The manganese deposits in the United States (exclusive of Alaska and Hawaii) are shown on the accompanying map. The deposits have been divided into several genetic types distinguished on the map by symbols. The principal distinction is between syngenetic deposits, in which the manganese was deposited contemporaneously with the enclosing rocks, and epigenetic, in which manganese was introduced into sedimentary rocks after their deposition or into igneous rocks after solidification. Because hydrothermal, metamorphic, and particularly supergene processes modify and in places concentrate manganese minerals after deposition of the element, classification of many deposits is subject to uncertainties. A third category, deposits of unknown or uncertain origin, is therefore included also. Subdivisions of these principal categories are based on the geologic history subsequent to original accumulation of the syngenetic deposits, and on gross mineralogic nature of the epigenetic ones.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mr23","usgsCitation":"Crittenden, M., and Pavlides, L., 1962, Manganese in the United States, exclusive of Alaska and Hawaii: U.S. Geological Survey Mineral Investigations Resource Map 23, Report: 8 p.; 1 Plate: 64.13 x 40.59 inches, https://doi.org/10.3133/mr23.","productDescription":"Report: 8 p.; 1 Plate: 64.13 x 40.59 inches","costCenters":[],"links":[{"id":179867,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mr/23/report-thumb.jpg"},{"id":260419,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mr/23/plate-1.pdf"},{"id":486401,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/mr/23/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"3168000","country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -127.25,24.25 ], [ -127.25,49.25 ], [ -66.5,49.25 ], [ -66.5,24.25 ], [ -127.25,24.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a82e4b07f02db64ae18","contributors":{"authors":[{"text":"Crittenden, Max D.","contributorId":43404,"corporation":false,"usgs":true,"family":"Crittenden","given":"Max D.","affiliations":[],"preferred":false,"id":266620,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pavlides, Louis","contributorId":79444,"corporation":false,"usgs":true,"family":"Pavlides","given":"Louis","email":"","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":266621,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2535,"text":"wsp1607 - 1962 - Reconnaissance of ground-water resources in the Eastern Coal Field Region, Kentucky","interactions":[],"lastModifiedDate":"2012-02-02T00:05:29","indexId":"wsp1607","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"1607","title":"Reconnaissance of ground-water resources in the Eastern Coal Field Region, Kentucky","docAbstract":"In the Eastern Coal Field region of Kentucky, water is obtained from consolidated sedimentary rocks ranging in age from Devonian to Pennsylvanian and from unconsolidated sediments of Quaternary age. About 95 percent of the area is underlain by shale, sandstone, and coal of Pennsylvanian age. Principal factors governing the availability of water in the region are depth, topographic location, and the lithology of the aquifer penetrated. In general, the yield of the well increases as the depth increases. Wells drilled in topographic lows, such as valleys, are likely to yield more water than wells drilled on topographic highs, such as hills. Sand and gravel, present in thick beds in the alluvium along the Ohio River, form the most productive aquifer in the Eastern Coal Field. Of the consolidated rocks in the region sandstone strata are the best aquifers chiefly because joints, openings along bedding planes, and intergranular pore spaces are best developed in them. Shale also supplies water to many wells in the region, chiefly from joints and openings along bedding planes. Coal constitutes a very small part of the sedimentary section, but it yields water from fractures to many wells. Limestone yields water readily from solution cavities developed along joint and bedding-plane openings. \r\n\r\nThe availability of water in different parts of the region was determined chiefly by analyzing well data collected during the reconnaissance. The resulting water-availability maps, published as hydrologic investigations atlases (Price and others, 1961 a, b; Kilburn and others, 1961) were designed to be used in conjunction with this report. The maps were constructed by dividing the region into 5 physiographic areas, into 10 subareas based chiefly on lithologic facies, and, in the case of the Kanawha section, into 2 quality-of-water areas. The 5 physiographic areas are the Knobs, Mississippian Plateau, Cumberland Plateau section, Kanawha section, and Cumberland Mountain section. \r\n\r\nThe 10 subareas are as follows: \r\n\r\n1. The Chattanooga shale. This black shale yields only enough water for a minimum domestic supply-100 to 500 gpd (gallons per day). \r\n\r\n2. Mississippian-Devonian rocks exposed along Pine Mountain. These rocks consist of shale, limestone, and sandstone. The limestone yields water to springs, and faulted limestone and sandstone lying below drainage may yield several hundred gallons per minute to wells. \r\n\r\n3. Mississippian rocks exposed along the western margin of the region. These rocks consist of thick limestone underlain by shale. The limestone yields enough water for a modern domestic supply (more than 500 gpd) , and discharges as much as 100 gpm (gallons per minute) to springs. The shale yields only enough water for a minimum domestic supply. \r\n\r\n4. Subarea 1 of the Lee formation of Pennsylvanian age. The thin shaly rocks of this subarea generally yield only enough water for a minimum domestic supply. \r\n\r\n5. Subarea 2 of the Lee formation of Pennsylvanian age. This subarea is predominantly underlain by massive sandstones; it generally yields enough water for a modern domestic supply, and in some places, enough water for small public and industrial supplies. \r\n\r\n6. Subarea 1 of the Breathitt and Conemaugh formations of Pennsylvanian age. Rocks in this subarea contain more shale than sandstone. Wells in this subarea range from adequate for a minimum domestic supply to adequate for a modern domestic supply. \r\n\r\n7. Subarea 2 of