslope excursion of carbonate deposition in deep-ocean basins (drop in the CCD). These phenomena collectively represent the “Terminal Eocene Event” (TEE). In the Carpathian Mountains, the TEE is manifested in the thin but regionally persistent&nbsp;</span><i>Globigerina</i><span>&nbsp;Marl, a calcareous unit containing abundant cool-water microplankton that occurs within very thick, siliceous, bathyal flysch sequences. In southern Poland, the marl is of very latest Eocene age, within planktonic foraminifera zone P17, calcareous nannoplankton zone NP19/20, and the zone of the dinoflagellate&nbsp;</span><i>Rhomdodinium perforatum</i><span>. Zircons from bentonites bracketing the marl are dated by fission-track analysis; at Polany, two underlying bentonites are 41.7 and 39.8 Ma, and at Znamirowice two overlying bentonites are 34.6 and 28.9 Ma, in sequence. This accords with glauconite K/Ar ages in Western Europe by which the Eo/Oligocene boundary age is estimated at 37–38 Ma. Global correlations indicate that the TEE corresponds to a major glacio-eustatic regression with a duration of about 0.5 Ma, in which a large Antarctic ice cap was formed, the ocean circulation was permanently changed to the psychrospheric condition, and world climate shifted irreversibly towards the modern state.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0031-0182(81)90111-5","issn":"00310182","usgsCitation":"Van Couvering, J.A., Aubry, M., Berggren, W., Bujak, J., Naeser, C.W., and Wieser, T., 1981, The terminal Eocene event and the Polish connection: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 36, no. 3-4, p. 321-362, https://doi.org/10.1016/0031-0182(81)90111-5.","productDescription":"42 p.","startPage":"321","endPage":"362","costCenters":[],"links":[{"id":221251,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Poland","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              14.337657367927704,\n              54.012571323156635\n            ],\n            [\n              14.337657367927704,\n              49.28513872073813\n            ],\n            [\n              24.006473984938538,\n              49.28513872073813\n            ],\n            [\n              24.006473984938538,\n              54.012571323156635\n            ],\n            [\n              14.337657367927704,\n              54.012571323156635\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"36","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb0eee4b08c986b325132","contributors":{"authors":[{"text":"Van Couvering, J. A.","contributorId":78469,"corporation":false,"usgs":true,"family":"Van Couvering","given":"J.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":361883,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Aubry, M.-P.","contributorId":100121,"corporation":false,"usgs":true,"family":"Aubry","given":"M.-P.","email":"","affiliations":[],"preferred":false,"id":361884,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Berggren, W.A.","contributorId":65601,"corporation":false,"usgs":true,"family":"Berggren","given":"W.A.","email":"","affiliations":[],"preferred":false,"id":361882,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bujak, J.P.","contributorId":49928,"corporation":false,"usgs":true,"family":"Bujak","given":"J.P.","email":"","affiliations":[],"preferred":false,"id":361881,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Naeser, C. W.","contributorId":17582,"corporation":false,"usgs":true,"family":"Naeser","given":"C.","middleInitial":"W.","affiliations":[],"preferred":false,"id":361880,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Wieser, T.","contributorId":107430,"corporation":false,"usgs":true,"family":"Wieser","given":"T.","email":"","affiliations":[],"preferred":false,"id":361885,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}}
,{"id":70011929,"text":"70011929 - 1981 - Aftershocks of the June 20, 1978, Greece earthquake: A multimode faulting sequence","interactions":[],"lastModifiedDate":"2025-08-28T16:43:12.995589","indexId":"70011929","displayToPublicDate":"2003-04-11T00:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Aftershocks of the June 20, 1978, Greece earthquake: A multimode faulting sequence","docAbstract":"<p>A 10-station portable seismograph network was deployed in northern Greece to study aftershocks of the magnitude (m<sub>b</sub>) 6.4 earthquake of June 20, 1978. The main shock occurred (in a graben) about 25 km northeast of the city of Thessaloniki and caused an east-west zone of surface rupturing 14 km long that splayed to 7 km wide at the west end. The hypocenters for 116 aftershocks in the magnitude range from 2.5 to 4.5 were determined. The epicenters for these events cover an area 30 km (east-west) by 18 km (north-south), and focal depths ranges from 4 to 12 km. Most of the aftershocks in the east half of the aftershock zone are north of the surface rupture and north of the graben. Those in the west half are located within the boundaries of the graben. Composite focalmechanism solutions for selected aftershocks indicate reactivation of geologically mapped normal faults in the area. Also, strike-slip and dip-slip faults that splay off the western end of the zone of surface ruptures may have been activated. </p><p>The epicenters for four large (M <i><span>≯</span></i>&nbsp; 4.8) foreshocks and the main shock were relocated using the method of joint epicenter determination. <span>Collectively, those five epicenters form an arcuate pattern convex southward, that is north of and 5 km distant from the surface rupturing. The 5-km separation, along with a focal depth of 8 km (average aftershock depth) or 16 km (NEIS main-shock depth), implies that the fault plane dips northward 58° or 73°, respectively. A preferred nodal-plane dip of 36° was determined by B.C. Papazachos and his colleagues in 1979 from a focal-mechanism solution for the main shock. If this dip is valid for the causal fault and that fault projects to the zone of surface rupturing, a decrease of dip with depth is required.</span> </p>","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(81)90222-5","issn":"00401951","usgsCitation":"Carver, D., and Bollinger, G.A., 1981, Aftershocks of the June 20, 1978, Greece earthquake: A multimode faulting sequence: Tectonophysics, v. 73, no. 4, p. 343-363, https://doi.org/10.1016/0040-1951(81)90222-5.","productDescription":"21 p.","startPage":"343","endPage":"363","costCenters":[],"links":[{"id":220943,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Greece","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              19.603655068347535,\n              41.173821485620664\n            ],\n            [\n              19.603655068347535,\n              34.8323066303216\n            ],\n            [\n              30.50271328108795,\n              34.8323066303216\n            ],\n            [\n              30.50271328108795,\n              41.173821485620664\n            ],\n            [\n              19.603655068347535,\n              41.173821485620664\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"73","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e8d3e4b0c8380cd47ed0","contributors":{"authors":[{"text":"Carver, David","contributorId":55867,"corporation":false,"usgs":true,"family":"Carver","given":"David","affiliations":[],"preferred":false,"id":362320,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bollinger, G. A.","contributorId":55809,"corporation":false,"usgs":true,"family":"Bollinger","given":"G.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":362321,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70012140,"text":"70012140 - 1981 - Monoclinal bending of strata over laccolithic intrusions","interactions":[],"lastModifiedDate":"2025-08-28T16:05:58.647293","indexId":"70012140","displayToPublicDate":"2003-04-11T00:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Monoclinal bending of strata over laccolithic intrusions","docAbstract":"<p>Sedimentary strata on top of some laccolithic intrusions are nearly horizontal and little deformed, but are bent into steeply dipping monoclinal flexures over the peripheries of these intrusions. This form of bending is not explained by previous theories of laccolithic intrusion, which predict either horizontal undeformed strata over the center and faulted strata around the periphery, or strata bent continuously into a dome. However, a slight generalization of these theories accomodates the observed form and contains the previous forms as special cases. A critical assumption is that the strength of contacts within a multilayered overburden is overcome locally by layer-parallel shear. If this strength is less than the strength of the layers themselves, then layers over the center remain bonded together and display negligible bending, whereas layers over the periphery slip over one another and are readily bent into a monoclinal flexure.