{"pageNumber":"413","pageRowStart":"10300","pageSize":"25","recordCount":10951,"records":[{"id":70220758,"text":"70220758 - 1962 - Aeromagnetic and gravity studies of theprecambrian in northeastern New Mexico","interactions":[],"lastModifiedDate":"2021-05-25T16:34:19.133489","indexId":"70220758","displayToPublicDate":"1962-06-01T11:30:09","publicationYear":"1962","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1808,"text":"Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"Aeromagnetic and gravity studies of theprecambrian in northeastern New Mexico","docAbstract":"<p><span>A contour map of the Precambrian surface for a part of&nbsp;</span><span class=\"ScopusTermHighlight\">northeastern</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">New</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Mexico</span><span>&nbsp;has been prepared from&nbsp;</span><span class=\"ScopusTermHighlight\">aeromagnetic</span><span>,&nbsp;</span><span class=\"ScopusTermHighlight\">gravity</span><span>, and drill-hole data. The area extends approximately from the Colorado border south to latitude34° N., and from the foothills of the Sangre de Cristo Mountains east to longitude 104° W. Thirty-seven depths to Precambrian rocks were computed from&nbsp;</span><span class=\"ScopusTermHighlight\">aeromagnetic</span><span>&nbsp;anomalies. Regional gravityanomalies were generally not suitable for quantitative analysis, but the&nbsp;</span><span class=\"ScopusTermHighlight\">gravity</span><span>&nbsp;highs correlated with known areas ofbasement highs, providing a basis for contouring&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;areas of meager depth control. Drill-hole data provided 61depths to basement&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;and near the survey area. The contouring along the east edge of the Sangre de Cristo Mountainswas guided by exposures of Precambrian rocks. A principal feature of the contour map is the Sierre Grande Arch, a basement highland that trends southwestacross the area to the northwest part of Guadalupe County. Major depressions are outlined west of Vegas Junction, northeast of Santa Rosa, and north and northeast of Las Vegas. The largest of these, the Las Vegas basin, occupiesmore than 1,000 square miles and may be more than 10,000 ft deep Copyright.&nbsp;</span></p>","language":"English","publisher":"Society of Exploration Geophysicists","doi":"10.1190/1.3301595","usgsCitation":"Andreasen, G.E., Kane, M.F., and Zietz, I., 1962, Aeromagnetic and gravity studies of theprecambrian in northeastern New Mexico: Geophysics, v. 27, no. 3, p. 343-358, https://doi.org/10.1190/1.3301595.","productDescription":"16 p.","startPage":"343","endPage":"358","costCenters":[],"links":[{"id":385942,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"New Mexico","otherGeospatial":"northeastern New Mexico","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -106.0400390625,\n              34.66935854524543\n            ],\n            [\n              -102.98583984374999,\n              34.66935854524543\n            ],\n            [\n              -102.98583984374999,\n              36.96744946416934\n            ],\n            [\n              -106.0400390625,\n              36.96744946416934\n            ],\n            [\n              -106.0400390625,\n              34.66935854524543\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"27","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Andreasen, G. E.","contributorId":105315,"corporation":false,"usgs":true,"family":"Andreasen","given":"G.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":816451,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kane, M. F.","contributorId":45708,"corporation":false,"usgs":true,"family":"Kane","given":"M.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":816452,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Zietz, I.","contributorId":59937,"corporation":false,"usgs":true,"family":"Zietz","given":"I.","email":"","affiliations":[],"preferred":false,"id":816453,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70220753,"text":"70220753 - 1962 - Paleozoic seas of central Idaho","interactions":[],"lastModifiedDate":"2021-05-26T12:04:10.351447","indexId":"70220753","displayToPublicDate":"1962-06-01T11:19:39","publicationYear":"1962","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Paleozoic seas of central Idaho","docAbstract":"<p><span>Some recent paleogeographic maps indicate that&nbsp;</span><span class=\"ScopusTermHighlight\">central</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>&nbsp;was part of a major geosyncline throughout&nbsp;</span><span class=\"ScopusTermHighlight\">Paleozoic</span><span>&nbsp;time. This concept, apparently based on thick marine accumulations far apart on the margins of the region, is inconsistent with field data. Within the area of the&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>&nbsp;batholith, Permian(?) volcanic rocks rest either on batholithic rocks or on the Belt Series. The Belt Series rocks have furnished the xenoliths in the batholith. To the west upper&nbsp;</span><span class=\"ScopusTermHighlight\">Paleozoic</span><span>&nbsp;and Mesozoic strata are invaded. Along the eastern margin, south of lat. 45°, thick&nbsp;</span><span class=\"ScopusTermHighlight\">Paleozoic</span><span>&nbsp;strata are intruded by the batholith. These locally exceed 30,000 feet in thickness and thin eastward. They have many variations. Those close to the batholith, especially those high in the sequence, are regarded as of near-shore origin. The&nbsp;</span><span class=\"ScopusTermHighlight\">Paleozoic</span><span>&nbsp;strata in southeastern&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>, more than 17,000 feet thick, are broadly similar except that Cambrian strata there are thicker and more widespread. The part of&nbsp;</span><span class=\"ScopusTermHighlight\">central</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>&nbsp;north of the vicinity of lat. 45° has no known&nbsp;</span><span class=\"ScopusTermHighlight\">Paleozoic</span><span>&nbsp;strata. Northern&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>&nbsp;has only a few outcrops of beds of Cambrian age. The differences in thickness and character between&nbsp;</span><span class=\"ScopusTermHighlight\">Paleozoic</span><span>&nbsp;strata in south-</span><span class=\"ScopusTermHighlight\">central</span><span>&nbsp;and southeastern&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>&nbsp;and those in western Montana and Wyoming (less than 7500 feet thick) suggest a hinge line near the eastern boundary between&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>&nbsp;and Montana with a shelf to the east and a trough to the west. In south-</span><span class=\"ScopusTermHighlight\">central</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>&nbsp;this trough had a maximum width of 90 miles and a western shore roughly at the east margin of the batholith. This trough wedged out northward a little beyond lat. 45°. Thus the area of the present&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>&nbsp;batholith has been a positive block since Precambrian time, comparable to but apparently of longer duration than the geanticline in northern Nevada. Any invasion of the positive block in&nbsp;</span><span class=\"ScopusTermHighlight\">Idaho</span><span>&nbsp;by marine waters during the&nbsp;</span><span class=\"ScopusTermHighlight\">Paleozoic</span><span>&nbsp;was local and brief, except perhaps along the western border. Uncertain correlations within the area of the batholith leave open the possibility of some deposition there early in&nbsp;</span><span class=\"ScopusTermHighlight\">Paleozoic</span><span>&nbsp;time.</span></p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1962)73[769:PSOCI]2.0.CO;2","usgsCitation":"Ross, C.P., 1962, Paleozoic seas of central Idaho: Geological Society of America Bulletin, v. 73, no. 6, p. 769-793, https://doi.org/10.1130/0016-7606(1962)73[769:PSOCI]2.0.CO;2.","productDescription":"25 p.","startPage":"769","endPage":"793","costCenters":[],"links":[{"id":385940,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"Idaho","otherGeospatial":"western-central Idaho","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -117.24609374999999,\n              43.26120612479979\n            ],\n            [\n              -114.5654296875,\n              43.26120612479979\n            ],\n            [\n              -114.5654296875,\n              45.398449976304086\n            ],\n            [\n              -117.24609374999999,\n              45.398449976304086\n            ],\n            [\n              -117.24609374999999,\n              43.26120612479979\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"73","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Ross, Clyde P.","contributorId":10473,"corporation":false,"usgs":true,"family":"Ross","given":"Clyde","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":816449,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70220746,"text":"70220746 - 1962 - Magnetic anomalies and magnetizations of the Biwabik iron-formation, Mesabi area, Minnesota","interactions":[],"lastModifiedDate":"2021-05-25T15:49:46.095599","indexId":"70220746","displayToPublicDate":"1962-06-01T10:44:49","publicationYear":"1962","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1808,"text":"Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"Magnetic anomalies and magnetizations of the Biwabik iron-formation, Mesabi area, Minnesota","docAbstract":"<p><span>In a study of the relationship of&nbsp;</span><span class=\"ScopusTermHighlight\">magnetic</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">anomalies</span><span>&nbsp;to the magnetite content and structure of layered Precambrian iron-formations, the effective induced and remanent&nbsp;</span><span class=\"ScopusTermHighlight\">magnetizations</span><span>&nbsp;of the&nbsp;</span><span class=\"ScopusTermHighlight\">Biwabik</span><span>&nbsp;iron-formation were determined by analyses of aeromagnetic&nbsp;</span><span class=\"ScopusTermHighlight\">anomalies</span><span>&nbsp;recorded 1,000 ft above the&nbsp;</span><span class=\"ScopusTermHighlight\">Biwabik</span><span>&nbsp;in areas of known geology. The induced&nbsp;</span><span class=\"ScopusTermHighlight\">magnetization</span><span>&nbsp;along the layers is relatively insignificant because the formation is almost perpendicular to the earth's&nbsp;</span><span class=\"ScopusTermHighlight\">magnetic</span><span>&nbsp;field. For the relatively unmetamorphosed iron-formation of the Main&nbsp;</span><span class=\"ScopusTermHighlight\">Mesabi</span><span>&nbsp;district, the dominant&nbsp;</span><span class=\"ScopusTermHighlight\">magnetization</span><span>&nbsp;was found to be across the layers, about 0.012 gauss, and most likely induced. For the strongly metamorphosed iron-formation of the East&nbsp;</span><span class=\"ScopusTermHighlight\">Mesabi</span><span>&nbsp;district, the dominant&nbsp;</span><span class=\"ScopusTermHighlight\">magnetization</span><span>&nbsp;was found to be along the layers, about 0.100 gauss, and remanent. These values are used as bases for explaining aeromagnetic&nbsp;</span><span class=\"ScopusTermHighlight\">anomalies</span><span>&nbsp;from correlatives of the&nbsp;</span><span class=\"ScopusTermHighlight\">Biwabik</span><span>&nbsp;iron-formation in the Gunflint, Cuyuna, and Gogebic districts.</span></p>","language":"English","publisher":"Society of Exploration Geophysicists","doi":"10.1190/1.1439073","usgsCitation":"Bath, G.D., 1962, Magnetic anomalies and magnetizations of the Biwabik iron-formation, Mesabi area, Minnesota: Geophysics, v. 27, no. 5, p. 627-650, https://doi.org/10.1190/1.1439073.","productDescription":"24 p.","startPage":"627","endPage":"650","costCenters":[],"links":[{"id":385939,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"Minnesota","otherGeospatial":"north-central Minnesota","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -95.47119140625,\n              47.32393057095941\n            ],\n            [\n              -92.373046875,\n              47.32393057095941\n            ],\n            [\n              -92.373046875,\n              48.96579381461063\n            ],\n            [\n              -95.47119140625,\n              48.96579381461063\n            ],\n            [\n              -95.47119140625,\n              47.32393057095941\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"27","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Bath, G. D.","contributorId":71968,"corporation":false,"usgs":true,"family":"Bath","given":"G.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":816448,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70207936,"text":"70207936 - 1962 - Lava tree molds of the September 1961 eruption, Kilauea Volcano, Hawaii","interactions":[],"lastModifiedDate":"2020-01-20T14:16:14","indexId":"70207936","displayToPublicDate":"1962-01-20T14:04:33","publicationYear":"1962","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Lava tree molds of the September 1961 eruption, Kilauea Volcano, Hawaii","docAbstract":"<p><span>Well-developed lava tree molds were formed during the September 1961 eruption along the east rift zone of Kilauea Volcano. The upright molds were produced where fluid lava, flowing through dense tropical forest, became chilled against the larger trees and tree ferns and later drained away. Where the lava ponded temporarily in a structural valley, tree molds more than 14 feet high mark the high level attained by the flow.</span></p>","language":"English","publisher":"GSA","doi":"10.1130/0016-7606(1962)73[1153:LTMOTS]2.0.CO;2","usgsCitation":"Moore, J.G., and Richter, D., 1962, Lava tree molds of the September 1961 eruption, Kilauea Volcano, Hawaii: GSA Bulletin, v. 73, no. 9, p. 1153-1158, https://doi.org/10.1130/0016-7606(1962)73[1153:LTMOTS]2.0.CO;2.","productDescription":"6 p.","startPage":"1153","endPage":"1158","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":371388,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Hawaii","otherGeospatial":"East rift zone","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -155.2532958984375,\n              19.197053439464852\n            ],\n            [\n              -154.8028564453125,\n              19.197053439464852\n            ],\n            [\n              -154.8028564453125,\n              19.51319789966427\n            ],\n            [\n              -155.2532958984375,\n              19.51319789966427\n            ],\n            [\n              -155.2532958984375,\n              19.197053439464852\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"73","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Moore, James G. 0000-0002-7543-2401 jmoore@usgs.gov","orcid":"https://orcid.org/0000-0002-7543-2401","contributorId":2892,"corporation":false,"usgs":true,"family":"Moore","given":"James","email":"jmoore@usgs.gov","middleInitial":"G.","affiliations":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":779824,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Richter, D.H.","contributorId":43325,"corporation":false,"usgs":true,"family":"Richter","given":"D.H.","email":"","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":779825,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70010465,"text":"70010465 - 1962 - K/Na ratio of Cenozoic igneous rocks of the western United States","interactions":[],"lastModifiedDate":"2020-11-19T17:17:10.952456","indexId":"70010465","displayToPublicDate":"1962-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"K/Na ratio of Cenozoic igneous rocks of the western United States","docAbstract":"<p>The potassium and sodium content of chemically analysed Cenozoic igneous rocks from about 150 areas of the western United States has been examined. For each area a plot of the molecular proportion<span>&nbsp;</span><span class=\"math\"><span id=\"MathJax-Element-1-Frame\" class=\"MathJax_SVG\" data-mathml=\"<math xmlns=&quot;http://www.w3.org/1998/Math/MathML&quot;><mtext>K</mtext><msub><mi></mi><mn>2</mn></msub><mtext>O</mtext><mtext>(K</mtext><msub><mi></mi><mn>2</mn></msub><mtext>O + Na</mtext><msub><mi></mi><mn>2</mn></msub><mtext>O)</mtext></math>\"><span class=\"MJX_Assistive_MathML\">K<sub>2</sub>O(K<sub>2</sub>O + Na<sub>2</sub>O)</span></span></span><span>&nbsp;</span>[Niggli's<span>&nbsp;</span><i>k</i>-value] is shown, and the projected<span>&nbsp;</span><i>k</i>-value determined at 50 and 60 weight per cent SiO<sub>2</sub>. The<span>&nbsp;</span><i>k</i>-values are plotted and contoured on maps of the western United States.