the Breathitt formation of Pennsylvanian age and undifferentiated post-Lee Pennsylvanian rocks. Wells in this subarea yield enough water for a modern domestic supply, and in many places, enough water for small public and industrial supplies. \r\n\r\n8. Alluvium along the Ohio River. Mostly composed of glacial outwash sand and gravel, the alluvium is reported to yield as much as 360 gpm to wells. \r\n\r\n9. Alluvium along the Big Sandy River and lower reaches of its Tug and Levisa Forks. Where consisting mostly of sand, ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1607","usgsCitation":"Price, W.E., Mull, D.S., and Kilburn, C., 1962, Reconnaissance of ground-water resources in the Eastern Coal Field Region, Kentucky: U.S. Geological Survey Water Supply Paper 1607, iv, 56 p. :ill., maps ;24 cm. + plates folded in pocket., https://doi.org/10.3133/wsp1607.","productDescription":"iv, 56 p. :ill., maps ;24 cm. + plates folded in pocket.","costCenters":[],"links":[{"id":138579,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1607/report-thumb.jpg"},{"id":28766,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28767,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28768,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28769,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28770,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28771,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28772,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28773,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28774,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28775,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1607/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28776,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1607/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a69e4b07f02db63c1ba","contributors":{"authors":[{"text":"Price, William E.","contributorId":84740,"corporation":false,"usgs":true,"family":"Price","given":"William","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":145361,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mull, D. S.","contributorId":43331,"corporation":false,"usgs":true,"family":"Mull","given":"D.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":145359,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kilburn, Chabot","contributorId":83499,"corporation":false,"usgs":true,"family":"Kilburn","given":"Chabot","email":"","affiliations":[],"preferred":false,"id":145360,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2879,"text":"wsp1609 - 1962 - Ground-water resources of Camas Prairie, Camas and Elmore Counties, Idaho","interactions":[],"lastModifiedDate":"2012-02-02T00:05:35","indexId":"wsp1609","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"1609","title":"Ground-water resources of Camas Prairie, Camas and Elmore Counties, Idaho","docAbstract":"Camas Prairie is an eastward-trending intermontane basin along the north flank of the Snake River Plain in southern Idaho. The basin is about 40 miles long and averages about 8 miles wide. It was formed as a structural depression in which a considerable thickness of alluvial and lake deposits accumulated behind basalt flows, which at times blocked the outlet to the east. Intrusive and extrusive rocks of Cretaceous to Quarternary age enclose the basin on the north, west, and east. The enclosing rocks yield small amounts of water to springs and wells from the weathered mantle and fractures. \r\n\r\nThe principal aquifers are sand and gravel in the alluvial fill, and basalt. Water in the shallow deposits is not confined, and the water table generally is less than 10 feet below the surface at most places. Ground water in the deeper deposits occurs chiefly in two horizons that comprise the upper and lower artesian aquifers. Throughout much of the prairie, the pressure is sufficient that water will flow from wells in these aquifers. \r\n\r\nRecharge to the basin is from direct precipitation and percolation of stream runoff from the bordering mountains. Ground water moves from the higher areas at the base of the encircling mountains toward the center of the basin and the eastern outlet. The artesian aquifers leak by upward percolation through the imperfectly confining beds and help maintain the shallow water table. Basalt, which interfingers with the alluvial deposits, is an important aquifer near the southeast margin of the prairie and at the east end. Annual recharge to the artesian aquifers is estimated to be about 40,000 acre-feet. Discharge from the artesian aquifers is about equally divided between upward leakage to the shallow aquifers and underflow out of the prairie. Most of the underflow discharges into Camas Creek or Magic Reservoir east of the prairie; little of the underflow reaches the Snake River Plain. \r\n\r\nWells drilled for irrigation generally yield 500 to 1,200 gallons per minute from the artesian aquifers. Better construction and development methods would result in considerably better yields. Wells drilled in the basalt will yield 2,000 to 3,000 gallons per minute with moderate drawdowns. \r\n\r\nComputations made using aquifer coefficients, estimated on the basis of data collected during the investigation, suggest that 12,000 acre-feet of ground water might be withdrawn annually. However, the aquifers are limited in areal extent, and productivity of the alluvial aquifers is not great. Consequently heavy development would result in large drawdowns in wells, and there would be much interference between wells. The postulated large withdrawals from wells on the prairie would be supplied in part by a reduction in underflow from the prairie and in part by a decrease in leakage from the artesian aquifers, which in turn would cause a decline in the shallow water table.