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(81)90189-X","issn":"00401951","usgsCitation":"Koch, F., Johnson, A., and Pollard, D.D., 1981, Monoclinal bending of strata over laccolithic intrusions: Tectonophysics, v. 74, no. 3-4, p. T21-T31, https://doi.org/10.1016/0040-1951(81)90189-X.","productDescription":"11 p.","startPage":"T21","endPage":"T31","costCenters":[],"links":[{"id":222395,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana, Utah","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -116.17491498728086,\n              48.9300297085812\n            ],\n            [\n              -112.95751598788759,\n              44.41755548853673\n            ],\n            [\n              -114.07822001812934,\n              36.917553018566466\n            ],\n            [\n              -108.84171548483499,\n              37.02156091708791\n            ],\n            [\n              -109.06142031682796,\n              40.952898801320174\n            ],\n            [\n              -111.17810860385198,\n              41.064834275515466\n            ],\n            [\n              -111.04695625836439,\n              42.00274969440763\n            ],\n            [\n              -111.11329314135119,\n              44.665083717871184\n            ],\n            [\n              -104.12181366847273,\n              45.05841955531777\n            ],\n            [\n              -102.93005817792101,\n              49.08533992232094\n            ],\n            [\n              -116.17491498728086,\n              48.9300297085812\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"74","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a5e01e4b0c8380cd70741","contributors":{"authors":[{"text":"Koch, F.G.","contributorId":65992,"corporation":false,"usgs":true,"family":"Koch","given":"F.G.","email":"","affiliations":[],"preferred":false,"id":362838,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, A. M.","contributorId":48903,"corporation":false,"usgs":true,"family":"Johnson","given":"A. M.","affiliations":[],"preferred":false,"id":362837,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pollard, D. D.","contributorId":72914,"corporation":false,"usgs":false,"family":"Pollard","given":"D.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":362839,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70012003,"text":"70012003 - 1981 - Gravitational potential as a source of earthquake energy","interactions":[],"lastModifiedDate":"2025-08-28T16:26:54.224528","indexId":"70012003","displayToPublicDate":"2003-04-10T00:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Gravitational potential as a source of earthquake energy","docAbstract":"<p>Some degree of tectonic stress within the earth originates from gravity acting upon density structures. The work performed by this \"gravitational tectonics stress\" must have formerly existed as gravitational potential energy contained in the stress-causing density structure. </p><p>According to the elastic rebound theory (Reid, 1910), the energy of earthquakes comes <i>from</i> an elastic strain field built up by fairly continuous elastic deformation in the period between events. For earthquakes resulting from gravitational tectonic stress, the elastic rebound theory requires the transfer of energy from the gravitational potential of the density structures into an elastic strain field prior to the event. </p><p>An alternate theory involves partial gravitational collapse of the stress-causing density structures. The earthquake energy comes directly from a net decrease in gravitational potential energy. The gravitational potential energy released at the time of the earthquake is split between the energy released by the earthquake, including work done in the fault zone and an increase in stored elastic strain energy. The stress associated with this elastic strain field should oppose further fault slip.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(81)90099-8","issn":"00401951","usgsCitation":"Barrows, L., and Langer, C., 1981, Gravitational potential as a source of earthquake energy: Tectonophysics, v. 76, no. 3-4, p. 237-255, https://doi.org/10.1016/0040-1951(81)90099-8.","productDescription":"19 p.","startPage":"237","endPage":"255","costCenters":[],"links":[{"id":220947,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -152.82909139827177,\n              60.75688602127542\n            ],\n            [\n              -154.84314000653433,\n              56.4305698481941\n            ],\n            [\n              -130.29098685632363,\n              54.609293746212245\n            ],\n            [\n              -134.61406544497407,\n              59.69136621447214\n            ],\n            [\n              -139.0373454219875,\n              60.34205568151435\n            ],\n            [\n              -140.87681925326558,\n              60.30571659534989\n            ],\n            [\n              -141.4540937541834,\n              61.2283677590821\n            ],\n            [\n              -143.01672736053365,\n              61.860875577040616\n            ],\n            [\n              -149.3868345984696,\n              62.348234765872405\n            ],\n            [\n              -152.82909139827177,\n              60.75688602127542\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"76","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a29f2e4b0c8380cd5ad8e","contributors":{"authors":[{"text":"Barrows, L.","contributorId":76885,"corporation":false,"usgs":true,"family":"Barrows","given":"L.","email":"","affiliations":[],"preferred":false,"id":362495,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Langer, C.J.","contributorId":31395,"corporation":false,"usgs":true,"family":"Langer","given":"C.J.","email":"","affiliations":[],"preferred":false,"id":362494,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70011989,"text":"70011989 - 1981 - Contemporary doming of the Adirondack Mountains: Further evidence from releveling","interactions":[],"lastModifiedDate":"2025-08-28T16:33:24.753325","indexId":"70011989","displayToPublicDate":"2003-04-08T00:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Contemporary doming of the Adirondack Mountains: Further evidence from releveling","docAbstract":"<p><span>The Adirondack Mountains constitute an anomalously large, domical uplift on the Appalachian foreland. The dome has a NNE—SSW axis about 190 km long, and an east—west dimension of about 140 km. It has a structural relief of at least 1600 m, and a local topographic relief of up to 1200 m. First-order leveling in 1955, and again in 1973 along a north—south line at the eastern margin of the Adirondack shows an uplift rate of 2.2 mm/yr at the latitude of the center of the dome and a subsidence rate of 2.8 mm/yr at the northern end of the line near the Canadian border. The net amount of arching along this releveled line is 9&nbsp;</span><i>cm</i><span>&nbsp;± 2&nbsp;</span><i>cm</i><span>&nbsp;(Isachsen, 1975). To test the idea that this arching represented an “edge effect” of contemporary doming of the Adirondacks as a whole, the National Geodetic Survey was encouraged to relevel a 1931 north—south line between Utica and Fort Covington (near the Canadian border) which crosses the center of the dome. The releveling showed that the mountain mass is undergoing contemporary domical uplift at a rate which reaches 3.7 mm/yr near the center of the dome (compare with 1 mm/yr for the Swiss Alps). Three other releveled lines in the area support this conclusion.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(81)90051-2","issn":"00401951","usgsCitation":"Isachsen, Y., 1981, Contemporary doming of the Adirondack Mountains: Further evidence from releveling: Tectonophysics, v. 71, no. 1-4, p. 95-96, https://doi.org/10.1016/0040-1951(81)90051-2.","productDescription":"2 p.","startPage":"95","endPage":"96","costCenters":[],"links":[{"id":220732,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New York","otherGeospatial":"Adirondack Mountains","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -75.08632613930284,\n              44.849722542694394\n            ],\n            [\n              -75.68357029846126,\n              44.12534350539521\n            ],\n            [\n              -75.11834401539436,\n              43.137593153404055\n            ],\n            [\n              -73.6455352174284,\n              43.04799214874441\n            ],\n            [\n              -73.31377725183206,\n              44.32023495222312\n            ],\n            [\n              -73.6455352174284,\n              44.89509467289085\n            ],\n            [\n              -75.08632613930284,\n              44.849722542694394\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"71","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059fa4ce4b0c8380cd4da21","contributors":{"authors":[{"text":"Isachsen, Y.W.","contributorId":100528,"corporation":false,"usgs":true,"family":"Isachsen","given":"Y.W.","affiliations":[],"preferred":false,"id":362460,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70012108,"text":"70012108 - 1981 - Plumbotectonics-the model","interactions":[],"lastModifiedDate":"2025-08-28T16:12:38.239092","indexId":"70012108","displayToPublicDate":"2003-04-07T00:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Plumbotectonics-the model","docAbstract":"<p>Plumbotectonics is an attempt to model the geochemical behaviour of U, Th and Pb, among major terrestrial reservoirs in agreement with observational data. By recycling rock through the orogenic environment, a dynamically communicating upper crust, lower crust, and mantle can produce the required patterns of lead-isotope evolution.