</p><p>These maps show that potassium is least abundant relative to total alkali (when rocks of the same SiO<sub>2</sub><span>&nbsp;</span>content are compared) in a zone along the Pacific Coast, becomes more abundant eastward, and is highest in the Colorado Plateau and Northern Rocky Mountains.</p><p>These<span>&nbsp;</span><i>k</i>-value variations can be related to regional variations in the abundance of certain trace elements and of different types of older granitic rocks, and to Bouguer gravity maps. This correspondence indicates that the alkali ratio of Cenozoic igneous rocks is closely related to the character of the crust where the rocks are formed.</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(62)90009-1","usgsCitation":"Moore, J., 1962, K/Na ratio of Cenozoic igneous rocks of the western United States: Geochimica et Cosmochimica Acta, v. 26, no. 1, p. 101-130, https://doi.org/10.1016/0016-7037(62)90009-1.","productDescription":"30 p.","startPage":"101","endPage":"130","numberOfPages":"30","costCenters":[],"links":[{"id":219009,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona, California, Colorado, Idaho, Montana, Nevada, New Mexico, Oregon, Texas, Utah, Washington, Wyoming","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -94.04296874999999,\n              29.84064389983441\n            ],\n            [\n              -94.2626953125,\n              33.61461929233378\n            ],\n            [\n              -99.931640625,\n              34.74161249883172\n            ],\n            [\n              -100.283203125,\n              36.491973470593685\n            ],\n            [\n              -102.919921875,\n              36.59788913307022\n            ],\n            [\n              -102.9638671875,\n              37.09023980307208\n            ],\n            [\n              -102.1728515625,\n              37.09023980307208\n            ],\n            [\n              -102.1728515625,\n              41.0130657870063\n            ],\n            [\n              -104.1064453125,\n              41.1455697310095\n            ],\n            [\n              -104.23828125,\n              48.951366470947725\n            ],\n            [\n              -123.22265625000001,\n              48.980216985374994\n            ],\n            [\n              -122.87109375,\n              48.16608541901253\n            ],\n            [\n              -124.892578125,\n              48.28319289548349\n            ],\n            [\n              -124.27734374999999,\n              45.49094569262732\n            ],\n            [\n              -124.76074218749999,\n              42.391008609205045\n            ],\n            [\n              -124.76074218749999,\n              40.58058466412761\n            ],\n            [\n              -120.10253906249999,\n              34.161818161230386\n            ],\n            [\n              -117.158203125,\n              32.43561304116276\n            ],\n            [\n              -115.13671875,\n              32.731840896865684\n            ],\n            [\n              -114.7412109375,\n              32.509761735919426\n            ],\n            [\n              -111.3134765625,\n              31.353636941500987\n            ],\n            [\n              -108.1494140625,\n              31.42866311735861\n            ],\n            [\n              -108.19335937499999,\n              31.728167146023935\n            ],\n            [\n              -106.6552734375,\n              31.690781806136822\n            ],\n            [\n              -104.32617187499999,\n              29.726222319395504\n            ],\n            [\n              -103.53515625,\n              28.844673680771795\n            ],\n            [\n              -102.4365234375,\n              29.726222319395504\n            ],\n            [\n              -101.3818359375,\n              29.6880527498568\n            ],\n            [\n              -100.1953125,\n              28.265682390146477\n            ],\n            [\n              -99.228515625,\n              26.902476886279832\n            ],\n            [\n              -97.20703125,\n              25.958044673317843\n            ],\n            [\n              -97.42675781249999,\n              27.488781168937997\n            ],\n            [\n              -95.80078125,\n              28.806173508854776\n            ],\n            [\n              -94.04296874999999,\n              29.84064389983441\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"26","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a4044e4b0c8380cd64c1f","contributors":{"authors":[{"text":"Moore, J.G.","contributorId":67496,"corporation":false,"usgs":true,"family":"Moore","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":358985,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70185586,"text":"70185586 - 1962 - Water and the arid zone of the United States","interactions":[],"lastModifiedDate":"2017-03-24T10:27:03","indexId":"70185586","displayToPublicDate":"0002-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Water and the arid zone of the United States","docAbstract":"<p>In a pluvial period associated with Wisconsin glaciation the closed basin of the Estancia Valley in New Mexico held a lake which, at its maximum extent, was 150 feet deep and had a surface area of 450 square miles. This basin, with a mean elevation of about 6,000 feet, has at present an annual precipitation of about 14 inches.</p><p>Estimates have been made of the Pleistocene precipitation necessary to maintain this pluvial lake. Instead of the present annual average of 14 inches it has been variously estimated that the precipitation must have been between 20 and 24 inches. Lakes existed during Pleistocene time in many places in the western United States that are now true deserts - with a precipitation of less than 4 inches - and there is abundant evidence that early man lived on the shores of these lakes. He must have adapted himself to the increasing aridity; this adaptation can be seen even at present in the form of floodwater farming practices, which have been highly developed by the Hopi Indians, particularly in northeastern Arizona.</p><p>A gradually changing climate is only one, and not the most important, of the changing conditions to which man must gradually adjust in his particular relation to the use of water. The changes in his own culture in conjunction with changes in population density are usually even more important determinants of man’s use of and attitude toward his water supplies. In a desert area of Central Arizona, near Florence, the remains of irrigation systems developed by the aborigines to irrigate the alluvial valley floor with water diverted from the Gila River, which was at that time perennial, have been mapped and partially excavated. Irrigated agriculture was not practised nearly so extensively in the arid portions of the United States as in Persia, India, and many Mediterranean countries, nor was the general culture of indigenous American tribes so highly developed. Even in the simple cultures of the American Indians patterns of adjustment to a changing climate and to a changing culture and population level can be discerned. These patterns include, however crudely, the development of irrigated agriculture, floodwater farming, water storage for both stock and community use, spring development, and even efforts at rain-making through the offices of prayers, rattles, and dances. These same patterns, more complex to be sure, can be seen to have characterized the adjustment of modern culture to the limited water supplies of the arid climates, even including the prayers and rattles.</p><p>An aspect of the development of American culture in the arid areas is probably typical and may have a counterpart in certain of the underdeveloped areas in other parts of the world at the present time. The local civilization of the arid climate usually does not develop to a very high level in situ. The indigenous cultures are usually transfused with new bursts of energy and knowledge by the incursion of other cultures which have developed in other climes. The cultural advances in the Fertile Crescent of Mesopotamia were gradually influenced by the barbarian invasion, which added much to, as well as detracted from, the locally developing society. Similarly the spurt of civilization which has characterized the arid parts of the United States since 1846 was determined by the superposition of a culture from the eastern United States on the essentially Spanish culture which had been developing since the initial exploration of the southwestern desert in 1630. </p>","conferenceTitle":"Arid Zone Research - XVIII: The Problems of the Arid Zone, Proceedings of the Paris Symposium","conferenceDate":"May 11-18, 1960","conferenceLocation":"Paris, France","language":"English","publisher":"UNESCO","publisherLocation":"Paris, France","usgsCitation":"Leopold, L.B., 1962, Water and the arid zone of the United States, Arid Zone Research - XVIII: The Problems of the Arid Zone, Proceedings of the Paris Symposium, Paris, France, May 11-18, 1960, p. 395-399.","productDescription":"5 p.","startPage":"395","endPage":"399","costCenters":[],"links":[{"id":338260,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":338258,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://www.unesco.org/ulis/cgi-bin/ulis.pl?catno=148747&set=0058D53A53_2_317&gp=1&lin=1&ll=1"}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"58d6304ce4b05ec799131149","contributors":{"authors":[{"text":"Leopold, Luna Bergere","contributorId":93884,"corporation":false,"usgs":true,"family":"Leopold","given":"Luna","email":"","middleInitial":"Bergere","affiliations":[],"preferred":false,"id":686037,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70157476,"text":"70157476 - 1961 - A preliminary study of the distribution of saline water in the bedrock aquifers of eastern Wisconsin","interactions":[],"lastModifiedDate":"2018-01-08T19:47:43","indexId":"70157476","displayToPublicDate":"2014-12-08T08:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":5596,"text":"Wisconsin Geological & Natural History Survey Information Circular","active":true,"publicationSubtype":{"id":2}},"seriesNumber":"5","title":"A preliminary study of the distribution of saline water in the bedrock aquifers of eastern Wisconsin","docAbstract":"<p>The occurrence of saline water in the bedrock aquifers of eastern Wisconsin has been known for many years. Because of the ready availability of fresh water from other sources, little has been known of the extent of the saline-water area. Saline ground water is a potential source of contamination to wells if it moves into fresh-water zones.</p>","language":"English","publisher":"Wisconsin Geological & Natural History Survey","publisherLocation":"Madison, WI","collaboration":"Prepared by United States Geological Survey in cooperation with the Wisconsin Geological and Natural History Survey","usgsCitation":"Ryling, R.W., 1961, A preliminary study of the distribution of saline water in the bedrock aquifers of eastern Wisconsin: Wisconsin Geological & Natural History Survey Information Circular 5, iv, 23 p.","productDescription":"iv, 23 p.","numberOfPages":"28","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":308493,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":350400,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://wgnhs.uwex.edu/pubs/download_ic05/"}],"country":"United States","state":"Wisconsin","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -86.68212890625,\n              45.38301927899065\n            ],\n            [\n              -88.52783203125,\n              45.390735154248894\n            ],\n            [\n              -89.23095703125,\n              44.15068115978091\n            ],\n            [\n              -89.417724609375,\n              43.644025847699496\n            ],\n            [\n              -89.45068359374999,\n              42.88401467044253\n            ],\n            [\n              -89.373779296875,\n              42.48019996901214\n            ],\n            [\n              -88.11035156249999,\n              42.512601715736665\n            ],\n            [\n              -87.747802734375,\n              42.512601715736665\n            ],\n            [\n              -87.56103515625,\n              42.50450285299051\n            ],\n            [\n              -87.637939453125,\n              43.26920624914964\n            ],\n            [\n              -87.593994140625,\n              43.89789239125797\n            ],\n            [\n              -87.38525390624999,\n              44.465151013519616\n            ],\n            [\n              -87.25341796875,\n              44.77013681219717\n            ],\n            [\n              -86.68212890625,\n              45.38301927899065\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"56051eb0e4b058f706e512a6","contributors":{"authors":[{"text":"Ryling, Roy W.","contributorId":147926,"corporation":false,"usgs":true,"family":"Ryling","given":"Roy","email":"","middleInitial":"W.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":573268,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":71747,"text":"tei791 - 1961 - Geologic summary of the Appalachian basin, with reference to the subsurface disposal of radioactive waste solutions","interactions":[],"lastModifiedDate":"2018-10-03T09:25:01","indexId":"tei791","displayToPublicDate":"2013-07-16T09:38:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":337,"text":"Trace Elements Investigations","code":"TEI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"791","title":"Geologic summary of the Appalachian basin, with reference to the subsurface disposal of radioactive waste solutions","docAbstract":"<p>The Appalachian basin is an elongate depression in the crystalline basement complex which contains a great volume of predominantly sedimentary stratified rocks. As defined in this paper it extends from the Adirondack Mountains in New York to central Alabama. From east to west it extends from the west flank of the Blue Ridge Mountains to the crest of the Findlay and Cincinnati arches and the Nashville dome. It encompasses an area of about 207,000 square miles, including all of West Virginia and parts of New York, New Jersey, Pennsylvania, Ohio, Maryland, Virginia, Kentucky, Tennessee, North Carolina, Georgia, and Alabama.</p><p>The stratified rocks that occupy the basin constitute a wedge-shaped mass whose axis of greatest thickness lies close to and parallel to the east edge of the basin. The maximum thickness of stratified rocks preserved in any one part of the basin today is between 35,000 and 40,000 feet. The volume of the sedimentary rocks is approximately 510,000 cubic miles and of volcanic rocks is a few thousand cubic miles. The sedimentary rocks are predominantly Paleozoic in age, whereas the volcanic rocks are predominantly Late Precambrian.</p><p>On the basis of gross lithology the stratified rocks overlying the crystalline basement complex can be divided into nine vertically sequential units, which are designated \"sequences\" in this report. The boundaries between contiguous sequences do not necessarily coincide with the commonly recognized boundaries between systems or series. All sequences are grossly wedge shaped, being thickest along the eastern margin of the basin and thinnest along the western margin.