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1609","usgsCitation":"Walton, W.C., 1962, Ground-water resources of Camas Prairie, Camas and Elmore Counties, Idaho: U.S. Geological Survey Water Supply Paper 1609, iv, 57 p. :maps (1 fold. col. in pocket) diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1609.","productDescription":"iv, 57 p. :maps (1 fold. col. in pocket) diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":138988,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1609/report-thumb.jpg"},{"id":29515,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1609/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29516,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1609/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d925","contributors":{"authors":[{"text":"Walton, William Clarence","contributorId":89511,"corporation":false,"usgs":true,"family":"Walton","given":"William","email":"","middleInitial":"Clarence","affiliations":[],"preferred":false,"id":145948,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3506,"text":"cir468 - 1962 - Ground-water studies and analog models","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"cir468","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"468","title":"Ground-water studies and analog models","docAbstract":"Hydrologists make ground-water studies to aid managers and users of water resources in solving their problems in the development and management of ground water. Geologic and hydrologic information provides the basic knowledge for construction of electric analog models that portray the ground-water system in miniature. Analog models can be analyzed electrically, and the results of the analysis are presented in terms of the ground-water system so that the effects of alternative methods of water development can be assessed.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/cir468","usgsCitation":"Robinove, C.J., 1962, Ground-water studies and analog models: U.S. Geological Survey Circular 468, 12 p. :ill. ;27 cm., https://doi.org/10.3133/cir468.","productDescription":"12 p. :ill. ;27 cm.","costCenters":[],"links":[{"id":123185,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1962/0468/report-thumb.jpg"},{"id":30520,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1962/0468/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db696865","contributors":{"authors":[{"text":"Robinove, Charles Joseph","contributorId":71153,"corporation":false,"usgs":true,"family":"Robinove","given":"Charles","email":"","middleInitial":"Joseph","affiliations":[],"preferred":false,"id":147055,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":62042,"text":"mr29 - 1962 - Titanium in the United States, exclusive of Alaska and Hawaii","interactions":[{"subject":{"id":43993,"text":"ofr61130 - 1961 - Titanium in the United States","indexId":"ofr61130","publicationYear":"1961","noYear":false,"title":"Titanium in the United States"},"predicate":"SUPERSEDED_BY","object":{"id":62042,"text":"mr29 - 1962 - Titanium in the United States, exclusive of Alaska and Hawaii","indexId":"mr29","publicationYear":"1962","noYear":false,"title":"Titanium in the United States, exclusive of Alaska and Hawaii"},"id":1}],"lastModifiedDate":"2025-05-23T13:33:48.606875","indexId":"mr29","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":324,"text":"Mineral Investigations Resource Map","code":"MR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"29","title":"Titanium in the United States, exclusive of Alaska and Hawaii","docAbstract":"The accompanying map shows the location of the principal deposits of titanium minerals in the United States (excluding Alaska and Hawaii). Four broad geologic categories of deposits have been distinguished on the map by the shapes of the symbols, and relative importance is indicated by their size. The smaller deposits and the deposits for which adequate data are lacking can only be rated as \"potential, unevaluated, or small\". The deposits placed in the next category have been characterized by modest production or can be described as having \"significant potential\". The larger deposits, for which, more information is available, arc divided into two categories, based on estimated production plus reserves: those containing 1,000,000 to 10,000,000 tons of TiO2, and those having more than 10,000,000 tons of TiO2.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mr29","usgsCitation":"Rogers, C.L., and Jaster, M.C., 1962, Titanium in the United States, exclusive of Alaska and Hawaii: U.S. Geological Survey Mineral Investigations Resource Map 29, Report: 18 p.; 1 Plate: 63.97 x 40.50 inches, https://doi.org/10.3133/mr29.","productDescription":"Report: 18 p.; 1 Plate: 63.97 x 40.50 inches","costCenters":[],"links":[{"id":180500,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mr/29/report-thumb.jpg"},{"id":486413,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/mr/29/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":260488,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mr/29/plate-1.pdf"}],"scale":"3168000","country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -127.25,24.25 ], [ -127.25,49.25 ], [ -66.5,49.25 ], [ -66.5,24.25 ], [ -127.25,24.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699a4c","contributors":{"authors":[{"text":"Rogers, Cleaves Lincoln","contributorId":12858,"corporation":false,"usgs":true,"family":"Rogers","given":"Cleaves","email":"","middleInitial":"Lincoln","affiliations":[],"preferred":false,"id":266767,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jaster, Marion Charlotte","contributorId":27117,"corporation":false,"usgs":true,"family":"Jaster","given":"Marion","email":"","middleInitial":"Charlotte","affiliations":[],"preferred":false,"id":266768,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70007280,"text":"tei816 - 1962 - Thermodynamic properties of minerals","interactions":[],"lastModifiedDate":"2014-07-15T08:07:43","indexId":"tei816","displayToPublicDate":"1963-01-01T13:10:00","publicationYear":"1962","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":"816","title":"Thermodynamic properties of minerals","docAbstract":"In the ten years since the publication of the national Bureau of Standards comprehensive tables of thermochemical properties, by Rossini and other (1952), a very large body of modern calorimetric and equilibrium data has become available. Because of the complex interrelations among many thermochemical data and the necessity for internal consistency among these values, a complete revision of this standard reference is required. This is also true of the summaries of thermochemical data for the sulfides (Richardson and Jeffes 1952) and for the oxides (Coughlin 1954).