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(81)90213-4","issn":"00401951","usgsCitation":"Zartman, R., and Doe, B.R., 1981, Plumbotectonics-the model: Tectonophysics, v. 75, no. 1-2, p. 135-162, https://doi.org/10.1016/0040-1951(81)90213-4.","productDescription":"28 p.","startPage":"135","endPage":"162","costCenters":[],"links":[{"id":221988,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"75","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a7c94e4b0c8380cd79a76","contributors":{"authors":[{"text":"Zartman, R. E.","contributorId":15632,"corporation":false,"usgs":true,"family":"Zartman","given":"R. E.","affiliations":[],"preferred":false,"id":362751,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Doe, B. R.","contributorId":52173,"corporation":false,"usgs":true,"family":"Doe","given":"B.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":362752,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70012107,"text":"70012107 - 1981 - Composition of the earth's upper mantle-I. Siderophile trace elements in ultramafic nodules","interactions":[],"lastModifiedDate":"2025-08-28T16:18:02.199665","indexId":"70012107","displayToPublicDate":"2003-04-07T00:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Composition of the earth's upper mantle-I. Siderophile trace elements in ultramafic nodules","docAbstract":"<p><span>Seven siderophile elements (Au, Ge, Ir, Ni, Pd, Os, Re) were determined by radiochemical neutron activation analysis in 19 ultramafic rocks, which are spinel lherzollites-xenoliths from North and Central America, Hawaii and Australia, and garnet Iherzolitexenoliths from Lesotho.</span></p><p><span>Abundances of the platinum metals are very uniform in spinel lherzolites averaging 3.4 ± 1.2 ppb Os, 3.7 ± 1.1 ppb Ir, and 4.6 ± 2.0 ppb Pd. Sheared garnet lherzolite PHN 1611 has similar abundances of these elements, but in 4 granulated garnet lherzolites, abundances are more variable. In all samples, the Pt metals retain cosmic ( Cl-chondrite) ratios. Abundances of Au and Re vary more than those of Pt metals, but the Au/Re ratio remains close to the cosmic value. The fact that higher values of Au and Re approach cosmic proportions with respect to the Pt metals, suggests that Au and Re have been depleted in some ultramafic rocks from an initially chondrite-like pattern equivalent to about 0.01 of Cl chondrite abundances. The relative enrichment of Au and Re in crustal rocks is apparently the result of crust—mantle fractionation and does not require a special circumstance of core—mantle partitioning.</span></p><p><span>Abundances of moderately volatile elements Ni, Co and Ge are very uniform in all rocks, and are much higher than those of the highly siderophile elements Au, Ir, Pd, Os and Re. When normalized to Cl chondrites, abundances of Ni and Co are nearly identical, averaging 0.20 ± 0.02 and 0.22 ± 0.02, respectively; but Ge is only 0.027 ± 0.004. The low abundance of Ge relative to Ni and Co is apparently a reflection of the general depletion of volatile elements in the Earth. The moderately siderophile elements cannot be derived from the same source as the highly siderophile elements because of the marked difference in Cl chondrite-normalized abundances and patterns. We suggest that most of the Ni, Co and Ge were enriched in the silicate by the partial oxidation of pre-existing volatile-poor Fe-Ni, whereas the corresponding highly siderophile elements remained sequestered by the surviving metal. The highly siderophile elements may have been introduced by a population of ~10<sup>3</sup>&nbsp;large (~10<sup>22</sup>&nbsp;g) planetisimals, similar to those forming the lunar mare basins.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(81)90209-2","issn":"00401951","usgsCitation":"Morgan, J.W., Wandless, G., Petrie, R., and Irving, A., 1981, Composition of the earth's upper mantle-I. Siderophile trace elements in ultramafic nodules: Tectonophysics, v. 75, no. 1-2, p. 47-67, https://doi.org/10.1016/0040-1951(81)90209-2.","productDescription":"21 p.","startPage":"47","endPage":"67","costCenters":[],"links":[{"id":221930,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"75","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f92ee4b0c8380cd4d4ab","contributors":{"authors":[{"text":"Morgan, J. W.","contributorId":92384,"corporation":false,"usgs":true,"family":"Morgan","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":362749,"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":362750,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Petrie, R.K.","contributorId":87266,"corporation":false,"usgs":true,"family":"Petrie","given":"R.K.","email":"","affiliations":[],"preferred":false,"id":362748,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Irving, A.J.","contributorId":51022,"corporation":false,"usgs":true,"family":"Irving","given":"A.J.","email":"","affiliations":[],"preferred":false,"id":362747,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":70011853,"text":"70011853 - 1981 - Vertebrate fossil-bearing paleosol units (Willwood Formation, Lower Eocene, Northwest Wyoming, U.S.A.): Implications for taphonomy, biostratigraphy, and assemblage analysis","interactions":[],"lastModifiedDate":"2025-06-16T22:53:40.305425","indexId":"70011853","displayToPublicDate":"2003-04-04T00:00:00","publicationYear":"1981","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":"Vertebrate fossil-bearing paleosol units (Willwood Formation, Lower Eocene, Northwest Wyoming, U.S.A.): Implications for taphonomy, biostratigraphy, and assemblage analysis","docAbstract":"<p>In the lower 300 m of the fluvial Willwood Formation of northwest Wyoming, most large concentrations of vertebrate fossils consist of disarticulated and broken skeletal remains that occur in widespread, tubular, thin (2 cm-1 m) greenish- and bluish-gray mudstones that are low in percentage of free iron, aluminum, and manganese, relatively high in percentages of organic carbon, and often show evidence of clay eluviation. These units lie atop sesquioxide-rich, sometimes clay-illuviated variegated unit (red, yellow, purple, and mottled variants) and are relicts of the A horizons of podzolic spodosols (aquods). </p><p>The wide distribution of bone fragments, the numerical proportions of bone elements, weathering of the fragments, and biogenic evidence indicate the vertebrate remains accumulated gradually as litter on the surface of the soils and became incorporated into the A horizon. The bones were disarticulated, broken, and otherwise disturbed by the action of scavengers prior to burial. Occurrence of abundant vertebrate remains in discrete, readily identifiable, and widespread paleosol units makes these units valuable biostratigraphic markers (zonules, faunules). Evidence of geologically short-term lag accumulation of the bones is important to assemblage analysis; the paleosol concentrations result from attritional mortalities that more closely reflect composition of the life assemblage than do remains concentrated by fluvial transport or predators.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0031-0182(81)90057-2","issn":"00310182","usgsCitation":"Bown, T.M., and Kraus, M.J., 1981, Vertebrate fossil-bearing paleosol units (Willwood Formation, Lower Eocene, Northwest Wyoming, U.S.A.): Implications for taphonomy, biostratigraphy, and assemblage analysis: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 34, p. 31-56, https://doi.org/10.1016/0031-0182(81)90057-2.","productDescription":"26 p.","startPage":"31","endPage":"56","costCenters":[],"links":[{"id":221780,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wyoming","otherGeospatial":"northwest Wyoming","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -109.27505184504837,\n              44.99057640111633\n            ],\n            [\n              -109.27505184504837,\n              43.52185648052293\n            ],\n            [\n              -107.05063593252248,\n              43.52185648052293\n            ],\n            [\n              -107.05063593252248,\n              44.99057640111633\n            ],\n            [\n              -109.27505184504837,\n              44.99057640111633\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"34","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bc22ae4b08c986b32a97c","contributors":{"authors":[{"text":"Bown, T. M.","contributorId":106858,"corporation":false,"usgs":true,"family":"Bown","given":"T.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":362122,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kraus, M. J.","contributorId":44605,"corporation":false,"usgs":false,"family":"Kraus","given":"M.