</p><p>The lowermost unit the Late Precambrian stratified sequence is present only along part of the eastern margin of the basin, where it lies unconformably on the basement complex. It consists largely of volcanic tuffs and flows but contains some interbedded sedimentary rocks. The Late Precambrian sequence is overlain by the Early Cambrian clastic sequence. Where the older sequence is absent, the Early Cambrian sequence rests on the basement complex. Interbedded fine- to coarse-grained noncarbonate detrital rocks comprise the bulk of the sequence, but some volcanic and carbonate rocks are included. Next above is the Cambrian-Ordovician carbonate sequence which consists largely of limestone and dolomite. Some quartzose sandstone is present in the lower part in the western half of the basin, and much shale is present in the upper part in the southeast part of the basin. The next higher sequence is the Late Ordovician clastic sequence, which consists largely of shale, siltstone, and sandstone. Coarse-grained light-gray to red rocks are common in the sequence along the eastern side of the basin, whereas fine-grained dark-gray to black calcareous rocks are common along the west side. The Late Ordovician clastic sequence is overlain unconformably in many places by the&nbsp;Early Silurian clastic sequence. The latter comprises a relatively thin wedge of coarse-grained clastic rocks. Some of the most prolific oil- and gas-producing sandstones in the Appalachian basin are included. Among these are the \"Clinton\" sands of Ohio, the Medina Sandstones of New York and Pennsylvania, and the Keefer or \"Big Six\" Sandstone of West Virginia and Kentucky. Conformably overlying the Early Silurian clastic sequence is the Silurian-Devonian carbonate sequence, which consists predominantly of limestone and dolomite. It also contains a salt-bearing unit in the north-central part of the basin and a thick wedge of coarse-grained red beds in the northeastern part. The sequence is absent in much of the southern part of the basin. Large volumes of gas and much oil are obtained from some of its rocks, especially from the Oriskany Sandstone and the Huntersville Ghert. The Silurian-Devonian carbonate sequence is abruptly overlain by the Devonian clastic sequence a thick succession of interbedded shale, mudrock, siltstone, and sandstone. Colors range from predominantly purple and red in the northeastern part of the basin to predominantly dark gray and black in the southwestern part. Many rocks in the upper part contain hydrocarbons in commercial quantities. The next higher sequence is a heterogeneous succession that comprises most rocks of Mississippian age in the basin. It is composed largely of fine-grained to very coarse-grained noncalcareous clastic rocks in the northern half of the basin, and largely of carbonate rocks in the southern part. Large quantities of oil and gas are produced from the sequence. The youngest sequence consists of coarse-grained clastic rocks largely of Pennsylvanian age. In the center of the basin a relatively small volume of lithologically similar rocks of Permian age are included. The sequence has been intensively mined for coal throughout most of its extent.</p><p>The waste-disposal possibilities of the stratified rocks in the Appalachian basin are considered in terms of the following: 1) gross lithology of the sequences; 2) general lithology of the rock units composing the sequences; and 3) the structural attitudes of the sequences in different parts of the basin. The degree of exploitation of economically significant mineral* resources is considered briefly where such exploitation may affect waste-disposal possibilities. Hydrologic aspects are not in general considered. Based largely on consideration of the above geologic factors the following types of reservoirs associated with particular geologic environments offer some prospects for the disposal of radioactive waste solutions. They are: 1) artificially created cavities in thick salt beds; 2) artificially fractured thin lenticular sandstone bodies isolated in shale or mudrock sequences; 3) portions of thick noncarbonate clastic sequences possessing appreciable natural porosity and permeability; 4) thin clastic units (with natural or artificially created openings) in the plate of a thrust fault overlain by impermeable strata.</p><p>Considered in its entirety the Late Ordovician clastic sequence appears to have a greater number of favorable geologic factors for waste-disposal purposes than the others. The Early Silurian clastic sequence, the Silurian-Devonian carbonate sequence, and the Devonian clastic sequence offer fewer possibilities. The Late Precambrian stratified sequence, Early Cambrian, and the Cambrian-Ordovician carbonate sequence offer few possibilities. The Mississippian and Pennsylvanian sequences appear to be generally unsuitable.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/tei791","collaboration":"Prepared on behalf of the U.S. Atomic Energy Commission","usgsCitation":"Colton, G.W., 1961, Geologic summary of the Appalachian basin, with reference to the subsurface disposal of radioactive waste solutions: U.S. Geological Survey Trace Elements Investigations 791, Report: 121 p.; 15 Maps; 1 Illustration, https://doi.org/10.3133/tei791.","productDescription":"Report: 121 p.; 15 Maps; 1 Illustration","costCenters":[],"links":[{"id":358066,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358065,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0028/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358067,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358068,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358069,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358070,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358071,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358072,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358073,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358074,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358075,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358076,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358077,"rank":14,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358078,"rank":15,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358079,"rank":16,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358080,"rank":17,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358081,"rank":18,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":290249,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0028/report-thumb.jpg"}],"country":"United States","otherGeospatial":"Appalachian Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -84.71,35.8 ], [ -84.71,43.91 ], [ -74.13,43.91 ], [ -74.13,35.8 ], [ -84.71,35.8 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53c79ef3e4b0194841642446","contributors":{"authors":[{"text":"Colton, George Willis","contributorId":12015,"corporation":false,"usgs":true,"family":"Colton","given":"George","email":"","middleInitial":"Willis","affiliations":[],"preferred":false,"id":284696,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":5200271,"text":"5200271 - 1961 - The effects on wildlife of applications of DDT and other insecticides for larval mosquito control in tidal marshes of the eastern United States","interactions":[],"lastModifiedDate":"2012-02-02T00:15:20","indexId":"5200271","displayToPublicDate":"2009-06-08T16:49:39","publicationYear":"1961","noYear":false,"publicationType":{"id":4,"text":"Book"},"title":"The effects on wildlife of applications of DDT and other insecticides for larval mosquito control in tidal marshes of the eastern United States","language":"English","publisher":"Thesis (Ph.D.)--Cornell University","publisherLocation":"Ithaca, NY","collaboration":"Study conducted while author was employed by PWRC.","usgsCitation":"Springer, P.F., 1961, The effects on wildlife of applications of DDT and other insecticides for larval mosquito control in tidal marshes of the eastern United States, xii, 185.","productDescription":"xii, 185","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":201327,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9be4b07f02db65ddc2","contributors":{"authors":[{"text":"Springer, P. F.","contributorId":56590,"corporation":false,"usgs":false,"family":"Springer","given":"P.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":327376,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":47382,"text":"b1082H - 1961 - Manganese deposits in the Drum Mountains, Juab and Millard Counties, Utah","interactions":[{"subject":{"id":47382,"text":"b1082H - 1961 - Manganese deposits in the Drum Mountains, Juab and Millard Counties, Utah","indexId":"b1082H","publicationYear":"1961","noYear":false,"chapter":"H","title":"Manganese deposits in the Drum Mountains, Juab and Millard Counties, Utah"},"predicate":"IS_PART_OF","object":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"id":1}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2017-10-18T15:15:22","indexId":"b1082H","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1082","chapter":"H","title":"Manganese deposits in the Drum Mountains, Juab and Millard Counties, Utah","docAbstract":"<p>The Drum Mountains are in west-central Utah 30 miles northwest of Delta, between the Sevier Desert on the east and Whirlwind Valley on the west. It is a typically barren desert range comprising a westward-tilted structural unit in which is exposed as much as 9,000 feet of quartzite (Cambrian and Precambrian?) and 3,000 feet of carbonate rocks of Cambrian age. These beds, which strike northward and dip west, are cut by myriad east- to northeast-trending faults with displacements of a few feet to a few thousand feet. Quartz monzonite dikes, pebble dikes, and vein deposits are present locally along the faults. The Cambrian rocks are overlain unconformably by volcanic rocks of probable Tertiary age. </p><p>Bodies of manganese carbonate ore were formed by replacement of two 20-foot beds of impure dolomite at the base of the sequence of carbonate rocks, along their intersection with certain preore faults. The feeding fissures locally contain veins in which rhodochrosite is associated with base metal sulfides. Downward- moving meteoric water has oxidized the ore bodies to a depth of 100 to 200 feet except where they are sealed off by structural or stratigraphic traps.<br></p><p>From 1925 to 1953, 72,462 long tons of manganese ore with an average grade of about 25 percent Mn were shipped.</p>","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to economic geology, 1958","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b1082H","usgsCitation":"Crittenden, M.D., Straczek, J.A., and Roberts, R.J., 1961, Manganese deposits in the Drum Mountains, Juab and Millard Counties, Utah: U.S. Geological Survey Bulletin 1082, Report: iv, 51 p.; 5 Plates: 21.87 x 22.85 inches or smaller, https://doi.org/10.3133/b1082H.","productDescription":"Report: iv, 51 p.; 5 Plates: 21.87 x 22.85 inches or smaller","startPage":"493","endPage":"544","costCenters":[],"links":[{"id":100019,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082h/plate-24.pdf","text":"Plate 24","size":"753 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 24"},{"id":100018,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082h/plate-23.pdf","text":"Plate 23","size":"832 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 23"},{"id":172970,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082h/report-thumb.jpg"},{"id":109306,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20749.htm","linkFileType":{"id":5,"text":"html"},"description":"20749"},{"id":100014,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082h/report.pdf","text":"Report","size":"4.26 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":100015,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082h/plate-20.pdf","text":"Plate 20","size":"2.77 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 20"},{"id":100016,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082h/plate-21.pdf","text":"Plate 21","size":"3.8 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 21"},{"id":100017,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082h/plate-22.pdf","text":"Plate 22","size":"1.25 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 22"}],"country":"United States","state":"Utah","county":"Juab County, Millard County","otherGeospatial":"Drum Mountains","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -113.3184814453125,\n              39.45316112807394\n            ],\n            [\n              -112.6812744140625,\n              39.45316112807394\n            ],\n            [\n              -112.6812744140625,\n              39.829631721333726\n            ],\n            [\n              -113.3184814453125,\n              39.829631721333726\n            ],\n            [\n              -113.3184814453125,\n              39.45316112807394\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a82e4b07f02db64aca4","contributors":{"authors":[{"text":"Crittenden, Max D. Jr.","contributorId":28951,"corporation":false,"usgs":true,"family":"Crittenden","given":"Max","suffix":"Jr.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":235192,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Straczek, John A.","contributorId":87194,"corporation":false,"usgs":true,"family":"Straczek","given":"John","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":235191,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Roberts, Ralph Jackson","contributorId":63010,"corporation":false,"usgs":true,"family":"Roberts","given":"Ralph","email":"","middleInitial":"Jackson","affiliations":[],"preferred":false,"id":235193,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":47384,"text":"b1082J - 1961 - Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming","interactions":[{"subject":{"id":12663,"text":"ofr5814 - 1956 - Geologic and structure contour maps of the Carlile quadrangle, Crook County, Wyoming","indexId":"ofr5814","publicationYear":"1956","noYear":false,"title":"Geologic and structure contour maps of the Carlile quadrangle, Crook County, Wyoming"},"predicate":"SUPERSEDED_BY","object":{"id":47384,"text":"b1082J - 1961 - Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming","indexId":"b1082J","publicationYear":"1961","noYear":false,"chapter":"J","title":"Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming"},"id":1},{"subject":{"id":47384,"text":"b1082J - 1961 - Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming","indexId":"b1082J","publicationYear":"1961","noYear":false,"chapter":"J","title":"Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming"},"predicate":"IS_PART_OF","object":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"id":2}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2017-10-18T15:31:20","indexId":"b1082J","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1082","chapter":"J","title":"Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming","docAbstract":"<p>The Carlile quadrangle-is along the northwestern flank of the Black Hills uplift in Crook County, Wyo. The area-is primarily one of canyons and divides that are a result of downcutting by the Belle Fourche River and its tributaries through an alternating succession of sandstone, siltstone, and mudstone or shale beds. The present topography is also influenced by the regional structure, as reflected by the beds that dip gently westward and by the local structural features such as anticlines, domes, synclines, basins, and terraces, which are superimposed upon the regional setting. </p><p>Rocks exposed include shale and thin limestone and sandstone beds belonging to the Redwater shale member of the Sundance formation and to the Morrison formation, both of Late Jurassic age; sandstone, siltstone, and mudstone of the Lakota and Fall River formations of Early Cretaceous age; and shale and sandstone of the Skull Creek shale, Newcastle sandstone, and Mowry shale, also of Early Cretaceous age. In the southwestern part of the quadrangle rocks of the Upper Cretaceous series are exposed. These include the Belle Fourche shale, Greenhorn formation, and Carlile shale. Gravel terraces, landslide debris, and stream alluvium comprise the surficial deposits. The Lakota and Fall River formations, which make up the Iriyan Kara group, contain uranium deposits locally in the northern Black Hills. These formations were informally subdivided in order to show clearly the vertical and lateral distribution of the sandstone, siltstone, and mudstone facies within them.