\nThe following tables present critically selected values for the heat and free energy of formation, the logarithm of the equilibrium constant of formation Log Kf, the entropy and the molar volume, at 298.15°K (25.0°C) and one atmosphere for minerals.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/tei816","usgsCitation":"Robie, R.A., 1962, Thermodynamic properties of minerals (Also published as USGS Open File Report 62-110): U.S. Geological Survey Trace Elements Investigations 816, 31 p., https://doi.org/10.3133/tei816.","productDescription":"31 p.","numberOfPages":"34","costCenters":[],"links":[{"id":290079,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":290078,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tei/0816/report.pdf"}],"edition":"Also published as USGS Open File Report 62-110","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb276e4b08c986b325804","contributors":{"authors":[{"text":"Robie, Richard A.","contributorId":92235,"corporation":false,"usgs":true,"family":"Robie","given":"Richard","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":356220,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220788,"text":"70220788 - 1962 - Tuscaloosa formation in Tennessee","interactions":[],"lastModifiedDate":"2021-05-25T18:15:12.552445","indexId":"70220788","displayToPublicDate":"1962-11-01T13:10:39","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":"Tuscaloosa formation in Tennessee","docAbstract":"Late Cretaceous Tuscaloosa Formation occurs as discontinuous remnants that cap many of the ridges in the Western Highland Rim. Typically the formation consists of well-rounded, poorly sorted chert gravel which is trimodal in size distribution. The gravel fraction (mode 15 to 40+ mm) consists of Devonian and Mississippian chert and a small percentage of sandstone pebbles. The medium sand fraction (mode 0.5 mm) consists mainly of angular to well-rounded chert grains developed by attrition during transport. Well-rounded and frosted quartz grains also are present. The fine fraction (mode 0.15 mm) consists of clay, authi-genic (?) mica, and quartz. At its eastern limit the Tuscaloosa is locally well sorted and contains quartz pebbles and a large proportion of quartz sand. Also present in the same area are well-sorted, heavy-mineral-bearing sands and bimodal (0.04, 0.2 mm) siltstone, which contains sand-sized pellet aggregates and fragmentary plant fossils. The finest fraction (less than 0.044 mm) of both eastern and western facies of the Tuscaloosa consists of 60-80 per cent quartz, 5-30 per cent kaolin, and 5-30 per cent montmorillonite, all of which are present in Devonian and Mississippian bedrock. Minor exotic constituents include volcanic(?) glass and heavy minerals. The Mississippian chert gravel in the Tuscaloosa is of local origin, but the Devonian chert was transported from a western source. Other components from a western source are sandstone pebbles and frosted sand grains, both of which probably were derived from Cambrian or Ordovician formations that cropped out on the Pascola arch, an eastward-sloping extension of the Ozark dome. Quartz pebbles, heavy minerals, and some of the angular quartz sand present at the eastern edge of the Tuscaloosa may have been derived from Pennsylvanian sandstone and conglomerates that cropped out north and south of the Pascola arch. Most of the Tuscaloosa Formation is believed to be of nonmarine origin, deposited on the eastward-sloping flank of the Pascola arch. The eastern facies of the Tuscaloosa is believed to be partly marine in origin, the exotic components having been swept in by longshore currents. During deposition of the Tuscaloosa, the Ozark dome and the Cincinnati arch were connected by the Pascola arch, which is now deeply buried beneath the Mississippi Embayment, At that time the Pascola arch stood structurally about 3000 feet higher than at present, and its structural shape and dimensions were comparable to the present Nashville dome. During deposition of the Tuscaloosa the Nashville dome was structurally about 1000 feet lower than at present, and its crest probably was submerged beneath the sea.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1962)73[1365:TFIT]2.0.CO;2","usgsCitation":"Marcher, M., and Stearns, R.G., 1962, Tuscaloosa formation in Tennessee: Geological Society of America Bulletin, v. 73, no. 11, p. 1365-1386, https://doi.org/10.1130/0016-7606(1962)73[1365:TFIT]2.0.CO;2.","productDescription":"22 p.","startPage":"1365","endPage":"1386","costCenters":[],"links":[{"id":385953,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Tennessee","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -89.82421875,\n 35.11990857099681\n ],\n [\n -82.52929687499999,\n 35.11990857099681\n ],\n [\n -82.52929687499999,\n 36.5978891330702\n ],\n [\n -89.82421875,\n 36.5978891330702\n ],\n [\n -89.82421875,\n 35.11990857099681\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"73","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Marcher, M.V.","contributorId":9267,"corporation":false,"usgs":true,"family":"Marcher","given":"M.V.","affiliations":[],"preferred":false,"id":816467,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stearns, R. G.","contributorId":95859,"corporation":false,"usgs":true,"family":"Stearns","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":816468,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70220655,"text":"70220655 - 1962 - Observations on the pyrite deposits of the huelva district, Spain, and their relation to volcanism","interactions":[],"lastModifiedDate":"2021-05-24T12:19:51.371943","indexId":"70220655","displayToPublicDate":"1962-11-01T07:13:42","publicationYear":"1962","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":"Observations on the pyrite deposits of the huelva district, Spain, and their relation to volcanism","docAbstract":"The felsitic porphyritic rocks that occur with Lower Carboniferous shale or slate in the Huelva district, Spain, were examined at the Rio Tinto, Tharsis, and La Zarza mines. Most of the bodies of porphyry are not intrusive into the shale, but instead consist of rhyolite flows overlain by variable thicknesses of coarse and fine pyroclastic rhyolite. These lie conformably beneath the shale. The pyroclastic beds are the ore horizon, and the ore bodies are confined to this stratigraphic zone. Various modes of formation have been postulated for the ore bodies of the Huelva district. The apparent limitation of ore to one strati-graphic horizon for more than 100 kilometers seems to favor a modified syngenetic origin with metallic elements derived from volcanic emanations.