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":362121,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70011790,"text":"70011790 - 1981 - A process-sedimentary framework for characterizing recent and ancient sabkhas","interactions":[],"lastModifiedDate":"2025-07-24T15:36:24.299431","indexId":"70011790","displayToPublicDate":"2003-04-04T00:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3368,"text":"Sedimentary Geology","active":true,"publicationSubtype":{"id":10}},"title":"A process-sedimentary framework for characterizing recent and ancient sabkhas","docAbstract":"<p><span>The discovery of sabkha environments during the 1960's, marked the beginning of Recent evaporite sedimentological studies and their perception as models for facies analysis. However, variation among Recent sabkhas, though recognized by the geologic community, has not been duly addressed, which has resulted in overuse of the Trucial Coast model in comparative sedimentological studies. Knowledge of the dominant physical processes which determine sabkha morphology, and of the sedimentary response to those processes, can lead to a fundamental understanding of a sabkha's origin and of how it differs from other sabkhas.</span></p><p><span>Physical processes thought to be most important (besides evaporation) include those operative under: (1) marine-; (2) fluvial-lacustrine-; and (3) eolian-dominated conditions. Dominance of one or more of these in the proper settings give rise to marine coastal sabkhas, continental playas, and interdune sabkhas.</span></p><p><span>Sedimentary responses to dominant physical processes lead to the development of sabkhas consisting of a combination of either: (1) terrigenous clastics; (2) carbonate-sulfate (anhydrite-gypsum) minerals; or (3) soluble salts (halite, sylvite, polyhalite, etc.). Sediment characterization can also allow discrimination of the range or compositional variety in, for example, coastal sabkhas.</span></p><p><span>Where applied to the stratigraphic record, this classification system may help unravel the sedimentary history of an ancient sabkha system, and a determination of the dominant physical processes that ruled its development.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0037-0738(81)90023-3","issn":"00370738","usgsCitation":"Handford, C., 1981, A process-sedimentary framework for characterizing recent and ancient sabkhas: Sedimentary Geology, v. 30, no. 4, p. 255-265, https://doi.org/10.1016/0037-0738(81)90023-3.","productDescription":"11 p.","startPage":"255","endPage":"265","costCenters":[],"links":[{"id":220789,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"30","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e50de4b0c8380cd46acd","contributors":{"authors":[{"text":"Handford, C.R.","contributorId":19705,"corporation":false,"usgs":true,"family":"Handford","given":"C.R.","email":"","affiliations":[],"preferred":false,"id":361965,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70011777,"text":"70011777 - 1981 - Late Cenozoic marine deposition in the United States Atlantic Coastal Plain related to tectonism and global climate","interactions":[],"lastModifiedDate":"2025-06-16T23:07:35.293923","indexId":"70011777","displayToPublicDate":"2003-04-04T00:00:00","publicationYear":"1981","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":"Late Cenozoic marine deposition in the United States Atlantic Coastal Plain related to tectonism and global climate","docAbstract":"<p><span>Major hiatuses in upper Cenozoic marine deposits in the United States Atlantic Coastal Plain are recognized on the basis of molluscan faunal changes at erosional unconformities. These hiatuses generally coincided with periods of global cooling and ice sheet formation. Such hiatuses provide information to supplement global climatic data. Major hiatuses are recognized within the early Miocene (23-20 m.y. ago), at the end of the middle Miocene (∼ 11-10 m.y. ago), at the end of the late Miocene (∼6.5-5 m.y. ago), at the end of the early Pliocene (∼4.0–2.5 m.y. ago), at the end of the late Pliocene (∼1.9 or 1.8 m.y. ago), within the Pleistocene (∼1.1-0.5 m.y. ago) and several times within the last 0.4 m.y.</span></p><p><span>Estimates of the amount of water contained in ice sheets at different times in the Pliocene and Pleistocene facilitate calculation of probable minimum sea levels on the Coastal Plain during different high stands of the sea. The altitudes of dated shoreline deposits in the Atlantic Coastal Plain show that the amount of uplift in the Cape Fear area has averaged at least 1.3 cm per 1000 years since the beginning of Pliocene time. The Coastal Plain of Georgia has apparently experienced relatively little vertical deformation during this same time.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0031-0182(81)90059-6","issn":"00310182","usgsCitation":"Blackwelder, B.W., 1981, Late Cenozoic marine deposition in the United States Atlantic Coastal Plain related to tectonism and global climate: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 34, p. 87-114, https://doi.org/10.1016/0031-0182(81)90059-6.","productDescription":"28 p.","startPage":"87","endPage":"114","costCenters":[],"links":[{"id":221691,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Florida, Georgia, Maryland, North Carolina, South Carolina, Virginia","otherGeospatial":"United States Atlantic Coastal Plain","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -76.63516713277578,\n              39.650707375103764\n            ],\n            [\n              -78.16936296799359,\n              37.273701106278935\n            ],\n            [\n              -82.45253436033947,\n              30.376169794098267\n            ],\n            [\n              -80.35086636430762,\n              25.113521234758892\n            ],\n            [\n              -78.84964037392687,\n              25.176580493302453\n            ],\n            [\n              -74.22618513239509,\n              36.42652595452515\n            ],\n            [\n              -75.6355614431913,\n              38.51737901406466\n            ],\n            [\n              -76.63516713277578,\n              39.650707375103764\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"34","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a44c6e4b0c8380cd66d83","contributors":{"authors":[{"text":"Blackwelder, B. W.","contributorId":104136,"corporation":false,"usgs":true,"family":"Blackwelder","given":"B.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":361937,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70011834,"text":"70011834 - 1981 - Lower Eocene alluvial paleosols (Willwood Formation, Northwest Wyoming, U.S.A.) and their significance for paleoecology, paleoclimatology, and basin analysis","interactions":[],"lastModifiedDate":"2025-06-16T22:59:15.637184","indexId":"70011834","displayToPublicDate":"2003-04-04T00:00:00","publicationYear":"1981","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":"Lower Eocene alluvial paleosols (Willwood Formation, Northwest Wyoming, U.S.A.) and their significance for paleoecology, paleoclimatology, and basin analysis","docAbstract":"<p>The lower Eocene Willwood Formation of northwest Wyoming is a 700 m thick accumulation of alluvial floodplain and channel mudstones and sandstones, nearly all of which show paleopedogenic modifications. Pedogenesis of Willwood sandstones is indicated by taproot and vertebrate and invertebrate bioturbation, early local cementation by calcium carbonate, and thin illuviation cutans on clastic grains. Pedogenesis in Willwood mudstones is indicated by plant bioturbation, insect and other invertebrate burrow casts and lebensspuren; free iron, aluminum, and manganese mobilization, including hydromorphic gleying; sesquioxide and calcareous glaebule formation in lower parts of the solum; presence of clay-rich and organic carbon-rich zones; and well differentiated epipedons and albic and spodic horizons. Probable A horizons are also locally well developed. </p><p>Occurrence of variegated paleosol units in thick floodplain mudstone deposits and their association with thin, lenticular, and unconnected fluvial sandstones in the Willwood Formation of the central and southeast Bighorn Basin suggest that these soils formed during times of rapid sediment accumulation. The tabular geometry and lateral persistence of soil units as well as the absence of catenization indicate that Willwood floodplains were broad and essentially featureless. </p><p>All Willwood paleosols were developed on alluvial parent materials and are complex in that B horizons of younger paleosols were commonly superimposed upon and mask properties of suspected A and B horizons of the next older paleosols. The soils appear to be wet varieties of the Spodosol and Entisol groups (aquods and ferrods, and aquents, respectively), though thick, superposed and less mottled red, purple, and yellow paleosols resemble some ultisols. Most Willwood paleosols resemble warm temperate to subtropical alluvial soils that form today under alternating wet and dry conditions and (or) fluctuating water tables. The up-section decrease in frequency of gley mottles, increase in numerical proportion and thickness of red versus orange coloration, and increase in abundance of calcrete glaebules indicate better drained soils and probably drier climate in late Willwood time. This drying is believed to be related to creation of rain shadows and spacing of rainfall (but not necessarily decrease in absolute rainfall) due to progressive tectonic structural elevation of the mountainous margins of the Bighorn Basin.