</p><p>The Lakota was subdivided into a sandstone unit and an overlying mudstone unit; the Fall River was subdivided, in ascending order, into a siltstone unit, a mudstone unit, a sandstone unit, and an upper unit. The lithologic character of the Lakota changes abruptly locally, and the units are quite inconsistent with respect to composition, thickness, and extent. This is in contrast to a notable consistency in the lithologic character and thickness among all the Fall River units, with the exception of the upper unit. Petrographic studies on selected samples of units from both formations show differences in composition between Lakota and Fall River rocks.</p><p>The Carlile quadrangle lies immediately east of the monocline that marks the outer limit of the Black Hills uplift, and the rocks in this area have a regional dip of less than 2° outward from the center of the uplift. Superimposed upon the regional uplift are many subordinate structural features anticlines, synclines, domes, basins, and terraces which locally modify the regional features. The most pronounced of these subordinate structural features are the doubly-plunging Pine Ridge, Oil Butte, and Dakota Divide anticlines, and the Eggie Creek syncline. Stress throughout the area was relieved almost entirely through folding; only a few small nearly vertical normal faults were found within the quadrangle.</p><p>Uranium has been mined from the Carlile deposit, owned by the Homestake Mining Co. The ore minerals, carnotite and tyuyamnuite occur in a sandstone lens that is enclosed within relatively impermeable clayey beds in the mudstone unit of the Lakota formation. The ore also includes unidentified black vanadium minerals and possibly coffinite. Uranium minerals are more abundant in and adjacent to thicker carbonaceous and silty seams in the sandstone lens. A mixture of fine-grained calcium carbonate and calcium sulfate fills the interstices between detrital quartz grains in mineralized sandstone. Selenium and arsenic are more abundant in samples that are high in uranium. </p><p>Drilling on Thorn Divide about 1 mile west of the Carlile mine has roughly outlined concentrations of a sooty black uranium mineral associated with pyrite In two stratigraphic intervals of the Lakota formation. One is in the same sandstone lens that contains the ore at the Carlile mine; the other is in conglomeratic sandstone near the base of the Lakota. These deposits are relatively deep, and no mining has been attempted. </p><p>The mineralogy of the Carlile deposits and the lithologic features of the sandstone host rock suggest that uranium and vanadium were transported in the high-valent state by carbonate or sulfate solutions, were extracted from solution by organic material, and were reduced to low-valent states to form an original assemblage of oxides and silicates. These primary minerals were oxidized in place, and the present carnotite-tyuyamunite assemblage was formed. In general, radioactivity analyses correspond fairly closely with chemical analyses of uranium, thus it is believed that only minor solution and migration of uranium has occurred since the present suite of oxidized minerals was formed. </p><p>The factors responsible for ore localization are not clear, but probably a combination of three lithologic and structural elements contributed to provide a favorable environment for precipitating uranium from aqueous solutions: abundant carbonaceous material or pyrite in a thin, permeable sandstone enclosed within relatively thick impermeable clays; local structural basins; and a regional structural setting involving a broad syncline between two anticlines. The structural features controlled the regional flow of ground water and the lithologic features controlled the local rate of flow and provided the proper chemical environment for uranium deposition. </p><p>Bentonite has been mined from an opencut in the Mowry shale in the southwest part of the quadrangle. A bentonite bed in the Newcastle sandstone also seems to be of minable thickness and quality. </p><p>Exploration for petroleum has been unsuccessful within the quadrangle; however, some wells that yielded oil were recently drilled on small anticlines to the west and southeast. It is possible that similar structural features in the Carlile area, that were previously overlooked, may be equally productive.</p>","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to economic geology, 1958","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b1082J","collaboration":"Prepared on behalf of the Atomic Energy Commission and published with permission of the Commission","usgsCitation":"Bergendahl, M., Davis, R.E., and Izett, G., 1961, Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming: U.S. Geological Survey Bulletin 1082, Report: v, 93 p.; 5 Plates: 29.49 x 30.66 inches or smaller, https://doi.org/10.3133/b1082J.","productDescription":"Report: v, 93 p.; 5 Plates: 29.49 x 30.66 inches or smaller","startPage":"613","endPage":"706","costCenters":[],"links":[{"id":100028,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-34.pdf","text":"Plate 34","size":"6.32 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 34"},{"id":100029,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-35.pdf","text":"Plate 35","size":"122 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 35"},{"id":100030,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-36.pdf","text":"Plate 36","size":"3.33 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 36"},{"id":100031,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-37.pdf","text":"Plate 37","size":"1.99 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 37"},{"id":100032,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-38.pdf","text":"Plate 38","size":"783 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 38"},{"id":172971,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082j/report-thumb.jpg"},{"id":100027,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082j/report.pdf","text":"Report","size":"6.87 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Wyoming","county":"Crook County","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -104.89059448242188,\n              44.37295026072434\n            ],\n            [\n              -104.73129272460936,\n              44.37295026072434\n            ],\n            [\n              -104.73129272460936,\n              44.512176171071054\n            ],\n            [\n              -104.89059448242188,\n              44.512176171071054\n            ],\n            [\n              -104.89059448242188,\n              44.37295026072434\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b46b5","contributors":{"authors":[{"text":"Bergendahl, M.H.","contributorId":23538,"corporation":false,"usgs":true,"family":"Bergendahl","given":"M.H.","affiliations":[],"preferred":false,"id":235196,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Davis, R. E.","contributorId":77153,"corporation":false,"usgs":true,"family":"Davis","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":235197,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Izett, G. A.","contributorId":21131,"corporation":false,"usgs":true,"family":"Izett","given":"G. A.","affiliations":[],"preferred":false,"id":235195,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":59057,"text":"mf202 - 1961 - Geologic map of part of the Beaver quadrangle, Utah","interactions":[],"lastModifiedDate":"2018-12-14T11:34:45","indexId":"mf202","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"202","title":"Geologic map of part of the Beaver quadrangle, Utah","docAbstract":"<p>Tertiary volcanic and intrusive rocks underlie a large area surrounding Marysvale in southwestern Utah. Part of the Beaver quadrangle and four complete 15-minute quadrangles, Marysvale, Delano Peak, Sevier, and Monroe, have been mapped to cover the areal extent of these rocks. Mapping in the Beaver quadrangle has been restricted to the northeastern part, the area containing the western part of this volcanic province.</p><p>The mapped area of the quadrangle contains the westernmost slopes of the Tushar Mountains, which slopes steeply to the eastern edge of the Great Basin. The area is thoroughly dissected and its topography is extremely rugged, having a maximum relief of more than 3,500 feet. Wildcat, Indian, and North Creeks have developed the most prominent and steeply walled canyons.</p><p>The area of about 42 square miles lies about 6 miles northeast of Beaver. A main nortb-south thoroughfare, United States Highway 91, connects Beaver with Salt Lake City 208 miles to the north. Roads in the canyons of Indian Creek and North Creek allow entry into the area.</p><p>The geology of the Beaver quadrangle was mapped by Callaghan, but most of the report was written by Parker from field notes, previous reports, and oral data supplied by Callaghan.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf202","usgsCitation":"Callaghan, E., and Parker, R., 1961, Geologic map of part of the Beaver quadrangle, Utah: U.S. Geological Survey Miscellaneous Field Studies Map 202, 28.57 x 18.71 inches, https://doi.org/10.3133/mf202.","productDescription":"28.57 x 18.71 inches","costCenters":[],"links":[{"id":183534,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/0202/report-thumb.jpg"},{"id":360321,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0202/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Utah","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112.63333333333334,38.31666666666667 ], [ -112.63333333333334,38.5 ], [ -112.5,38.5 ], [ -112.5,38.31666666666667 ], [ -112.63333333333334,38.31666666666667 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b12e4b07f02db6a28ea","contributors":{"authors":[{"text":"Callaghan, Eugene","contributorId":79855,"corporation":false,"usgs":true,"family":"Callaghan","given":"Eugene","email":"","affiliations":[],"preferred":false,"id":261341,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Parker, R. L.","contributorId":19170,"corporation":false,"usgs":true,"family":"Parker","given":"R. L.","affiliations":[],"preferred":false,"id":261340,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":47386,"text":"b1082L - 1961 - Tertiary geology and oil-shale resources of the Piceance Creek basin between the Colorado and White Rivers, northwestern Colorado","interactions":[{"subject":{"id":47386,"text":"b1082L - 1961 - Tertiary geology and oil-shale resources of the Piceance Creek basin between the Colorado and White Rivers, northwestern Colorado","indexId":"b1082L","publicationYear":"1961","noYear":false,"chapter":"L","title":"Tertiary geology and oil-shale resources of the Piceance Creek basin between the Colorado and White Rivers, northwestern Colorado"},"predicate":"IS_PART_OF","object":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"id":1}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2017-10-18T15:54:08","indexId":"b1082L","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1082","chapter":"L","title":"Tertiary geology and oil-shale resources of the Piceance Creek basin between the Colorado and White Rivers, northwestern Colorado","docAbstract":"<p>The area of the Piceance Creek basin between the Colorado and White Rivers includes approximately 1,600 square miles and is characterized by an extensive plateau that rises 1,000 to more than 4,000 feet above the surrounding lowlands. Relief is greatest in Naval Oil-Shale Reserves Nos. 1 and 3 near the south margin of the area, where the spectacular Roan Cliffs tower above the valley of the Colorado River. </p><p>The oldest rocks exposed in the mapped area are sandstone, shale, and coal beds of the Mesaverde group of Late Cretaceous age, which crop out along the east margin of the area. Overlying the Mesaverde is an unnamed sequence of dark-colored sandstone and shale, Paleocene in age. The Ohio Creek conglomerate, composed of black and red chert and quartzite pebbles in a white sandstone matrix, is probably the basal unit in the Paleocene sequence. The Wasatch formation of early Eocene age overlies the Paleocene sedimentary rocks. It is composed of brightly colored shale, lenticular beds of sandstone, and a few thin beds of fresh-water limestone. The Kasatch formation interfingers with and is overlain by the Green River formation of middle Eocene age. </p><p>The Green River formation has been divided into the Douglas Creek, Garden Gulch, Anvil Points, Parachute Creek, and Evacuation Creek members. The basal and uppermost members, the Douglas Creek and Evacuation Creek, respectively, are predominantly sandy units. The two middle members, the Garden Gulch and Parachute Creek, are composed principally of finer clastic rocks. The Anvil Points member is present only on the southeast, east, and northeast margins of the area. It is a nearshore facies composed principally of sandstone and is the equivalent of the Douglas Creek, Garden Gulch, and the lower part of the Parachute Creek members. </p><p>All of the richer exposed oil-shale beds are found in the Parachute Creek member, which is divided into two oil-shale zones by a series of low-grade oilshale beds. The upper oil-shale zone has several key beds and zones which can be traced throughout most of the mapped area. One of these, the Mahogany ledge or zone, is a group of very rich oil-shale beds at the base of the upper oil-shale zone. Drilling for oil and gas in the northeastern part of the area has revealed rich oil-shale zones in the Garden Gulch member also.</p><p>Local unconformities within and at the base of the Evacuation Creek member are exposed at several places along Piceance Creek and at one place near the mouth of Yellow Creek; otherwise, the rock sequence is conformable. </p><p>The mapped area is the major part of a large syncline, modified by numerous smaller structural features. Fractures, probably associated genetically with the minor structural features, are present in the central part of the area. These fractures are high-angle normal faults with small displacement. They occur in pairs with the intervening block downdropped. Two sets of joints are prominent, one trending northwest and the other northeast. The joint systems control the drainage pattern in the south-central part of the area. </p><p>More than 20,000 feet of sedimentary rocks underlies the area. Many of the formations yield oil or gas in northwestern Colorado, northeastern Utah, and southwestern Wyoming. The Piceance Creek gas field, in which gas occurs in the Douglas Creek member of the Green River formation, is the largest oil or gas field discovered thus far within the area. </p><p>About 7,000 million barrels of oil is contained in oil shale that yields an average of 45 gallons per ton from a continuous sequence 5 or more feet thick in the Mahogany zone. Oil shale in the Mahogany zone and adjacent beds that yields an average of 30 gallons of oil per ton from a continuous sequence 15 or more feet thick contains about 91,000 million barrels of oil. Similar shale in deeper zones in the northern part of the area, for which detailed estimates have not been prepared, are now known to contain at least an additional 72,000 million barrels of oil. Oil shale in a sequence 15 or more feet thick that yields an average of 25 gallons of oil per ton contains about 154,000 million barrels of oil in the Mahogany zone and adjacent beds; such shale in deeper zones in the northern part of the area probably contains at least an additional 157,000 million barrels of oil, although detailed estimates were not made. Oil shale in a sequence greater than 15 feet thick that yields an average of 15 gallons of oil per ton contains more than 900,000 million barrels of oil. These estimates of the oil content of the deposit do not take into account any loss in mining or processing of the shale.