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.57.7.1071","usgsCitation":"Kinkel, A., 1962, Observations on the pyrite deposits of the huelva district, Spain, and their relation to volcanism: Economic Geology, v. 57, no. 7, p. 1071-1080, https://doi.org/10.2113/gsecongeo.57.7.1071.","productDescription":"10 p.","startPage":"1071","endPage":"1080","costCenters":[],"links":[{"id":385881,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Spain","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -9.140625,\n 41.77131167976407\n ],\n [\n -8.349609375,\n 42.22851735620852\n ],\n [\n -7.998046875,\n 42.00032514831621\n ],\n [\n -6.50390625,\n 41.96765920367816\n ],\n [\n -6.240234374999999,\n 41.50857729743935\n ],\n [\n -6.85546875,\n 40.91351257612758\n ],\n [\n -6.85546875,\n 39.977120098439634\n ],\n [\n -7.250976562499999,\n 39.639537564366684\n ],\n [\n -7.163085937499999,\n 39.095962936305476\n ],\n [\n -7.250976562499999,\n 38.47939467327645\n ],\n [\n -7.338867187500001,\n 37.75334401310656\n ],\n [\n -7.3828125,\n 37.19533058280065\n ],\n [\n -5.8447265625,\n 35.92464453144099\n ],\n [\n -1.9775390625,\n 36.80928470205937\n ],\n [\n -0.8349609375,\n 37.71859032558816\n ],\n [\n 0.3076171875,\n 38.788345355085625\n ],\n [\n 3.4716796874999996,\n 42.06560675405716\n ],\n [\n 2.98828125,\n 42.52069952914966\n ],\n [\n 0.8349609375,\n 42.8115217450979\n ],\n [\n -1.9335937499999998,\n 43.48481212891603\n ],\n [\n -7.646484374999999,\n 43.739352079154706\n ],\n [\n -8.173828125,\n 43.644025847699496\n ],\n [\n -9.31640625,\n 43.004647127794435\n ],\n [\n -9.140625,\n 41.77131167976407\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"57","issue":"7","noUsgsAuthors":false,"publicationDate":"1962-11-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Kinkel, A.R. Jr.","contributorId":87200,"corporation":false,"usgs":true,"family":"Kinkel","given":"A.R.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":816307,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220653,"text":"70220653 - 1962 - Trace element distribution in the searchlight, Nevada quartz monzonite stock","interactions":[],"lastModifiedDate":"2021-05-24T12:04:48.097911","indexId":"70220653","displayToPublicDate":"1962-11-01T07:01:09","publicationYear":"1962","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":"Trace element distribution in the searchlight, Nevada quartz monzonite stock","docAbstract":"Gold, silver, copper, and lead-bearing veins, non-radially zoned, occur just beyond the southern and western margins of the Searchlight, Nevada, quartz monzonite stock. Seven samples of the quartz monzonite and purified individual constituent minerals of the rock, representing apophyses and marginal and interior parts of the intrusive mass, were analyzed petrographically and spectrographically. A semiquantitative total-energy spectrographic method proved satisfactory for Cu, Pb, Ni, Co, Ga, Mo, Mn, Ti, V, Cr, Sr, and Zr, but too insensitive for Zn, Ag, and Au. A synthetic silicate base was used for preparation of standards and working curves. The modal trace element content of unaltered (hypothetical) quartz monzonite samples was determined from the trace element content of the purified minerals. Ferromagnesian minerals contain concentrations of Cu, Pb, Ni, Co, Mn, and Cr. Felsic minerals are low in these but high in Sr and Ga. Cu appears to have been partly released during chloritization of the mafic minerals. Ni, Cr, Zr show little difference between the unaltered (hypothetical) and actual rock. Ga, V, Mn, Sr are in lesser quantities in the altered rock. Pb and Cu also show a loss, especially nearest largest Pb and Cu producers. Pb, Cu, V occur in the spatially related veins, but Sr or Ga have not been reported to date. Pb/Cu in unaltered rock compared to altered rock is 1.6/1; past mining production ratio of Pb/Cu is 2.6/1. While further work is needed, the trace element pattern suggests a possible means of identifying a \"productive\" intrusive body.
","language":"English","publisher":"Society for Economic Geologist","doi":"10.2113/gsecongeo.57.7.1062","usgsCitation":"Shrivastava, J., and Proctor, P., 1962, Trace element distribution in the searchlight, Nevada quartz monzonite stock: Economic Geology, v. 57, no. 7, p. 1062-1070, https://doi.org/10.2113/gsecongeo.57.7.1062.","productDescription":"9 p.","startPage":"1062","endPage":"1070","costCenters":[],"links":[{"id":385879,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"57","issue":"7","noUsgsAuthors":false,"publicationDate":"1962-11-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Shrivastava, J.N.","contributorId":258272,"corporation":false,"usgs":false,"family":"Shrivastava","given":"J.N.","email":"","affiliations":[],"preferred":false,"id":816304,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Proctor, P.D.","contributorId":45391,"corporation":false,"usgs":true,"family":"Proctor","given":"P.D.","email":"","affiliations":[],"preferred":false,"id":816305,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70220657,"text":"70220657 - 1962 - The origin of jasperoid in limestone","interactions":[],"lastModifiedDate":"2021-05-24T12:37:43.054398","indexId":"70220657","displayToPublicDate":"1962-09-01T07:33:31","publicationYear":"1962","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":"The origin of jasperoid in limestone","docAbstract":"The name jasperoid has been applied to rocks that consist mainly of silica and that have formed by replacement. This paper considers only those jasperoids formed by replacement of limestone. Major problems involved in the origin of such jasperoid include: source of the silica; nature of solutions that dissolve, transport, and precipitate silica; and the mechanism of replacement of limestone by silica. The answers to these problems are of practical as well as scientific interest because many jasperoid bodies are closely related to mineralization. Silica may be derived from: juvenile silica of magmatic origin; silica leached from underlying rocks by hydrothermal solutions; silica locally derived from enclosing rocks by circulating solutions; and silica carried downward in ground water from the weathering of overlying rocks. The nature and the concentration of other substances in solutions influence,in a complex manner, the ability of these solutions to dissolve, transport, and precipitate silica. Nevertheless, the following generalizations can be made. The solubility and rate of solution of silica in water at moderate pressure increase slowly with temperature up to 200 degrees C.; from 200 degrees to 360 degrees C. they increase rapidly; above 360 degrees C. solubility is pressure dependent, increasing steadily at high pressure and decreasing slightly at moderate pressure due to the formation of a vapor phase. The pH has slight effect on the ionic solubility of silica in the range from pH 1 to ph 9 at low temperature. The effect of other components on the solubility of silica is probably subordinate to that of temperature above 200 degrees C., but becomes increasingly important as the temperature falls below that point. Most jasperoid bodies form by both replacement and silica deposition in voids, with replacement dominant during the early phase, and precipitation dominant during later phases. Replacement of limestone by silica is favored by relatively low temperature acid solutions, and the presence of CO 2 . As limestone dissolves, Ca ions are released to promote the precipitation of colloidal silica. Acid solutions then diffuse through this gelatinous film to continue dissolving limestone behind it; the Ca ions diffusing outward cause the precipitation of more colloidal silica at the solution-gel interface. As the gel mass ages, it shrinks, hardens, and ruptures. More silica is then deposited in the fractures. Eventually the gel crystallizes to a dense mass of aphanitic quartz and chalcedony, with shrinkage cracks and vugs filled or coated with younger coarse-grained quartz and other minerals that have been deposited directly from solution. The theory that relatively low temperature favors the formation of jasperoid replacement bodies in carbonate rocks, and high temperature inhibits their formation, offers an explanation for the gap that is observed in some districts between contact metasomatic lime silicates and siliceous replacement of limestone. This gap is characterized by the lack of any reaction between limestone and silica-bearing solutions moving through it.