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0031-0182(81)90056-0","issn":"00310182","usgsCitation":"Bown, T.M., and Kraus, M.J., 1981, Lower Eocene alluvial paleosols (Willwood Formation, Northwest Wyoming, U.S.A.) and their significance for paleoecology, paleoclimatology, and basin analysis: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 34, p. 1-30, https://doi.org/10.1016/0031-0182(81)90056-0.","productDescription":"30 p.","startPage":"1","endPage":"30","costCenters":[],"links":[{"id":221472,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wyoming","otherGeospatial":"northwest Wyoming","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -109.27505184504837,\n              44.99057640111633\n            ],\n            [\n              -109.27505184504837,\n              43.52185648052293\n            ],\n            [\n              -107.05063593252248,\n              43.52185648052293\n            ],\n            [\n              -107.05063593252248,\n              44.99057640111633\n            ],\n            [\n              -109.27505184504837,\n              44.99057640111633\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"34","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a4a6ae4b0c8380cd68d50","contributors":{"authors":[{"text":"Bown, T. M.","contributorId":106858,"corporation":false,"usgs":true,"family":"Bown","given":"T.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":362069,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kraus, M. J.","contributorId":44605,"corporation":false,"usgs":false,"family":"Kraus","given":"M.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":362068,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":5221655,"text":"5221655 - 1981 - Olfactory pedunculotomy induced anosmia in the wolf (Canis lupus)","interactions":[],"lastModifiedDate":"2025-06-23T16:47:11.026977","indexId":"5221655","displayToPublicDate":"2003-03-25T00:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3077,"text":"Physiology & Behavior","printIssn":"0031-9384","active":true,"publicationSubtype":{"id":10}},"title":"Olfactory pedunculotomy induced anosmia in the wolf (Canis lupus)","docAbstract":"<p><span>A procedure for the surgical induction of anosmia in the wolf is described. Six wolves (4 altered and 2 sham) and one mongrel dog were operated; four wolves and the dog were bilaterally pedunculotomized, and two wolves were sham operated. Behavioral tests with the wolves confirmed that they were anosmic, and anatomical verification in the dog showed that the olfactory peduncle (corresponds to the human olfactory tract) was completely sectioned. Use of this procedure will make possible tests of the role of olfaction in these animals.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0031-9384(81)90346-2","usgsCitation":"Peterson, E., Letellier, M., Parsons, J., Plotka, E., Mech, L., and Seal, U., 1981, Olfactory pedunculotomy induced anosmia in the wolf (Canis lupus): Physiology & Behavior, v. 27, no. 3, p. 543-546, https://doi.org/10.1016/0031-9384(81)90346-2.","productDescription":"4 p.","startPage":"543","endPage":"546","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":197530,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"27","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4af3e4b07f02db691c0c","contributors":{"authors":[{"text":"Peterson, E.K.","contributorId":77261,"corporation":false,"usgs":true,"family":"Peterson","given":"E.K.","email":"","affiliations":[],"preferred":false,"id":334368,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Letellier, M.A.","contributorId":39085,"corporation":false,"usgs":true,"family":"Letellier","given":"M.A.","email":"","affiliations":[],"preferred":false,"id":334365,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Parsons, J.A.","contributorId":91958,"corporation":false,"usgs":true,"family":"Parsons","given":"J.A.","email":"","affiliations":[],"preferred":false,"id":334370,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Plotka, E.D.","contributorId":89248,"corporation":false,"usgs":true,"family":"Plotka","given":"E.D.","email":"","affiliations":[],"preferred":false,"id":334369,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Mech, L.D. 0000-0003-3944-7769","orcid":"https://orcid.org/0000-0003-3944-7769","contributorId":75466,"corporation":false,"usgs":false,"family":"Mech","given":"L.D.","email":"","affiliations":[],"preferred":false,"id":334367,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Seal, U.S.","contributorId":40564,"corporation":false,"usgs":false,"family":"Seal","given":"U.S.","email":"","affiliations":[],"preferred":false,"id":334366,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}}
,{"id":70187610,"text":"mf1280_1981 - 1981 - Seismicity map of the state of Pennsylvania","interactions":[{"subject":{"id":70187610,"text":"mf1280_1981 - 1981 - Seismicity map of the state of Pennsylvania","indexId":"mf1280_1981","publicationYear":"1981","noYear":false,"title":"Seismicity map of the state of Pennsylvania"},"predicate":"SUPERSEDED_BY","object":{"id":60995,"text":"mf1280 - 1987 - Seismicity map of the state of Pennsylvania","indexId":"mf1280","publicationYear":"1987","noYear":false,"title":"Seismicity map of the state of Pennsylvania"},"id":1}],"supersededBy":{"id":60995,"text":"mf1280 - 1987 - Seismicity map of the state of Pennsylvania","indexId":"mf1280","publicationYear":"1987","noYear":false,"title":"Seismicity map of the state of Pennsylvania"},"lastModifiedDate":"2017-05-11T14:41:25","indexId":"mf1280_1981","displayToPublicDate":"1999-11-29T00:00:00","publicationYear":"1981","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":"1280","title":"Seismicity map of the state of Pennsylvania","docAbstract":"<p><span>The earthquake data shown on this map and listed in table 1 are a list of earthquakes that were originally used in preparing the Seismic Risk Studies in the United States in the United States (Algermissen, 1969) which have been recompiled and updated through 1977. These data have been reexamined which resulted in some revisions of epicenters and intensities as well as assignment of intensities to earthquakes that previously had none assigned. Intensity values were updated from new and additional data sources that were not available at the time of original compilation. Some epicenters were relocated on the basis of new information. The data shown in table 1 are estimates of the most accurate epicenter, magnitude, and intensity of each earthquake, on the basis of historical and current information. Some of the aftershocks from large earthquakes are listed but are incomplete in many instances, especially for ones that occurred before seismic instruments were in universal usage.</span></p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf1280_1981","usgsCitation":"Stover, C.W., Reagor, B., and Algermissen, S.T., 1981, Seismicity map of the state of Pennsylvania: U.S. Geological Survey Miscellaneous Field Studies Map 1280, 35.40 x 24.50 inches, https://doi.org/10.3133/mf1280_1981.","productDescription":"35.40 x 24.50 inches","costCenters":[],"links":[{"id":341153,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1280_1981/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":341067,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/1280_1981/mf1280_1981.JPG"}],"country":"United 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W.","contributorId":70369,"corporation":false,"usgs":true,"family":"Stover","given":"C.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":694740,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reagor, B.G.","contributorId":99121,"corporation":false,"usgs":true,"family":"Reagor","given":"B.G.","affiliations":[],"preferred":false,"id":694741,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Algermissen, S. T.","contributorId":39790,"corporation":false,"usgs":true,"family":"Algermissen","given":"S.