</p>","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to economic geology, 1958","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b1082L","usgsCitation":"Donnell, J., 1961, Tertiary geology and oil-shale resources of the Piceance Creek basin between the Colorado and White Rivers, northwestern Colorado: U.S. Geological Survey Bulletin 1082, Report: v, 56 p.; 7 Plates: 33.54 x 39.62 inches or smaller, https://doi.org/10.3133/b1082L.","productDescription":"Report: v, 56 p.; 7 Plates: 33.54 x 39.62 inches or smaller","startPage":"835","endPage":"891","costCenters":[],"links":[{"id":100042,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082l/report.pdf","text":"Report","size":"5.76 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,{"id":52228,"text":"ofr6228 - 1961 - Geologic summary of the Appalachian Basin, with reference to the subsurface disposal of radioactive waste solutions","interactions":[],"lastModifiedDate":"2018-10-03T09:24:58","indexId":"ofr6228","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"62-28","title":"Geologic summary of the Appalachian Basin, with reference to the subsurface disposal of radioactive waste solutions","docAbstract":"<p>The Appalachian basin is an elongate depression in the crystalline basement complex which contains a great volume of predominantly sedimentary stratified rocks. As defined in this paper it extends from the Adirondack Mountains in New York to central Alabama. From east to west it extends from the west flank of the Blue Ridge Mountains to the crest of the Findlay and Cincinnati arches and the Nashville dome. It encompasses an area of about 207,000 square miles, including all of West Virginia and parts of New York, New Jersey, Pennsylvania, Ohio, Maryland, Virginia, Kentucky, Tennessee, North Carolina, Georgia, and Alabama.</p><p>The stratified rocks that occupy the basin constitute a wedge-shaped mass whose axis of greatest thickness lies close to and parallel to the east edge of the basin. The maximum thickness of stratified rocks preserved in any one part of the basin today is between 35,000 and 40,000 feet. The volume of the sedimentary rocks is approximately 510,000 cubic miles and of volcanic rocks is a few thousand cubic miles. The sedimentary rocks are predominantly Paleozoic in age, whereas the volcanic rocks are predominantly Late Precambrian.</p><p>On the basis of gross lithology the stratified rocks overlying the crystalline basement complex can be divided into nine vertically sequential units, which are designated \"sequences\" in this report. The boundaries between contiguous sequences do not necessarily coincide with the commonly recognized boundaries between systems or series. All sequences are grossly wedge shaped, being thickest along the eastern margin of the basin and thinnest along the western margin.</p><p>The lowermost unit the Late Precambrian stratified sequence is present only along part of the eastern margin of the basin, where it lies unconformably on the basement complex. It consists largely of volcanic tuffs and flows but contains some interbedded sedimentary rocks. The Late Precambrian sequence is overlain by the Early Cambrian clastic sequence. Where the older sequence is absent, the Early Cambrian sequence rests on the basement complex. Interbedded fine- to coarse-grained noncarbonate detrital rocks comprise the bulk of the sequence, but some volcanic and carbonate rocks are included. Next above is the Cambrian-Ordovician carbonate sequence which consists largely of limestone and dolomite. Some quartzose sandstone is present in the lower part in the western half of the basin, and much shale is present in the upper part in the southeast part of the basin. The next higher sequence is the Late Ordovician clastic sequence, which consists largely of shale, siltstone, and sandstone. Coarse-grained light-gray to red rocks are common in the sequence along the eastern side of the basin, whereas fine-grained dark-gray to black calcareous rocks are common along the west side. The Late Ordovician clastic sequence is overlain unconformably in many places by the&nbsp;Early Silurian clastic sequence. The latter comprises a relatively thin wedge of coarse-grained clastic rocks. Some of the most prolific oil- and gas-producing sandstones in the Appalachian basin are included. Among these are the \"Clinton\" sands of Ohio, the Medina Sandstones of New York and Pennsylvania, and the Keefer or \"Big Six\" Sandstone of West Virginia and Kentucky. Conformably overlying the Early Silurian clastic sequence is the Silurian-Devonian carbonate sequence, which consists predominantly of limestone and dolomite. It also contains a salt-bearing unit in the north-central part of the basin and a thick wedge of coarse-grained red beds in the northeastern part. The sequence is absent in much of the southern part of the basin. Large volumes of gas and much oil are obtained from some of its rocks, especially from the Oriskany Sandstone and the Huntersville Ghert. The Silurian-Devonian carbonate sequence is abruptly overlain by the Devonian clastic sequence a thick succession of interbedded shale, mudrock, siltstone, and sandstone. Colors range from predominantly purple and red in the northeastern part of the basin to predominantly dark gray and black in the southwestern part. Many rocks in the upper part contain hydrocarbons in commercial quantities. The next higher sequence is a heterogeneous succession that comprises most rocks of Mississippian age in the basin. It is composed largely of fine-grained to very coarse-grained noncalcareous clastic rocks in the northern half of the basin, and largely of carbonate rocks in the southern part. Large quantities of oil and gas are produced from the sequence. The youngest sequence consists of coarse-grained clastic rocks largely of Pennsylvanian age. In the center of the basin a relatively small volume of lithologically similar rocks of Permian age are included. The sequence has been intensively mined for coal throughout most of its extent.</p><p>The waste-disposal possibilities of the stratified rocks in the Appalachian basin are considered in terms of the following: 1) gross lithology of the sequences; 2) general lithology of the rock units composing the sequences; and 3) the structural attitudes of the sequences in different parts of the basin. The degree of exploitation of economically significant mineral* resources is considered briefly where such exploitation may affect waste-disposal possibilities. Hydrologic aspects are not in general considered. Based largely on consideration of the above geologic factors the following types of reservoirs associated with particular geologic environments offer some prospects for the disposal of radioactive waste solutions. They are: 1) artificially created cavities in thick salt beds; 2) artificially fractured thin lenticular sandstone bodies isolated in shale or mudrock sequences; 3) portions of thick noncarbonate clastic sequences possessing appreciable natural porosity and permeability; 4) thin clastic units (with natural or artificially created openings) in the plate of a thrust fault overlain by impermeable strata.</p><p>Considered in its entirety the Late Ordovician clastic sequence appears to have a greater number of favorable geologic factors for waste-disposal purposes than the others. The Early Silurian clastic sequence, the Silurian-Devonian carbonate sequence, and the Devonian clastic sequence offer fewer possibilities. The Late Precambrian stratified sequence, Early Cambrian, and the Cambrian-Ordovician carbonate sequence offer few possibilities. The Mississippian and Pennsylvanian sequences appear to be generally unsuitable.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ofr6228","collaboration":"Prepared on behalf of the U.S. Atomic Energy Commission","usgsCitation":"Colton, G.W., 1961, Geologic summary of the Appalachian Basin, with reference to the subsurface disposal of radioactive waste solutions: U.S. Geological Survey Open-File Report 62-28, Report: 121 p.; 15 Maps; 1 Illustration, https://doi.org/10.3133/ofr6228.","productDescription":"Report: 121 p.; 15 Maps; 1 Illustration","costCenters":[],"links":[{"id":86729,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86730,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":177170,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0028/report-thumb.jpg"},{"id":86731,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86732,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86733,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86734,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86735,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86736,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86737,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86738,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86739,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86740,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86741,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86742,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86743,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86744,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86745,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0028/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","otherGeospatial":"Appalachian Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -84.71,35.8 ], [ -84.71,43.91 ], [ -74.13,43.91 ], [ -74.13,35.8 ], [ -84.71,35.8 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db688132","contributors":{"authors":[{"text":"Colton, George Willis","contributorId":12015,"corporation":false,"usgs":true,"family":"Colton","given":"George","email":"","middleInitial":"Willis","affiliations":[],"preferred":false,"id":244999,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":67012,"text":"i329 - 1961 - Geology of the Huntsville quadrangle, Alabama","interactions":[],"lastModifiedDate":"2013-12-17T09:24:39","indexId":"i329","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":320,"text":"IMAP","code":"I","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"329","title":"Geology of the Huntsville quadrangle, Alabama","docAbstract":"<p>The 7 1/2-minute Huntsville quadrangle is in south-central Madison County, Ala., and includes part of the city of Hunstville. The south, north, east, and west boundaries of the quadrangle are about 3 miles north of the Tennessee River, 15 1/2 miles south of the Tennessee line, 8 miles west of the Jackson County line, and 9 miles east of the Limestone County line.</p>\n<br/>\n<p>The bedrock geology of the Huntsville quadrangle was mapped by the U.S. Geological Survey in cooperation with the city of Hunstville and the Geological Survey of Alabama as part of a detailed study of the geology and ground-water resources of Madison County, with special reference to the Huntsville area. G. T. Malmberg began the geologic mapping of the county in July 1953, and completed it in April 1954. T. H. Sanford, Jr., assisted Malmberg in the final phases of the county mapping, which included measuring geologic sections with hand level and steel tape. In November 1958 Sanford, assisted by L. R. West, checked contacts and elevations in the Hunstville quadrangle; made revisions in the contact lines; and wrote the text for this report. The fieldwork for this report was completed in April 1959.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/i329","collaboration":"Prepared in cooperation with the City of Hunstville and Geological Survey of Alabama","usgsCitation":"Sanford, T., Malmberg, G., and West, L., 1961, Geology of the Huntsville quadrangle, Alabama: U.S. Geological Survey IMAP 329, Plate: 46.39 x 36.10 inches, https://doi.org/10.3133/i329.","productDescription":"Plate: 46.39 x 36.10 inches","costCenters":[],"links":[{"id":102907,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_1374.htm","linkFileType":{"id":5,"text":"html"},"description":"1374"},{"id":187989,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/imap/0329/report-thumb.jpg"},{"id":279957,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/imap/0329/plate-1.pdf"}],"scale":"24000","country":"United States","state":"Alabama","county":"Madison County","city":"Hunstville","otherGeospatial":"Cumberland Plateau;Highland Rim","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -86.625,34.625 ], [ -86.625,34.75 ], [ -86.5,34.75 ], [ -86.5,34.625 ], [ -86.625,34.625 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acfe4b07f02db67fff0","contributors":{"authors":[{"text":"Sanford, T.H. Jr.","contributorId":80575,"corporation":false,"usgs":true,"family":"Sanford","given":"T.H.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":275451,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Malmberg, G.T.","contributorId":76811,"corporation":false,"usgs":true,"family":"Malmberg","given":"G.T.","email":"","affiliations":[],"preferred":false,"id":275450,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"West, L.R.","contributorId":54499,"corporation":false,"usgs":true,"family":"West","given":"L.R.","email":"","affiliations":[],"preferred":false,"id":275449,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":14707,"text":"ofr6189 - 1961 - Structure and stratigraphy of the Pybus-Gambier area, Alaska","interactions":[{"subject":{"id":14707,"text":"ofr6189 - 1961 - Structure and stratigraphy of the Pybus-Gambier area, Alaska","indexId":"ofr6189","publicationYear":"1961","noYear":false,"title":"Structure and stratigraphy of the Pybus-Gambier area, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":34971,"text":"b1178 - 1964 - Stratigraphy and petrography of the Pybus-Gambier area, Admiralty Island, Alaska","indexId":"b1178","publicationYear":"1964","noYear":false,"title":"Stratigraphy and petrography of the Pybus-Gambier area, Admiralty Island, Alaska"},"id":1}],"supersededBy":{"id":34971,"text":"b1178 - 1964 - Stratigraphy and petrography of the Pybus-Gambier area, Admiralty Island, Alaska","indexId":"b1178","publicationYear":"1964","noYear":false,"title":"Stratigraphy and petrography of the Pybus-Gambier area, Admiralty Island, Alaska"},"lastModifiedDate":"2024-04-10T18:25:46.212153","indexId":"ofr6189","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"61-89","title":"Structure and stratigraphy of the Pybus-Gambier area, Alaska","docAbstract":"<p>The Pybus-Gambier area comprises about 215 square miles of uninhabited land on the southeastern coast of Admiralty Island, southeastern Alaska. The section consists of more than 20,000 feet of intensely folded sedimentary, volcanic, and metamorphic rocks, all probably of marine origin, ranging in age from Silurian(?) to Early Cretaceous, unconformably overlain by more than 10,000 feet of gently dipping nonmarine, coarse-grained sedimentary rocks, and basalt and andesite flows of Eocene age. Diorite plutons and associated contact metamorphic rocks occur in the little-know northwestern part of the area.</p><p>The section here is subdivided into nine formations, eight of which are named for the first time, as follows: Gambier Bay formation of Middle(?) Devonian age, composed of greenschist, phyllite, marble, and metachert; Hood Bay formation or Silurian and Devonian age, composed of dark, carbonaceous, thin-bedded chert, argillite, limestone, and graywacke; Cannery formation of Permian age, composed of thin-bedded chert, argillite, and graywacke; Pybus dolomite of Permian age, composed of fossiliferous, cherty dolomite; Hyd formation of Late Triassic age, composed of a basal chert breccia, a limestone member, a thin-bedded argillite member, and a spilitic volcanic member; Seymour Canal formation of Late Cretaceous and Early Cretaceous age, composed of argillite, graywacke, and conglomerate; Brothers volcanic of Early Cretaceous age, composed of andesitic flows and breccia; unnamed conglomerate and sandstone of Eocene age, and Admiralty Island volcanics of Eocene age, composed of basaltic and andesitic flows.