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.57.6.861","usgsCitation":"Lovering, T., 1962, The origin of jasperoid in limestone: Economic Geology, v. 57, no. 6, p. 861-889, https://doi.org/10.2113/gsecongeo.57.6.861.","productDescription":"29 p.","startPage":"861","endPage":"889","costCenters":[],"links":[{"id":385883,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"57","issue":"6","noUsgsAuthors":false,"publicationDate":"1962-09-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Lovering, T.G.","contributorId":91098,"corporation":false,"usgs":true,"family":"Lovering","given":"T.G.","email":"","affiliations":[],"preferred":false,"id":816309,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220764,"text":"70220764 - 1962 - Distribution and composition of sulfide minerals at Balmat, New York","interactions":[],"lastModifiedDate":"2021-05-25T17:00:24.762347","indexId":"70220764","displayToPublicDate":"1962-07-01T11:54:41","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":"Distribution and composition of sulfide minerals at Balmat, New York","docAbstract":"In the Balmat area in northern New York, tabular deposits of sulfide minerals parallel the layering in folded, siliceous magnesian marbles of a metamorphic complex commonly referred to as the Precambrian Granville Series. Sphalerite, pyrite, and, locally, pyrrhotite and galena have replaced the carbonate minerals in parts of the marble units. The contacts between ore and marble are, in general, ill-defined; scattered grains of sulfides are present from several inches to hundreds of feet from the massive portions of ore. Access to the ore is provided through the Balmat No. 2 and No. 3 mines. The isotopic composition of lead from primary galena is uniform within an individual mine. The model age of this lead agrees with the age of the mineralization determined by other means - about a billion years. The isotopic composition of the leads in the marble is not uniform today, and calculations indicate that it was probably not uniform a billion years ago. Unless the lead in the ores is a uniform mixture of lead isotopes from an isotopically poorly mixed source, it is doubtful that the lead in the ores was derived from the surrounding marbles. Cobalt and nickel concentrations in pyrite from grains disseminated in the metasedimentary rocks away from the ore bodies are each greater than 200 ppm. Most samples of pyrite from the ore bodies at the No. 2 and No. 3 mines contain less than 50 ppm each of cobalt and nickel. Therefore the author believes it unlikely that the pyrite of the ores is genetically related to the pyrite in the metasedimentary rocks. Textural relationships suggest that pyrrhotite formed after most of the sphalerite, which in turn formed after most of the pyrite in the ore bodies. By use of the experimentally determined systems FeS-ZnS and FeS-FeS2, it is inferred from the amounts of iron in sphalerite and sulfur in pyrrhotite that the bulk of the sulfide minerals in the No. 2 mine formed above 320° C. The absolute temperature of formation of pyrrhotite indicated by the FeS-ZnS system is about 150° higher than that indicated by the FeS-FeS2 system. The former system probably gives the more reliable estimate. The concentrations of individual minor elements in sphalerite and pyrite range considerably among specimens of the same sulfide mineral from the same level and ore body. An exception is cadmium in sphalerite which has a narrow concentration range around 1400 ppm in both the No. 2 and No. 3 mines. The ratio of the concentrations of minor elements between sphalerite-pyrite pairs varies considerably also. This variation probably indicates that exchange of minor elements between pyrite and sphalerite durin g the formation of the ores was very slow and incomplete.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1962)73[833:DACOSM]2.0.CO;2","usgsCitation":"Doe, B.R., 1962, Distribution and composition of sulfide minerals at Balmat, New York: Geological Society of America Bulletin, v. 73, no. 7, p. 833-854, https://doi.org/10.1130/0016-7606(1962)73[833:DACOSM]2.0.CO;2.","productDescription":"22 p.","startPage":"833","endPage":"854","costCenters":[],"links":[{"id":480372,"rank":0,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://doi.org/10.7907/y53k-nc70","text":"External Repository"},{"id":385944,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New York","city":"Gouverneur","otherGeospatial":"Balmat","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.53787231445312,\n 44.213709909702054\n ],\n [\n -75.399169921875,\n 44.213709909702054\n ],\n [\n -75.399169921875,\n 44.37785821716272\n ],\n [\n -75.53787231445312,\n 44.37785821716272\n ],\n [\n -75.53787231445312,\n 44.213709909702054\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"73","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Doe, Bruce R.","contributorId":87554,"corporation":false,"usgs":true,"family":"Doe","given":"Bruce","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":816455,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010571,"text":"70010571 - 1962 - Temperature dependence of decay time and intensity of alpha pulses in pure and thallium-activated cesium iodide","interactions":[],"lastModifiedDate":"2020-11-19T17:46:33.453266","indexId":"70010571","displayToPublicDate":"1962-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3276,"text":"Review of Scientific Instruments","active":true,"publicationSubtype":{"id":10}},"title":"Temperature dependence of decay time and intensity of alpha pulses in pure and thallium-activated cesium iodide","docAbstract":"The intensity and decay time of Po210 alpha particle scintillations produced in pure and thallium‐activated cesium iodide have been measured with a fast electronic system as a function of temperature down to 77°K. Three modes of decay due to alpha excitation have been observed for CsI(Tl), and two for CsI. Other than the 7‐ and 0.55‐μsec modes (at room temperature) reported in the literature for CsI(Tl), an additional temperature‐independent mode of about 1.3 μsec has been detected between 77 and 150°K. In CsI a fast temperature‐dependent mode of decay (≈100 nsec) was observed between 100–200°K in addition to the known principal mode.