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":694742,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70188678,"text":"70188678 - 1981 - Tonalites in crustal evolution","interactions":[],"lastModifiedDate":"2025-06-17T16:19:23.460931","indexId":"70188678","displayToPublicDate":"1997-01-01T00:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3047,"text":"Philosophical Transactions of the Royal Society A: Mathematical, Physical and Engineering Sciences","active":true,"publicationSubtype":{"id":10}},"title":"Tonalites in crustal evolution","docAbstract":"<p><span>Tonalites, including trondhjemite as a variety, played three roles through geological time in the generation of Earth’s crust. Before about 2.9 Ga ago they were produced largely by simple partial melting of metabasalt to give the dominant part of Archaean grey gneiss terranes. These terranes are notably bimodal; andesitic rocks are rare. Tonalites played a crucial role in the generation of this protocontinental and oldest crust 3.7- 2.9 Ga ago in that they were the only low-density, high-SiO</span><sub>2</sub><span>&nbsp;rocks produced directly from basaltic crust. In the enormous event giving the greenstone-granite terranes, mostly 2.8-2.6 Ga ago, tonalites formed in lesser but still important proportions by partial melting of metabasalt in the lower regions of down-buckled greenstone belts and by remobilization of older grey gneisses. Tectonism in the Archaean (3.9- 2.5 Ga ago) perhaps was controlled by small-cell convection (McKenzie &amp; Weiss 1975). Little or no ophiolite or eclogite formed, and only minor andesite. Plate tectonics of modern type (involving large, rigid plates) commenced in the early Proterozoic. Uniformitarianism thus goes back one-half of the age of the earth. Tonalites compose about 5-10 % of crust generated in Proterozoic and Phanerozoic time at convergent oceanic-continental margins. They occur here as minor to prominent members of the compositionally continuous continental-margin batholiths. A simple model of generation of these batholiths is offered: mantle-derived mafic magma pools in the lower crust above a subduction zone reacts with and incorporates wall-rock components (Bowen 1922), and breaches its roof rocks as an initial diapir. This mantle magma also develops a gradient of partial melting in its wall rocks. This wall-rock melt accretes in the collapsed chamber and moves up the conduit broached by the initial diapir, the higher, less siliceous fractions of melting first, the lower, more siliceous (and further removed) fractions of melting last. The process gives in the optimum case a mafic-to-siliceous sequence of diorite or quartz diorite through tonalite or quartz monzodiorite to granodiorite and granite. The model implies that great masses of cumulate phases and refractory wall rock form the roots of continentalmargin batholiths, and that migmatites overlie that residuum and underlie the batholiths.</span></p>","language":"English","publisher":"The Royal Society","doi":"10.1098/rsta.1981.0112","usgsCitation":"Barker, F., Arth, J.G., and Hudson, T., 1981, Tonalites in crustal evolution: Philosophical Transactions of the Royal Society A: Mathematical, Physical and Engineering Sciences, v. 301, no. 1461, p. 293-303, https://doi.org/10.1098/rsta.1981.0112.","productDescription":"11 p.","startPage":"293","endPage":"303","costCenters":[],"links":[{"id":342701,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"301","issue":"1461","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"594b85b9e4b062508e382bd4","contributors":{"authors":[{"text":"Barker, F.","contributorId":101368,"corporation":false,"usgs":true,"family":"Barker","given":"F.","affiliations":[],"preferred":false,"id":698875,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Arth, Joseph G.","contributorId":104546,"corporation":false,"usgs":true,"family":"Arth","given":"Joseph","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":698876,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hudson, T.","contributorId":33446,"corporation":false,"usgs":true,"family":"Hudson","given":"T.","affiliations":[],"preferred":false,"id":698877,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":48662,"text":"ofr8167 - 1981 - Floods in the English River basin, Iowa","interactions":[],"lastModifiedDate":"2016-03-02T14:51:02","indexId":"ofr8167","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1981","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":"81-67","title":"Floods in the English River basin, Iowa","docAbstract":"<p>Information describing floods is essential for proper planning, design, and operation of bridges and other structures&nbsp;on or over streams and their flood plains. This report provides information on flood stages and discharges, flood magnitude and frequency, bench mark data, and flood profiles for the English River and some of its tributaries. It covers the English River, the North English River to near&nbsp;Guernsey, the south Eaglish River to Barnes City and the lower reaches of the Biddle English and Deep Rivers</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Iowa City","doi":"10.3133/ofr8167","collaboration":"Prepared in cooperation with the Highway Research Board, the Highway Division and the Iowa Department of Transportation","usgsCitation":"Heinitz, A., and Riddle, D., 1981, Floods in the English River basin, Iowa: U.S. Geological Survey Open-File Report 81-67, v, 61 p., https://doi.org/10.3133/ofr8167.","productDescription":"v, 61 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"links":[{"id":287220,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1981/0067/report.pdf"},{"id":287221,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1981/0067/report-thumb.jpg"}],"country":"United States","state":"Iowa","otherGeospatial":"English River Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -91.773161,41.423635 ], [ -91.773161,41.511706 ], [ -91.637326,41.511706 ], [ -91.637326,41.423635 ], [ -91.773161,41.423635 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dbe4b07f02db5e0ebd","contributors":{"authors":[{"text":"Heinitz, A.J.","contributorId":62610,"corporation":false,"usgs":true,"family":"Heinitz","given":"A.J.","affiliations":[],"preferred":false,"id":237978,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Riddle, D.E.","contributorId":6930,"corporation":false,"usgs":true,"family":"Riddle","given":"D.E.","email":"","affiliations":[],"preferred":false,"id":237977,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":37161,"text":"rp138 - 1981 - Waterfowl and their wintering grounds in Mexico, 1937-64","interactions":[],"lastModifiedDate":"2016-11-02T11:43:18","indexId":"rp138","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"seriesTitle":{"id":79,"text":"Resource Publication","active":false,"publicationSubtype":{"id":1}},"seriesNumber":"138","title":"Waterfowl and their wintering grounds in Mexico, 1937-64","docAbstract":"<p>The U.S. Fish and Wildlife Service has been interested in migratory birds, especially waterfowl, in Mexico for many years, An early period of cooperation in waterfowl administration was culminated in 1937 with the final ratification of the Convention Between the United States and the United Mexican States for the Protection of Migratory Birds and Game Mammals, usually referred to as the Migratory Bird Treat.</p><p>Management of waterfowl on this continent is primarily carried out by hunting regulations. Current information on the status of each species must be obtained each year to serve as a basis for any needed modifications in the regulations. In the United States and Canada, wildlife biologists of the U.S. Fish and Wildlife Service and the Canadian Wildlife Service annually make the surveys to obtain this basic information. But the Government of Mexico has made no comparable surveys. Mexicans are not interested in hunting waterfowl to the extent that citizens of the United States and Canada are. As a consequence, Mexico's Department of Game emphasizes activities other than waterfowl management.</p><p>Waterfowl, especially ducks, winter in or migrate through Mexico in large numbers, so it is obvious that and continental surveys of the winter population should include Mexico. Some general investigations of waterfowl distribution there were made in 1926 and earlier by E. A. Goldman. He was familiar with much of Mexico because he and E. W. Nelson studied mammals and biota there for many years. In the 1930's, because of the greater emphasis on waterfowl conservation and management, more detailed surveys were made of the continental breeding and wintering populations. One of these activities was designated as the midwinter, or January, inventory.</p><p>In the early 1940's the senior author, who had been the Central Flyaway Biologist since 1937, recommended that the waterfowl wintering grounds in Mexico be included in the coverage of the midwinter waterfowl inventory. This was arranged in 1947, and the first aerial coverage, which only included coastal localities, was made in January-February of that year. The information obtained confirmed the value and advisability of including the Mexican wintering grounds in the annual survey; beginning in 1951 the wintering grounds in the Mexican highlands also were included. The surveys of Mexico were continued, except in 1957, through 1965; after 1965 they were greatly reduced.