</p><p>A marked angular unconformity occurs at the base of the Tertiary section, and unconformities of less angularity occur as follows: at the base of the Cannery formation; at the base of the Hyd formation, and at the base of the Seymour Canal formation. In general, pre-Seymour Canal deformation seems to have been mild, but the intensity of the post-Gambier Bay - pre-Cannery deformation is uncertain. The complex structure of the pre-Tertiary rocks seem to be the product chiefly of the post-Seymour Canal - pre-Eocene formation.</p><p>The structure of the pre-Tertiary rocks is studied by graphical statistical analysis of the preferred orientation of the planar and linear structural elements. This analysis indicates that the post-Seymour Canal - pre-Eocene deformation consisted chiefly of three episodes of folding, all of which appear to have resulted from sub-horizontal, northeast-southwest compression. The first episode produced isoclinal folds in bedding, and in places associated axial plane foliation, that had north-northwesterly striking axial planes in eastern Pybus-Gambier area, but generally northeasterly striking axial planes west of False Point Pybus. Compression during the second episode deformed the first folds in the west where their axial planes were oriented about parallel to the compression into complex second folds in both bedding and axial plane foliation, having northwesterly striking axial planes. The second folds are absent in the east where the axial planes and limbs of the first folds were oriented about normal to the second compression. The divergence of the axial planes of the first folds in the west from those in the east may have been caused by the crowding of the first folds in the west against the irregular western margin of the geosyncline during the first compression. Northweststriking thrust and reverse faults occur between domains in which the axial planes of the first folds are strongly divergent. The third episode produced kink folds, having axial planes with subvertical dips but widely varying strikes, that are confined to the thinly fissile schists and phyllites of the Gambier Bay formation.</p><p>The episodes of folding in the Gambier Bay formation are accompanied by metamorphic recrystallization not found in either younger or possibly coeval (Hood Bay formation) pre-Tertiary rocks. If these episodes are contemporaneous with those in nonmetamorphic pre-Tertiary rocks, then the metamorphism dies out both vertically and laterally, and may be part of the regional decrease in metamorphism westward away from the Coast Range batholith, located about 25 miles to the east.</p><p>The gently dipping Tertiary strata have been broken into fault blocks by subvertical, north-and north-east striking, normal and reverse faults.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6189","usgsCitation":"Loney, R.A., 1961, Structure and stratigraphy of the Pybus-Gambier area, Alaska: U.S. Geological Survey Open-File Report 61-89, Report: xi, 200 p.; 4 Plates: 54.77 x 27.69 inches or smaller, https://doi.org/10.3133/ofr6189.","productDescription":"Report: xi, 200 p.; 4 Plates: 54.77 x 27.69 inches or smaller","costCenters":[],"links":[{"id":427678,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1961/0089/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":427677,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1961/0089/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":427676,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1961/0089/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":427675,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1961/0089/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":427674,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1961/0089/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":147628,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1961/0089/report-thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Pybus-Gambier area","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -135.4161999804407,\n              57.800343437171534\n            ],\n            [\n              -135.4161999804407,\n              56.87392354672548\n            ],\n            [\n              -133.41015612007976,\n              56.87392354672548\n            ],\n            [\n              -133.41015612007976,\n              57.800343437171534\n            ],\n            [\n              -135.4161999804407,\n              57.800343437171534\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b13e4b07f02db6a371f","contributors":{"authors":[{"text":"Loney, Robert Ahlberg","contributorId":72802,"corporation":false,"usgs":true,"family":"Loney","given":"Robert","email":"","middleInitial":"Ahlberg","affiliations":[],"preferred":false,"id":169881,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":1304,"text":"wsp1475D - 1961 - Geology and occurrence of ground water at Jewel Cave National Monument, South Dakota","interactions":[],"lastModifiedDate":"2016-04-05T09:49:55","indexId":"wsp1475D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1475","chapter":"D","title":"Geology and occurrence of ground water at Jewel Cave National Monument, South Dakota","docAbstract":"<p>Jewel Cave National Monument occupies 2 square miles of a broad plateau of sedimentary rocks in western Custer County, S. Dak., and is at an altitude of about 5,400 feet above mean sea level. The sedimentary rocks that constitute the plateau range in age from Cambrian to Pennsylvanian. Rocks of Silurian and Devonian age are absent. The presence of rocks of Ordovician age has not been established definitely but they may be represented by 10 feet of sandstone directly beneath the Englewood limestone of Mississippian age. The sedimentary formations are underlain by schist of Precambrian age.</p>\n<p>Study of outcrops in the vicinity of the monument confirms the existence of a fault about 1,500 feet north of the entrance to Jewel Cave. The fault trends generally east-west across the monument and has a displacement of about 120 feet about 1 mile west of the entrance to the cave. The effect of the fault on the occurrence of ground water near the cave is not known. In addition to the spring that furnishes the present (1959) water supply for the facilities at Jewel Cave, three springs outside the monument were visited during the study. Combined yield of the 3 springs is less than 2 gpm (gallons per minute).</p>\n<p>A single test well indicates that the monument at the well site is underlain by 665 feet of limestone, dolomite, and sandstone of Paleozoic age and an undetermined thickness of quartzbiotite schist of Precambrian age. Pumping tests using a cylinder pump indicate that the test well is capable of producing 15 to 18 gpm for a short time from 2 zones of sandstone below the Englewood limestone. These sandstones are believed to present the best possibilities for development of a permanent water supply at the monument.</p>","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Hydrology of the Public Domain","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1475D","collaboration":"Prepared in cooperation with the National Park Service","usgsCitation":"Dyer, C., 1961, Geology and occurrence of ground water at Jewel Cave National Monument, South Dakota: U.S. Geological Survey Water Supply Paper 1475, 23 p., https://doi.org/10.3133/wsp1475D.","productDescription":"23 p.","startPage":"139","endPage":"157","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":137886,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1475d/report-thumb.jpg"},{"id":26336,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1475d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"South Dakota","otherGeospatial":"Jewel Cave National Monument","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -103.85478973388672,\n              43.71057158566884\n            ],\n            [\n              -103.85478973388672,\n              43.74381677850666\n            ],\n            [\n              -103.81153106689452,\n              43.74381677850666\n            ],\n            [\n              -103.81153106689452,\n              43.71057158566884\n            ],\n            [\n              -103.85478973388672,\n              43.71057158566884\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db64986f","contributors":{"authors":[{"text":"Dyer, C.F.","contributorId":23917,"corporation":false,"usgs":true,"family":"Dyer","given":"C.F.","email":"","affiliations":[],"preferred":false,"id":143533,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":3275,"text":"cir443 - 1961 - Availability of ground water in the Gallup area, New Mexico","interactions":[],"lastModifiedDate":"2013-07-29T14:45:31","indexId":"cir443","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"443","title":"Availability of ground water in the Gallup area, New Mexico","docAbstract":"A thick succession of sedimentary rocks (about 6,000 feet) underlies the town of Gallup and crops out nearby. Although all the sedimentary rocks are capable of yielding some water, only a few units of sandstone and limestone yield water in sufficient quantity and of acceptable quality to be considered as sources of large supplies. The five stratigraphic units that are most productive of ground water form three aquifers, as follows: (a) the Glorieta sandstone and San Andres limestone, (b) the Westwater Canyon member of the Morrison formation and the Dakota sandstone, and (e) the Gallup sandstone. The Glorieta sandstone yields only small amounts of water to wells, except where it is intensely fractured. It probably contributes large amounts of water to the overlying, more permeable San Andres limestone by slow vertical leakage over large areas, as water is withdrawn from the San Andres. The San Andres limestone is discontinuous in the eastern part of the area, wedging out entirely a few miles east of Gallup. Its permeability varies widely because locally the permeability has been greatly increased by fractures and solution channels. On the north flank of the Zuni Mountains, near its outcrop, the San Andres yields as much as 1,100 gpm (gallons per minute) of water to wells. The specific capacity of wells that tap the aquifer formed by this Glorieta sandstone and San Andres limestone ranges from 0.1 to 29 gpm per foot of drawdown. \n\nIn general, the water in the Glorieta sandstone and San Andres limestone is hard, because it contains much calcium. Both bicarbonate and sulfate anions are abundant. The chemical quality of the water deteriorates with increasing distance from the outcrop. \n\nThe Westwater Canyon member of the Morrison formation and the Dakota sandstone form a single hydrologic unit extending from about 5 miles east of Gallup westward into Arizona. To the east they are separated by shale of the Brushy Basin member of the Morrison formation. The water-bearing properties of the Westwater Canyon member and the Dakota sandstone are ill defined, because few wells in the area tap either of them exclusively. The specific capacity of wells that tap the Westwater Canyon member, the Dakota sandstone, or both ranges from 0.02 to 2.3 gpm per foot of drawdown. \n\nWater in this aquifer generally contains less that 1,000 ppm (parts per million) of dissolved solids. The concentration of sodium and bicarbonate typically is high, and the concentration of sulfate is high locally. The Gallup sandstone is the principal aquifer in the immediate vicinity of, and to the north and south of, Gallup. It yields as much as 260 gpm of water to wells; the specific capacity of wells that tap the Gallup sandstone ranges from 0.08 to 4.7 gpm per foot of drawdown. In general, the water in the Gal]up sandstone is potable, although in places it yields water high in iron, sulfate, and dissolved solids; the concentration of dissolved solids generally is less than 1,000 ppm. \n\nBecause the yields of all the formations tested at Gallup are small, the town needs a better source of water. The San Juan River discharges annually a larger volume of water than is available from any other source in northwestern New Mexico. Gallup has applied for 15,000 acre-feet of San Juan River water a year, an average of 13,400,000 gpd (gallons per day). This water would be expensive, because about 50 miles of pipeline would be required to transport the water, and it would have to be liked about 1,000 feet over a high ridge north of town. \n\nDespite the expense involved, at this time the San Juan River seems to offer the most secure long-term supply of water for the Gallup area.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/cir443","collaboration":"Prepared in cooperation with the New Mexico State Engineer and the town of Gallup","usgsCitation":"West, S.W., 1961, Availability of ground water in the Gallup area, New Mexico: U.S. Geological Survey Circular 443, Report: iv, 21 p.; 1 Plate: 16.40 x 18.09 inches, https://doi.org/10.3133/cir443.","productDescription":"Report: iv, 21 p.; 1 Plate: 16.40 x 18.09 inches","numberOfPages":"26","costCenters":[],"links":[{"id":124367,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/0443/report-thumb.jpg"},{"id":30272,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/0443/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271084,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/0443/plate-1.pdf"}],"country":"United States","state":"New Mexico","city":"Gallup","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -108.847,35.493 ], [ -108.847,35.55 ], [ -108.59,35.55 ], [ -108.59,35.493 ], [ -108.847,35.493 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d8c6","contributors":{"authors":[{"text":"West, Samuel Wilson","contributorId":24763,"corporation":false,"usgs":true,"family":"West","given":"Samuel","email":"","middleInitial":"Wilson","affiliations":[],"preferred":false,"id":146559,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":14568,"text":"ofr6274 - 1961 - Gravity survey in the eastern Snake River Plain, Idaho — A progress report","interactions":[],"lastModifiedDate":"2022-01-24T22:09:51.144703","indexId":"ofr6274","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"62-74","title":"Gravity survey in the eastern Snake River Plain, Idaho — A progress report","docAbstract":"<p>A regional gravity survey in the eastern Snake River Plain was conducted in the early summer of 1961. Seven hundred and seven gravity stations were established between latitudes 42°15'N and 44°30'N between longitudes 111°30'W and 114°30'W. Three hundred and twenty-five of these stations were located in 2,700 square miles of the eastern part with an average density of one station per 8.3 square miles. The remaining 9,300 square miles were covered by several lines, with an average lineal density of one station per 2.0 miles. A simple-Bouguer gravity contour map has been made of the area by standard methods. The low gravity relief and broad high of the eastern Snake River Plain strongly contrasts with the high amplitude anomalies of the western plain. The major anomalies of the eastern plain consist of 1) a broad high, which is an extension of the large gravity highs of the western plain, 2) a set of elongated alternating lows and highs that trend normal to the axis of the eastern plain, 3) a series of small, local highs on the boundary of the plain, and 4) a prominent low centered over Mud Lake in the northern part of the surveyed area. The basalts of the eastern plain have probably filled troughs or valleys in an undulating subsurface floor rather than a large regional graben.