","language":"English","publisher":"AIP Publishing","doi":"10.1063/1.1717979","usgsCitation":"Senftle, F.E., Martinez, P., and Alekna, V.P., 1962, Temperature dependence of decay time and intensity of alpha pulses in pure and thallium-activated cesium iodide: Review of Scientific Instruments, v. 33, no. 8, p. 819-822, https://doi.org/10.1063/1.1717979.","productDescription":"4 p.","startPage":"819","endPage":"822","numberOfPages":"4","costCenters":[],"links":[{"id":219019,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"33","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505ba4c1e4b08c986b320570","contributors":{"authors":[{"text":"Senftle, F. E.","contributorId":47788,"corporation":false,"usgs":true,"family":"Senftle","given":"F.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":359199,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Martinez, P.","contributorId":38706,"corporation":false,"usgs":true,"family":"Martinez","given":"P.","email":"","affiliations":[],"preferred":false,"id":359198,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Alekna, V. P.","contributorId":35459,"corporation":false,"usgs":true,"family":"Alekna","given":"V.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":359197,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2000020,"text":"2000020 - 1962 - A photoelectric amplifier as a dye detector","interactions":[],"lastModifiedDate":"2013-01-28T14:07:08","indexId":"2000020","displayToPublicDate":"1962-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":3,"text":"Organization Series"},"seriesTitle":{"id":222,"text":"Technical Report","active":false,"publicationSubtype":{"id":3}},"seriesNumber":"4","title":"A photoelectric amplifier as a dye detector","docAbstract":"A dye detector, based on a modified photoelectric amplifier, has been planned, built, and tested. It was designed to record automatically the time of arrival of fluorescein dye at predetermined points in a stream system. Laboratory tests and stream trials proved the instrument to be efficient. Small changes in color can be detected in turbid or clear water. The unit has been used successfully for timing intervals of more than 17 hours; significant savings of time and manpower have resulted. Replacement of the clock, included in the original device, with a recording milliammeter increases the efficiency of the unit by contin,!ously recording changes in turbidity. The addition of this component would increase the cost from $75 to approximately $105.","language":"English","publisher":"Great Lakes Fishery Commission","usgsCitation":"Ebel, W.J., 1962, A photoelectric amplifier as a dye detector: Technical Report 4, p. 19-26.","productDescription":"p. 19-26","startPage":"19","endPage":"26","numberOfPages":"8","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":198043,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":92069,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://www.glfc.org/pubs/TechReports/Tr04.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1fe4b07f02db6ab801","contributors":{"authors":[{"text":"Ebel, Wesley J.","contributorId":88307,"corporation":false,"usgs":true,"family":"Ebel","given":"Wesley","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":324938,"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":"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.
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.
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.
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.
","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":70176018,"text":"70176018 - 1961 - Geology and ground-water resources of Sumner County, Kansas","interactions":[],"lastModifiedDate":"2018-09-27T11:55:07","indexId":"70176018","displayToPublicDate":"2015-11-16T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2579,"text":"Kansas Geological Survey Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Geology and ground-water resources of Sumner County, Kansas","docAbstract":"This report describes the geography, geology, and ground-water resources of Sumner County in south-central Kansas. The hydrologic and geologic data upon which this report is based were obtained in the field during the summers of 1955 and 1956. Records of 300 wells and 2 springs, chemical analyses of 219 water samples from wells and test holes and of 15 from streams, and logs of 362 wells and test holes are included in tables.
Sumner County has an area of 1,183 square miles and lies in the Wellington Lowland and Arkansas River Lowlands of the Central Lowland physiographic province. It is drained by Arkansas River, Ninnescah River, and Chikaskia River and their tributaries. The land surface in general is a southeastward-sloping, gently rolling plain. The average annual precipitation at Wellington is about 31 inches. Wheat fanning is the principal industry of the county, and oil is the chief natural resource.
The Wellington Formation, of Permian age, crops out in the eastern two-thirds of the county except where it is covered by Pleistocene deposits. The Ninnescah Shale (Permian) overlies the Wellington Formation and crops out in parts of the western third of the county. The Permian rocks yield small quantities of hard water to wells. Pleistocene sand and gravel deposits of Nebraskan age are present in the northwestern corner of the county and yield moderate quantities of good water to wells. Discontinuous deposits of Kansan or Illinoisan age, locally mantled by colluvium, forms terraces in southern and eastern Sumner County, and may yield moderate quantities of water. Wisconsinan terrace deposits and Recent alluvium along the major streams yield large quantities of water. Colluvium and dune sand are unimportant as sources of water but may facilitate recharge.