</p><p>Ground reconnaissance and surveys had begun in Mexico with the preliminary work of Goldman in 1926, but quantitative studies were not started until 1937. The ground surveys continued at intervals in various parts of the Republic until 1960. Ground surveys are invaluable for such purposes as securing ecological information, specimens of birds and plants, and historical data about the areas from local residents, but the only satisfactory method of obtaining accurate quantitative information on waterfowl populations and their distribution is by airplane. Consequently, the major emphasis since 1947 has been on the annual aerial surveys. Ground studies were made much less frequently and were carried out mainly to obtain correlative information on the waterfowl foods available, the ecology of habitats, and for liaison with wildlife officials and biologists in Mexico.</p><p>An important reason for the surveys of the waterfowl wintering grounds in Mexico was to determine their adequacy for the population of birds using them, and their potential to accommodate additional waterfowl if the wintering grounds in the United States became inadequate and larger flights entered Mexico. Other advantages included providing accurate information to hunters and other interested persons in the United States regarding the waterfowl shooting in Mexico, and determining the current status of these birds and their habitats in that country. Some of these findings were previously summarized by us (Saunders and Saunders 1949; Saunders 1964).</p>","language":"English","publisher":"U.S. Fish and Wildlife Service","usgsCitation":"Saunders, G.B., and Saunders, D.C., 1981, Waterfowl and their wintering grounds in Mexico, 1937-64: Resource Publication 138, vi, 151 p.","productDescription":"vi, 151 p.","numberOfPages":"160","temporalStart":"1937-01-01","temporalEnd":"1964-12-31","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":330651,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":290220,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/37161/report.pdf"}],"country":"Mexico","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4ba6","contributors":{"authors":[{"text":"Saunders, George B.","contributorId":56285,"corporation":false,"usgs":true,"family":"Saunders","given":"George","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":511193,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Saunders, Dorothy Chapman","contributorId":82980,"corporation":false,"usgs":true,"family":"Saunders","given":"Dorothy","email":"","middleInitial":"Chapman","affiliations":[],"preferred":false,"id":511194,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":58473,"text":"mf1053J - 1981 - Gravity anomaly and interpretation map of the Chignik and Sutwik Island quadrangles, Alaska","interactions":[],"lastModifiedDate":"2014-03-10T12:17:59","indexId":"mf1053J","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1981","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":"1053","chapter":"J","title":"Gravity anomaly and interpretation map of the Chignik and Sutwik Island quadrangles, Alaska","docAbstract":"<p>The gravity field of the Chignik and Sutwik Island\nquadrangles near the center of the Alaska Peninsula represents\na complex series of transitions between probable\ncontinental crust on the north, probable oceanic crust on the\nsouth, sedimentary basins on each side of the peninsula, and a\ncentral structural high and volcanic arc. The resulting\ngravity field may be generalized as a central southwest- to\nnortheast-trending gravity high bordered on both sides by\nflanking gravity lows over sedimentary basins underlying the\nlowlands and continental shelf. All three gravitational\nfeatures show discontinuities and magnitude variations that\nreflect the complex geologic setting.</p>\n<br/>\n<p>Data concerning this complex gravity field have accumulated\nslowly and intermittently since an initial measurement\nwas made at Port Heiden more than 25 years go (Thiel\nand others, 1958, 1959). A few reconnaissance measurements\nby R. V. Allen and an offshore traverse conducted by the U.S.\nCoast and Geodetic Survey R/V Surveyor were made in the\nearly 1960's (Barnes and others, 1966; Barnes, 1967). At\nabout the same time, Gulf Oil Corp. contracted for a\nrelatively detailed survey of the lowlands on the north shore\nof the peninsula; the map prepared from this survey is now\navailable (Gulf Oil Corp., Port Moller Development Contract\nReport, available at U.S. Geological Survey, Anchorage,\nAlaska). In the early 1970's, a few new land measurements\nwere made by P. L. Dobey, of the Alaska Division of\nGeological and Geophysical Surveys, and an offshore traverse\nwas completed by the R/V C. Greene on contract to the U.S.\nGeological Survey (Fisher, 1979, and M. A. Fisher, written\ncommun., 1977). The most recent measurements, the basis\nfor this map, were made by M. E. Yount, D. L. Detra, D. R.\nJefferis, and J. E. Case during the mineral assessment of the\ntwo quadrangles. D. F. Barnes, R. L. Morin, D. R. Jefferis,\nand R. F. Sikora have shared in the data compilation.\nGeologic background for the text was provided by R. L.\nDetterman, T. P. Miller, E. Young, and F. H. Wilson (1979,\n1981).</p>","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/mf1053J","usgsCitation":"Case, J.E., Barnes, D., Detterman, R.L., Morin, R.L., and Sikora, R.F., 1981, Gravity anomaly and interpretation map of the Chignik and Sutwik Island quadrangles, Alaska: U.S. Geological Survey Miscellaneous Field Studies Map 1053, 5 p., https://doi.org/10.3133/mf1053J.","productDescription":"5 p.","costCenters":[],"links":[{"id":105440,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_6424.htm","linkFileType":{"id":5,"text":"html"},"description":"6424"},{"id":183839,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/mf1053j.PNG"},{"id":283651,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/mf/1053-J/report.pdf"}],"country":"United States","state":"Alaska","otherGeospatial":"Chignik Island;Sutwik Island","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -158.4642,56.2719 ], [ -158.4642,56.5864 ], [ -156.9661,56.5864 ], [ -156.9661,56.2719 ], [ -158.4642,56.2719 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b12e4b07f02db6a268c","contributors":{"authors":[{"text":"Case, J. E.","contributorId":56625,"corporation":false,"usgs":true,"family":"Case","given":"J.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":259375,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Barnes, D.F.","contributorId":48960,"corporation":false,"usgs":true,"family":"Barnes","given":"D.F.","email":"","affiliations":[],"preferred":false,"id":259374,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Detterman, R. L.","contributorId":71525,"corporation":false,"usgs":true,"family":"Detterman","given":"R.","middleInitial":"L.","affiliations":[],"preferred":false,"id":259376,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Morin, R. L.","contributorId":95484,"corporation":false,"usgs":true,"family":"Morin","given":"R.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":259377,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Sikora, R. F.","contributorId":21923,"corporation":false,"usgs":true,"family":"Sikora","given":"R.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":259373,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":9851,"text":"ofr81184 - 1981 - Seismic-reflection and sidescan-sonar data collected off eastern Cape Cod, Massachusetts, during April 1979","interactions":[],"lastModifiedDate":"2018-06-18T14:44:54","indexId":"ofr81184","displayToPublicDate":"1994-01-01T01:00:00","publicationYear":"1981","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":"81-184","title":"Seismic-reflection and sidescan-sonar data collected off eastern Cape Cod, Massachusetts, during April 1979","docAbstract":"<p>The U.S. Geological Survey collected 98 line kilometers of single-channel seismic-reflection profiles and sidescan sonar records on the inner shelf of eastern Cape Cod, Massachusetts, during April 1979. The data were obtained during cruise NE-1-79 of the R/V NEECHO. The purposes of the survey were: (1) to study the development of barrier islands; (2) to document the frequency and rate of migration of inlets that breach barrier islands; and (3) to define the characteristics of shoreface ridges on a barrier island.</p><p>he survey uti I ized two acoustic systems. Information about the bottom was obtained by using an EDO Western model 606 sidescan-sonar system (100 kHz). Profiles of the subbottom were collected by an EG&amp;G Uni boom transducer (400-4,000 Hz) and a Del Norte streamer. Positional control for al I track! ines was provided by a shore-based Miniranger system and by LORAN-C.</p><p>The quality of the records generally is very good. However, subbottom penetration did vary somewhat from place to place during the survey due to the nature of the bottom sediments and to the presence or absence of buried channels.</p><p>The original records may be examined at the U.S. Geological Survey, Woods Hole, MA 02543. Microfilm copies of the data are avai I able for purchase from the National Geophysical pnd Solar-Terrestrial Data Center, NOAA/EDIS/NGSDC, Code D621, 325 Broadway, Boulder, CO 80303 (303-497-6338).