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6274","usgsCitation":"LaFehr, T.R., 1961, Gravity survey in the eastern Snake River Plain, Idaho — A progress report: U.S. Geological Survey Open-File Report 62-74, Report: 58 p.; 1 Plate: 49.35 × 45.58 inches, https://doi.org/10.3133/ofr6274.","productDescription":"Report: 58 p.; 1 Plate: 49.35 × 45.58 inches","costCenters":[],"links":[{"id":394788,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8032.htm"},{"id":43238,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0074/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43237,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0074/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":146546,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0074/report-thumb.jpg"}],"country":"United States","state":"Idaho","otherGeospatial":"eastern Snake River Plain","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -114.750,\n              42.25\n            ],\n            [\n              -111.5,\n              42.25\n            ],\n            [\n              -111.5,\n              45\n            ],\n            [\n              -114.750,\n              45\n            ],\n            [\n              -114.750,\n              42.25\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b11e4b07f02db6a23f4","contributors":{"authors":[{"text":"LaFehr, Thomas R.","contributorId":65858,"corporation":false,"usgs":true,"family":"LaFehr","given":"Thomas","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":169664,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70220609,"text":"70220609 - 1961 - Geophysical study of subsurface structure in southern Owens Valley, California","interactions":[],"lastModifiedDate":"2021-05-20T23:39:11.496193","indexId":"70220609","displayToPublicDate":"1961-12-31T18:34:15","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1808,"text":"Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"Geophysical study of subsurface structure in southern Owens Valley, California","docAbstract":"<p><span>Gravity and seismic measurements&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">southern</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Owens</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Valley</span><span>,&nbsp;</span><span class=\"ScopusTermHighlight\">California</span><span>, have outlined a deep&nbsp;</span><span class=\"ScopusTermHighlight\">subsurface</span><span>&nbsp;trough, bounded throughout the greater part of its length by steep faults. Depths to the bedrock floor along the central part of the&nbsp;</span><span class=\"ScopusTermHighlight\">valley</span><span>&nbsp;range from 3,000 to 9,000 ft below the surface. The&nbsp;</span><span class=\"ScopusTermHighlight\">subsurface</span><span>&nbsp;trough is divided into two parts, a narrow channel-like depression near Lone Pine bounded by northwest-trending faults, and a broad basin at&nbsp;</span><span class=\"ScopusTermHighlight\">Owens</span><span>&nbsp;Lake bounded by a more complex series of border faults. The bedrock ridge that crops out to form Alabama Hills is shown to extend from Independence to the north edge of&nbsp;</span><span class=\"ScopusTermHighlight\">Owens</span><span>&nbsp;Lake, nearly twice its visible extent. The main direction of faults that have formed the&nbsp;</span><span class=\"ScopusTermHighlight\">valley</span><span>&nbsp;is northwest; subsidiary faults trend north, northeast, and east. A fairly sharp velocity boundary within the Cenozoic&nbsp;</span><span class=\"ScopusTermHighlight\">valley</span><span>&nbsp;deposits suggests a change&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;the rate and character of deposition which was probably the result of renewed uplift&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;the nearby mountains.</span></p>","language":"English","publisher":"Society of Exploration Geophysicists","doi":"10.1190/1.1438835","usgsCitation":"Kane, M.F., and Pakisek, L., 1961, Geophysical study of subsurface structure in southern Owens Valley, California: Geophysics, v. 26, no. 1, p. 12-26, https://doi.org/10.1190/1.1438835.","productDescription":"15 p.","startPage":"12","endPage":"26","costCenters":[],"links":[{"id":385825,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"California","otherGeospatial":"Owens Valley","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -120.33325195312499,\n              37.74465712069939\n            ],\n            [\n              -119.46533203125,\n              37.74465712069939\n            ],\n            [\n              -119.46533203125,\n              39.45316112807394\n            ],\n            [\n              -120.33325195312499,\n              39.45316112807394\n            ],\n            [\n              -120.33325195312499,\n              37.74465712069939\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"26","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Kane, M. F.","contributorId":45708,"corporation":false,"usgs":true,"family":"Kane","given":"M.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":816143,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pakisek, L.C.","contributorId":258180,"corporation":false,"usgs":false,"family":"Pakisek","given":"L.C.","email":"","affiliations":[],"preferred":false,"id":816144,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70220645,"text":"70220645 - 1961 - Reconnaissance study of quaternary faults in and south of Yellowstone National Park, Wyoming","interactions":[],"lastModifiedDate":"2021-05-21T19:21:30.166576","indexId":"70220645","displayToPublicDate":"1961-12-31T14:17:30","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Reconnaissance study of quaternary faults in and south of Yellowstone National Park, Wyoming","docAbstract":"<p><span>Normal&nbsp;</span><span class=\"ScopusTermHighlight\">faults</span><span>&nbsp;offset a bedrock surface scoured by Pleistocene ice&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;several areas within and&nbsp;</span><span class=\"ScopusTermHighlight\">south</span><span>&nbsp;of&nbsp;</span><span class=\"ScopusTermHighlight\">Yellowstone</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">National</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Park</span><span>. Recurrent earthquake shocks and fresh appearance of some scarps suggest that movement is continuing along some&nbsp;</span><span class=\"ScopusTermHighlight\">faults</span><span>. Four systems of&nbsp;</span><span class=\"ScopusTermHighlight\">faults</span><span>&nbsp;are described.&nbsp;</span><span class=\"ScopusTermHighlight\">Quaternary</span><span>&nbsp;movement occurred along more than 60&nbsp;</span><span class=\"ScopusTermHighlight\">faults</span><span>&nbsp;on the Mirror Plateau, 15 miles northeast of&nbsp;</span><span class=\"ScopusTermHighlight\">Yellowstone</span><span>&nbsp;Lake.&nbsp;</span><span class=\"ScopusTermHighlight\">Faults</span><span>&nbsp;trend northwest, and several are more than 6 miles long. Maximum displacement exceeds 250 feet. The majority have northeast blocks downdropped, but some grabens and horsts are present. Eocene to Pliocene igneous or pyroclastic rocks are displaced. Ice moved southwest and&nbsp;</span><span class=\"ScopusTermHighlight\">south</span><span>&nbsp;from the Beartooth and Absaroka ranges, nearly at right angles to the&nbsp;</span><span class=\"ScopusTermHighlight\">fault</span><span>&nbsp;trends. Drainage&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;many ice-scoured valleys was disrupted by faulting, and small lakes (such as Mirror Lake) formed on downthrown blocks. Thermal activity occurs along some of these&nbsp;</span><span class=\"ScopusTermHighlight\">faults</span><span>. Directly east of Mirror Plateau, the Lamar normal&nbsp;</span><span class=\"ScopusTermHighlight\">fault</span><span>&nbsp;has a displacement of 1300 + feet; perhaps 1000 feet of this may have occurred during&nbsp;</span><span class=\"ScopusTermHighlight\">Quaternary</span><span>&nbsp;time. The&nbsp;</span><span class=\"ScopusTermHighlight\">Yellowstone</span><span>&nbsp;Falls&nbsp;</span><span class=\"ScopusTermHighlight\">fault</span><span>&nbsp;system cuts Pliocene rhyolite southeast of the Upper Falls of the&nbsp;</span><span class=\"ScopusTermHighlight\">Yellowstone</span><span>&nbsp;River.&nbsp;</span><span class=\"ScopusTermHighlight\">Faults</span><span>&nbsp;trend northwest; maximum displacement exceeds 200 feet. The Solfatara&nbsp;</span><span class=\"ScopusTermHighlight\">fault</span><span>&nbsp;system trends north-northwest, cuts Pliocene rhyolite, and has a maximum&nbsp;</span><span class=\"ScopusTermHighlight\">Quaternary</span><span>&nbsp;displacement of about 200 feet. The Hering Lake&nbsp;</span><span class=\"ScopusTermHighlight\">fault</span><span>&nbsp;system is a northern extension of the Teton&nbsp;</span><span class=\"ScopusTermHighlight\">fault</span><span>, trends northward, and cuts Pliocene rhyolite and rhyolitic welded tuff. Maximum displacement is about 200 feet. West-flowing streams established on bedrock scoured by ice were disrupted, and Beula, Hering, and&nbsp;</span><span class=\"ScopusTermHighlight\">South</span><span>&nbsp;Boundary lakes formed on the downthrown (east) blocks. The sharp angular unstepped appearance of&nbsp;</span><span class=\"ScopusTermHighlight\">fault</span><span>&nbsp;scarps 50 to 200 feet high&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;these&nbsp;</span><span class=\"ScopusTermHighlight\">fault</span><span>&nbsp;systems suggests that each scarp of this type was formed by one continuous movement. The displacement along&nbsp;</span><span class=\"ScopusTermHighlight\">faults</span><span>&nbsp;associated with the Hebgen earthquake of August 1959 is commonly less than 20 feet. The abundance of&nbsp;</span><span class=\"ScopusTermHighlight\">Quaternary</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">faults</span><span>&nbsp;and the record of 18 earthquakes&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;historic time suggest that additional faulting and earthquake activity can be expected&nbsp;</span><span class=\"ScopusTermHighlight\">in</span><span>&nbsp;the future. Recognition of this probability should influence the location and type of construction of buildings and other facilities.&nbsp;</span></p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1749:RSOQFI]2.0.CO;2","usgsCitation":"Love, D., 1961, Reconnaissance study of quaternary faults in and south of Yellowstone National Park, Wyoming: Geological Society of America Bulletin, v. 72, no. 12, p. 1749-1764, https://doi.org/10.1130/0016-7606(1961)72[1749:RSOQFI]2.0.CO;2.","productDescription":"16 p.","startPage":"1749","endPage":"1764","costCenters":[],"links":[{"id":480377,"rank":0,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://figshare.com/articles/figure/Reconnaissance_study_of_Quaternary_faults_in_and_south_of_Yellowstone_National_Park_Wyoming/13687621","text":"External Repository"},{"id":385865,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"Wyoming","otherGeospatial":"Yellowstone National Park","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -111.03881835937499,\n              43.6599240747891\n            ],\n            [\n              -108.797607421875,\n              43.6599240747891\n            ],\n            [\n              -108.797607421875,\n              45.01141864227728\n            ],\n            [\n              -111.03881835937499,\n              45.01141864227728\n            ],\n            [\n              -111.03881835937499,\n              43.6599240747891\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"72","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Love, D.","contributorId":15809,"corporation":false,"usgs":true,"family":"Love","given":"D.","email":"","affiliations":[],"preferred":false,"id":816284,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70220644,"text":"70220644 - 1961 - Paleoecology of an early oligocene biota from Douglass Creek Basin, Montana","interactions":[],"lastModifiedDate":"2021-05-21T19:16:21.510182","indexId":"70220644","displayToPublicDate":"1961-12-31T14:08:45","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Paleoecology of an early oligocene biota from Douglass Creek Basin, Montana","docAbstract":"<p><span class=\"ScopusTermHighlight\">Douglass</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Creek</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>&nbsp;lies west of the Continental Divide in the northern part of the Rocky Mountain physiographic province. Numerous minor environmental differences exist between the&nbsp;</span><span class=\"ScopusTermHighlight\">Douglass</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Creek</span><span>&nbsp;area and the Pipestone Springs and Canyon Ferry areas east of the Divide. In the 19th century, however, the three areas had identical mammalian species representation, although not equally dense populations. Fossils of an&nbsp;</span><span class=\"ScopusTermHighlight\">early</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Oligocene</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">biota</span><span>&nbsp;have been collected from the&nbsp;</span><span class=\"ScopusTermHighlight\">Douglass</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Creek</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>. Presence of all but one of the&nbsp;</span><span class=\"ScopusTermHighlight\">Douglass</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Creek</span><span>&nbsp;mammalian species in the Pipestone Springs-Canyon Ferry&nbsp;</span><span class=\"ScopusTermHighlight\">early</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Oligocene</span><span>&nbsp;fauna suggests that the three ancient ecosystems resembled each other in much the same way as the 19th century systems. The&nbsp;</span><span class=\"ScopusTermHighlight\">early</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Oligocene</span><span>&nbsp;deposits and&nbsp;</span><span class=\"ScopusTermHighlight\">biota</span><span>&nbsp;of the&nbsp;</span><span class=\"ScopusTermHighlight\">Douglass</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Creek</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>&nbsp;indicate a moist, temperate climate with seasonal variations. Sediment size and distribution suggest that the cross-valley relief was no greater than it is now. The fish and invertebrate faunas show that a shallow, hard-water lake existed in the area. The flora included a lowland, lake-border association and an upland coniferous forest. Although the ancient&nbsp;</span><span class=\"ScopusTermHighlight\">Douglass</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Creek</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">biota</span><span>&nbsp;doubtless included many species not represented in the fossil collections, most of the mammalian species are probably represented in the combined&nbsp;</span><span class=\"ScopusTermHighlight\">Douglass</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Creek</span><span>, Pipestone Springs, and Canyon Ferry fossil assemblages. If so, the number of mammalian species was about the same as in the 19th century ecosystem.</span></p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1633:POAEOB]2.0.CO;2","usgsCitation":"Konizeski, R.L., 1961, Paleoecology of an early oligocene biota from Douglass Creek Basin, Montana: Geological Society of America Bulletin, v. 72, no. 11, p. 1633-1642, https://doi.org/10.1130/0016-7606(1961)72[1633:POAEOB]2.0.CO;2.","productDescription":"10 p.","startPage":"1633","endPage":"1642","costCenters":[],"links":[{"id":385864,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"Montana","otherGeospatial":"Douglas Creek","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -113.06510925292969,\n              46.584350070440536\n            ],\n            [\n              -112.91130065917969,\n              46.584350070440536\n            ],\n            [\n              -112.91130065917969,\n              46.62963563393178\n            ],\n            [\n              -113.06510925292969,\n              46.62963563393178\n            ],\n            [\n              -113.06510925292969,\n              46.584350070440536\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"72","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Konizeski, Richard L.","contributorId":80248,"corporation":false,"usgs":true,"family":"Konizeski","given":"Richard","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":816283,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70220634,"text":"70220634 - 1961 - An aeromagnetic profile from anchorage to Nome, Alaska","interactions":[],"lastModifiedDate":"2021-05-21T17:35:10.663879","indexId":"70220634","displayToPublicDate":"1961-12-31T12:31:47","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1808,"text":"Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"An aeromagnetic profile from anchorage to Nome, Alaska","docAbstract":"<p><span>A total-intensity&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>&nbsp;was obtained on a 500-mile flight by a U. S. Geological Survey airplane from&nbsp;</span><span class=\"ScopusTermHighlight\">Anchorage</span><span>&nbsp;to&nbsp;</span><span class=\"ScopusTermHighlight\">Nome</span><span>,&nbsp;</span><span class=\"ScopusTermHighlight\">Alaska</span><span>, on May 4, 1954. The average flight altitude was 6,000 ft above sea level except over the&nbsp;</span><span class=\"ScopusTermHighlight\">Alaska</span><span>&nbsp;Range where the flight altitude was 9,000 ft. This&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>&nbsp;crossed eight of the major tectonic elements of&nbsp;</span><span class=\"ScopusTermHighlight\">Alaska</span><span>&nbsp;at right angles to their trend and gives valuable regional information in an area where other geophysical and geological information is scarce or lacking. The&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>&nbsp;has a net gradient downward to the northwest, most of which is ascribed to the component of the earth's main magnetic field along the flight traverse. The great variety of magnetic anomalies which are superimposed on this gradient originate from variations in lithology along the traverse. All the magnetic anomalies, except a large one over the Yukon River, are caused by magnetic rocks at or near the surface. The magnetic&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>&nbsp;may be divided into four major segments and nine subsegments, each having a characteristic magnetic pattern. Most of these can be related to a tectonic unit. The large plutons of the Talkeetna geanticline are clearly defined by a group of anomalies having the highest amplitudes of any on the&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>. The Matanuska geosyncline to the east is represented by a 25-mile section of sloping&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>&nbsp;consistent with a thick sedimentary section but indicating that the geosyncline is comparatively narrow near&nbsp;</span><span class=\"ScopusTermHighlight\">Anchorage</span><span>. The 200-mile central magnetic segment is relatively free from all but very minor anomalies. This segment includes the&nbsp;</span><span class=\"ScopusTermHighlight\">Alaska</span><span>&nbsp;Range geosyncline, the Tanana geanticline, and the Kuskokwim geosyncline; showing only slight magnetic contrasts between each of these elements. The two geosynclines either have thick Mesozoic sedimentary sections or have underlying crystalline rocks which are low in magnetic susceptibility at shallow depths. The rocks of the geanticline have a low but not negligible magnetic susceptibility and are predominantly Paleozoic sedimentary rocks. A single 300-gamma anomaly on the west edge of the central segment is caused by a small, mafic intrusive body in the Paleozoic metamorphic rocks of Mt. Hurst. West of this anomaly the&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>&nbsp;consists of a series of small sharp anomalies which are probably caused by Paleozoic metavolcanic rocks of the Ruby geanticline. The second largest anomaly on the&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>&nbsp;is in the Koyukuk geosyncline over the Yukon River. The source is calculated to be more than a mile deep and may be an intrusive body at least 15 miles wide. This anomaly is flanked by 20-mile sections of flat or sloping&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>&nbsp;which indicate areas of thick sedimentary rocks, particularly in the region west of the Yukon River. The 150-mile Norton Sound magnetic segment on the western end of the&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>&nbsp;consists of many closely spaced anomalies produced by rocks which are either volcanic or similar to the Seward complex. Of the four Cenozoic basins or lowlands crossed by the&nbsp;</span><span class=\"ScopusTermHighlight\">profile</span><span>, three are underlain by rocks of moderate to high magnetic susceptibility at shallow depths. These are the Cook Inlet basin, part of which overlaps rocks of the Talkeetna geanticline, the Innoko basin of central&nbsp;</span><span class=\"ScopusTermHighlight\">Alaska</span><span>&nbsp;which overlies the rocks of the Ruby geanticline, and the Norton basin, in which sedimentary deposits are thin or absent. The fourth, the Minchumina basin, is underlain by the low-susceptibility rocks at the Tanana geanticline, which are also probably close to the surface.&nbsp;</span></p>","language":"English","publisher":"Society of Exploration Geophysicists","doi":"10.1190/1.1438945","usgsCitation":"King, E.R., 1961, An aeromagnetic profile from anchorage to Nome, Alaska: Geophysics, v. 26, no. 6, p. 716-726, https://doi.org/10.1190/1.1438945.","productDescription":"11 p.","startPage":"716","endPage":"726","costCenters":[],"links":[{"id":385854,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"Alaska","city":"Nome","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -166.46484375,\n              63.97596090918338\n            ],\n            [\n              -163.740234375,\n              63.97596090918338\n            ],\n            [\n              -163.740234375,\n              65.10914820386473\n            ],\n            [\n              -166.46484375,\n              65.10914820386473\n            ],\n            [\n              -166.46484375,\n              63.97596090918338\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"26","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"King, E. R.","contributorId":93482,"corporation":false,"usgs":true,"family":"King","given":"E.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":816264,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70220631,"text":"70220631 - 1961 - Origin and development of the Three Forks Basin, Montana","interactions":[],"lastModifiedDate":"2021-05-21T17:04:12.208306","indexId":"70220631","displayToPublicDate":"1961-12-31T11:50:04","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5935,"text":"Bulletin of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Origin and development of the Three Forks Basin, Montana","docAbstract":"<p><span>The&nbsp;</span><span class=\"ScopusTermHighlight\">Three</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Forks</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Basin</span><span>&nbsp;sprawls where the intricately deformed sedimentary and volcanic rocks of the Disturbed Belt along the Rocky Mountain front are faulted against the Precambrian metamorphic rocks that make the core of the Tobacco Root, Madison, Gallatin, and Beartooth ranges. Its eastern edge is linear, controlled by steep faults at the west front of the Bridger Range. All other boundaries are sinuous and show little sign of structural control. Tertiary deposits in the&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>, rich in contemporaneous rhyolitic and latitic ash, are about equally of lake, bolson, and stream&nbsp;</span><span class=\"ScopusTermHighlight\">origin</span><span>. The western part of the&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>&nbsp;is dominated by moderately folded Eocene and lower Oligocene rocks, more than 2000 feet thick. They dip eastward beneath apparently unfolded upper Miocene and Pliocene rocks, more than 1300 feet thick, that also dip gently eastward to the&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>&nbsp;edge. Thin but extensive Quaternary deposits lying unconformably on the Tertiary and pre-Tertiary rocks are mainly of rounded terrace and flood-plain gravel, angular fan gravel, and wind-blown silt. The&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>&nbsp;began as part of an east-flowing stream system that developed in Late Cretaceous and Paleocene time, concurrently with Laramide folding and thrusting; the faulted contact between metamorphic and sedimentary rocks was especially erodible and became a main drainage way. Recurrent uplift to the west throughout the Tertiary provided gradient and load to the streams; additional load was provided by showers of ash from unknown vents. Relative uplifts of the Bridger Range in Eocene and early Oligocene time, and again in late Miocene and Pliocene time, impeded flow from the&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>&nbsp;and led to deposits in channels, flood plains, and lakes. During most of Oligocene and Miocene time, however, the&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>&nbsp;was being eroded. By the end of the Tertiary the&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>&nbsp;was deeply filled and became part of a regional surface of low relief. Regional northwestward tilting stimulated headward erosion of the Missouri River which then captured the formerly east-draining or closed&nbsp;</span><span class=\"ScopusTermHighlight\">basin</span><span>. The Tertiary deposits have been deeply eroded, and the rugged pre-</span><span class=\"ScopusTermHighlight\">basin</span><span>&nbsp;surface partly exhumed.</span></p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1003:OADOTT]2.0.CO;2","usgsCitation":"Robinson, G.D., 1961, Origin and development of the Three Forks Basin, Montana: Bulletin of the Geological Society of America, v. 72, no. 7, p. 1303-1313, https://doi.org/10.1130/0016-7606(1961)72[1003:OADOTT]2.0.CO;2.","productDescription":"11 p.","startPage":"1303","endPage":"1313","costCenters":[],"links":[{"id":385851,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"Montana","city":"Three Forks","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -111.7913818359375,\n              45.80391388619765\n            ],\n            [\n              -111.37115478515625,\n              45.80391388619765\n            ],\n            [\n              -111.37115478515625,\n              46.02938880791639\n            ],\n            [\n              -111.7913818359375,\n              46.02938880791639\n            ],\n            [\n              -111.7913818359375,\n              45.80391388619765\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"72","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Robinson, G. D.","contributorId":96669,"corporation":false,"usgs":true,"family":"Robinson","given":"G.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":816261,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70220602,"text":"70220602 - 1961 - Sandstone-type uranium deposits at Ambrosia Lake, New Mexico-An interim report","interactions":[],"lastModifiedDate":"2021-05-21T14:30:00.203583","indexId":"70220602","displayToPublicDate":"1961-11-01T16:44:43","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Sandstone-type uranium deposits at Ambrosia Lake, New Mexico-An interim report","docAbstract":"<p><span>The&nbsp;</span><span class=\"ScopusTermHighlight\">Ambrosia</span><span>&nbsp;</span><span class=\"ScopusTermHighlight\">Lake</span><span>&nbsp;district in northwestern&nbsp;</span><span class=\"ScopusTermHighlight\">New</span><span>&nbsp;Mexico is the most important&nbsp;</span><span class=\"ScopusTermHighlight\">uranium</span><span>&nbsp;mining and milling district in the United States. Together with the nearby Laguna district it contains more than 50 percent of the nation's reserves.Most of the ore occurs in the Morrison formation of Late Jurassic age as elongate, tabular, mantolike bodies principally in the upper half of the Westwater Canyon sandstone member and near the base of the Poison Canyon sandstone tongue (9). Individual&nbsp;</span><span class=\"ScopusTermHighlight\">deposits</span><span> are distributed along two easterly trending belts 2 to 3 miles apart. The ore bodies are as much as 3,000 feet long, several hundred feet wide, and 100 feet thick. Depths to the ore range from 0 to 2,200 feet. Some ore is also mined from the Todilto limestone of Late Jurassic age and from the Dakota sandstone of Early (?) and Late Cretaceous age.Two types of unoxidized ore are recognized: prefault ore, which is considered to be primary, and postfault ore, which may be redistributed. The prefault ore shows no obvious relationship to tectonic structures but appears to be controlled by a variety of sedimentary structures. Postfault ore is controlled by a combination of sedimentary and tectonic structures. Disseminated carbonaceous matter, believed to be plant derived, appears to be the dominant control in the localization of the&nbsp;</span><span class=\"ScopusTermHighlight\">uranium</span><span>.The ore mineralogy is comparatively simple, and coffinite is by far the most abundant ore mineral. Molybdenum, selenium, vanadium, and iron occur in anomalous quantities in the&nbsp;</span><span class=\"ScopusTermHighlight\">deposits</span><span>&nbsp;in both oxidized and unoxidized minerals.U/eU ratios and radioisotope distribution indicate almost universal disequilibrium and fairly recent migration of radioisotopes in all&nbsp;</span><span class=\"ScopusTermHighlight\">deposits</span><span>&nbsp;that have been sampled.Further studies on the organic carbonaceous matter, sandstone alteration, age determinations, and sulfur isotope composition are required to obtain a better understanding of the source, transportation, and deposition of&nbsp;</span><span class=\"ScopusTermHighlight\">uranium</span><span>&nbsp;and other elements in the&nbsp;</span><span class=\"ScopusTermHighlight\">deposits</span><span>.</span></p>","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.56.7.1179","usgsCitation":"Granger, H., Santos, E., Dean, B., and Moore, F.B., 1961, Sandstone-type uranium deposits at Ambrosia Lake, New Mexico-An interim report: Economic Geology, v. 56, no. 7, p. 1179-1210, https://doi.org/10.2113/gsecongeo.56.7.1179.","productDescription":"32 p.","startPage":"1179","endPage":"1210","costCenters":[],"links":[{"id":385818,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"New Mexico","otherGeospatial":"Ambrosia Lake","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -107.962646484375,\n              35.11990857099681\n            ],\n            [\n              -107.5286865234375,\n              35.11990857099681\n            ],\n            [\n              -107.5286865234375,\n              35.61711648382185\n            ],\n            [\n              -107.962646484375,\n              35.61711648382185\n            ],\n            [\n              -107.962646484375,\n              35.11990857099681\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"56","issue":"7","noUsgsAuthors":false,"publicationDate":"1961-11-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Granger, H.C.","contributorId":15203,"corporation":false,"usgs":true,"family":"Granger","given":"H.C.","email":"","affiliations":[],"preferred":false,"id":816126,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Santos, E.S.","contributorId":95883,"corporation":false,"usgs":true,"family":"Santos","given":"E.S.","email":"","affiliations":[],"preferred":false,"id":816127,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dean, B.G.","contributorId":18845,"corporation":false,"usgs":true,"family":"Dean","given":"B.G.","email":"","affiliations":[],"preferred":false,"id":816128,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Moore, F. B.","contributorId":12461,"corporation":false,"usgs":true,"family":"Moore","given":"F.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":816129,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
]}