</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr81184","usgsCitation":"Knebel, H.J., 1981, Seismic-reflection and sidescan-sonar data collected off eastern Cape Cod, Massachusetts, during April 1979: U.S. Geological Survey Open-File Report 81-184, 3 p., https://doi.org/10.3133/ofr81184.","productDescription":"3 p.","numberOfPages":"3","costCenters":[{"id":680,"text":"Woods Hole Science Center","active":false,"usgs":true}],"links":[{"id":141851,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":259859,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1981/0184/ofr1981184.pdf","text":"Report","size":"5.02 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 1998-184"}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -71.0,41.0 ], [ -71.0,42.0 ], [ -69.5,42.0 ], [ -69.5,41.0 ], [ -71.0,41.0 ] ] ] } } ] }","contact":"<p><a href=\"https://woodshole.er.usgs.gov/\" data-mce-href=\"https://woodshole.er.usgs.gov/\">Coastal and Marine Geology Program</a><br> U.S. Geological Survey<br> 384 Woods Hole Road<br> Woods Hole, MA 02543</p>","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a09e4b07f02db5fa965","contributors":{"authors":[{"text":"Knebel, Harley J.","contributorId":25930,"corporation":false,"usgs":true,"family":"Knebel","given":"Harley","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":160406,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":37142,"text":"rp140 - 1981 - Procedures for the use of aircraft in wildlife biotelemetry studies","interactions":[],"lastModifiedDate":"2017-10-20T12:22:12","indexId":"rp140","displayToPublicDate":"1994-01-01T01:00:00","publicationYear":"1981","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"seriesTitle":{"id":79,"text":"Resource Publication","active":false,"publicationSubtype":{"id":1}},"seriesNumber":"140","title":"Procedures for the use of aircraft in wildlife biotelemetry studies","docAbstract":"This is a report on the state of the art methodology and on questions that arise while one is preparing to use aircraft in a biotelemetry study. In general the first step in preparing to mount an antenna on an aircraft is to consult with a certified aircraft mechanic. Aircraft certification is discussed to provide background information concerning the role of the Federal Aviation Administration (FAA) in regulating the use of biotelemetry antennas on aircraft. However, approval of any specific design of antenna mount rests with local FAA authority. Airplane and helicopter antenna attachments are described. Performance of the receiving antenna system is discussed with emphasis on how variables as aircraft type and antenna configuration may influence reception. The side-looking vs. front-looking antenna configuration and the VHF vs. HF frequency band are generally recommended for most aerial tracking studies. Characteristics of receivers, transmitters, and antennas that might influence tracking are discussed. Specific topics such as calibration of receivers and transmitter quality control are considered. Suggestions in preparing for and conducting tracking flights that will improve overall efficiency and safety are presented. Search techniques, including procedures for conducting large and specific area surveys as well as methods to improve and evaluate search efficiency, are discussed. A concluding section considers special topics such as low-level operations and the use of helicopters. Diagrams of antenna mounts, equipment check-off lists, and antenna test procedures are included as appendices.","language":"English","publisher":"U.S. Fish and Wildlife Service","publisherLocation":"Washington, D.C.","usgsCitation":"Gilmer, D.S., Cowardin, L.M., Duval, R.L., Mechlin, L.M., Shaiffer, C.W., and Kuechle, V., 1981, Procedures for the use of aircraft in wildlife biotelemetry studies: Resource Publication 140, 19 p.","productDescription":"19 p.","costCenters":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true},{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"links":[{"id":204228,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ee4b07f02db660904","contributors":{"authors":[{"text":"Gilmer, David S.","contributorId":59508,"corporation":false,"usgs":true,"family":"Gilmer","given":"David","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":217554,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cowardin, Lewis M.","contributorId":34574,"corporation":false,"usgs":true,"family":"Cowardin","given":"Lewis","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":217553,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Duval, Renee L.","contributorId":65595,"corporation":false,"usgs":true,"family":"Duval","given":"Renee","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":217555,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mechlin, Larry M.","contributorId":107842,"corporation":false,"usgs":true,"family":"Mechlin","given":"Larry","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":217557,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Shaiffer, Charles W.","contributorId":16148,"corporation":false,"usgs":true,"family":"Shaiffer","given":"Charles","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":217552,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Kuechle, V.B.","contributorId":83478,"corporation":false,"usgs":true,"family":"Kuechle","given":"V.B.","email":"","affiliations":[],"preferred":false,"id":217556,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}}
,{"id":59455,"text":"mf1348A - 1981 - Geologic map of the Beaver Creek Wilderness, McCreary County, Kentucky","interactions":[],"lastModifiedDate":"2025-09-24T16:51:26.969392","indexId":"mf1348A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1981","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":"1348","chapter":"A","title":"Geologic map of the Beaver Creek Wilderness, McCreary County, Kentucky","docAbstract":"The Beaver Creek Wilderness comprises approximately 4,800 acres and is principally within the cliffline bordering the Beaver Creek drainage basin in McCreary County, southeastern Kentucky. It is part of the Beaver Creek Cooperative Wildlife management Area in the Daniel Boone National Forest, which is managed by the U.S. Forest Service and the Kentucky Department of Fish and Wildlife Resources. The wilderness is about 11 mi southeast of Burnside, Ky., and is accessible from thr north and south via U.S. Route 27 and Forest Service Road 50, at its northwest border (fig. 1). From the east the area can be reached via State Route 90 and Forest Service Road 46, at the eastern end of the wilderness. The interiors is accessible by foot along an abandoned Forest Service road and by several primitive trails that extend along the major streams. The Beaver Creek Wilderness is centrally located at the western edge of the Appalachian coal regions and is within the highly dissected Cumberland Plateau section of the Appalachian Plateaus physiographic province (fig. 2). It is drained by Beaver Creek and tributaries, which flow northeastward into Cumberland Lake, a reservoir on the Cumberland River about 1 mi north of the wilderness. Altitudes range from about 730 ft on the lower part of Beaver Creek to about 1,200 ft at its headwaters.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf1348A","usgsCitation":"Englund, K., and Teaford, N.K., 1981, Geologic map of the Beaver Creek Wilderness, McCreary County, Kentucky: U.S. Geological Survey Miscellaneous Field Studies Map 1348, 1 Plate: 22.98 x 30.08 inches, https://doi.org/10.3133/mf1348A.","productDescription":"1 Plate: 22.98 x 30.08 inches","costCenters":[],"links":[{"id":496034,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_7005.htm","linkFileType":{"id":5,"text":"html"}},{"id":284426,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1348-A/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":180325,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/mf1348a.jpg"}],"scale":"24000","country":"United States","state":"Kentucky","county":"Mccreary County","otherGeospatial":"Beaver Creek Wilderness","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -84.5,\n              36.95\n            ],\n            [\n              -84.5,\n              36.833\n            ],\n            [\n              -84.375,\n              36.833\n            ],\n            [\n              -84.375,\n              36.95\n            ],\n            [\n              -84.5,\n              36.95\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd5c1ae4b0b290850fa4fa","contributors":{"authors":[{"text":"Englund, Kenneth J.","contributorId":105371,"corporation":false,"usgs":true,"family":"Englund","given":"Kenneth J.","affiliations":[],"preferred":false,"id":262040,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Teaford, Nancy K.","contributorId":73919,"corporation":false,"usgs":true,"family":"Teaford","given":"Nancy","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":262039,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
]}