Maps of Sumner County included in this report show the outcrop areas of the formations, geologic cross sections, the shape and slope of the water table, the locations of wells and test holes for which records are given, and the distribution of chloride in water samples.
The ground-water reservoir is recharged principally from rain and snow that fall within the county, by percolation from streams and other surface bodies of water, and by underflow from adjacent areas. Water is discharged from the ground-water reservoir by seepage into streams, by transpiration and evaporation, by movement into adjacent areas, and by wells. Water is pumped from wells for domestic, stock, municipal, industrial, and irrigation use. Irrigation from wells is most extensive in the valley of Arkansas River, in which area further development is most probable.
Chemical analyses of samples of water from Sumner County indicate that the quality varies greatly from place to place. Sulfate is common in water from the Wellington Formation and Ninnescah Shale. Water from Pleistocene deposits is generally suitable for most uses except in local areas where it contains excessive chloride.
","language":"English","publisher":"University of Kansas","publisherLocation":"Lawrence, KS","usgsCitation":"Walters, K., 1961, Geology and ground-water resources of Sumner County, Kansas: Kansas Geological Survey Bulletin, v. 151, 198 p. .","productDescription":"198 p. ","costCenters":[{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"links":[{"id":327735,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":327734,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://www.kgs.ku.edu/General/Geology/Sumner/index.html"}],"volume":"151","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57bd73dbe4b03fd6b7df2ce7","contributors":{"authors":[{"text":"Walters, K.L.","contributorId":105765,"corporation":false,"usgs":true,"family":"Walters","given":"K.L.","affiliations":[],"preferred":false,"id":646804,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"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":"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.
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.
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.
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.
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.
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.
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.
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.
","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 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":100043,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-48.pdf","text":"Plate 48","size":"5.31 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 48"},{"id":100044,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-49.pdf","text":"Plate 49","size":"889 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 49"},{"id":100045,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-50.pdf","text":"Plate 50","size":"411 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 50"},{"id":100046,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-51.pdf","text":"Plate 51","size":"308 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 51"},{"id":100047,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-52.pdf","text":"Plate 52","size":"309 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 52"},{"id":100048,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-53.pdf","text":"Plate 53","size":"387 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 53"},{"id":100049,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-54.pdf","text":"Plate 54","size":"872 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 54"},{"id":172973,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082l/report-thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"Colorado River, Piceance Creek basin, White River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -109.05303955078125,\n 40.04023218690451\n ],\n [\n -109.04754638671875,\n 39.2832938689385\n ],\n [\n -108.9349365234375,\n 39.24501680713314\n ],\n [\n -108.78662109375,\n 39.16839998800286\n ],\n [\n -108.56414794921875,\n 39.06718050308463\n ],\n [\n -108.44741821289062,\n 39.04585261214505\n ],\n [\n -108.32794189453125,\n 39.10768574604533\n ],\n [\n -108.23181152343749,\n 39.308800296002914\n ],\n [\n -108.09860229492188,\n 39.4054277294279\n ],\n [\n -107.841796875,\n 39.51145753426751\n ],\n [\n -107.72918701171875,\n 39.59722324495565\n ],\n [\n -107.71820068359374,\n 39.71986348549764\n ],\n [\n -107.81158447265624,\n 39.84439484396462\n ],\n [\n -108.0010986328125,\n 39.9434364619742\n ],\n [\n -108.15490722656249,\n 40.052847601823984\n ],\n [\n -108.30047607421876,\n 40.143189742924406\n ],\n [\n -108.42132568359375,\n 40.19670806662855\n ],\n [\n -108.533935546875,\n 40.18307014852534\n ],\n [\n -108.67538452148438,\n 40.163132874122084\n ],\n [\n -108.7591552734375,\n 40.09908414736847\n ],\n [\n -109.05303955078125,\n 40.04023218690451\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db68500d","contributors":{"authors":[{"text":"Donnell, John R.","contributorId":84330,"corporation":false,"usgs":true,"family":"Donnell","given":"John R.","affiliations":[],"preferred":false,"id":235200,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3523,"text":"cir450 - 1961 - Sonic depth sounder for laboratory and field use","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"cir450","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":"450","title":"Sonic depth sounder for laboratory and field use","docAbstract":"The laboratory investigation of roughness in alluvial channels has led to the development of a special electronic device capable of mapping the streambed configuration under dynamic conditions. This electronic device employs an ultrasonic pulse-echo principle, similar to that of a fathometer, that utilizes microsecond techniques to give high accuracy in shallow depths. This instrument is known as the sonic depth sounder and was designed to cover a depth range of 0 to 4 feet with an accuracy of ? 0.5 percent. The sonic depth sounder is capable of operation at frequencies of 500, 1,000 and 2,000 kilocycles. The ultrasonic beam generated at the transducer is designed to give a minimum-diameter interrogating signal over the extended depth range. The information obtained from a sonic depth sounder is recorded on a strip-chart recorder. This permanent record allows an analysis to be made of the streambed configuration under different dynamic conditions. \r\n\r\nThe model 1024 sonic depth sounder was designed principally as a research instrument to meet laboratory needs. As such, it is somewhat limited in its application as a field instrument on large streams and rivers. The principles employed in this instrument, however, have many potentials for field applications such as the indirect measurement of bed load when the bed roughness is ripples and (or) dunes, depth measurement, determination of bed configuration, and determination of depth of scour around bridge piers and abutments. For field application a modification of the present system into a battery-operated lightweight instrument designed to operate at a depth range of 0 to 30 feet is possible and desirable.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/cir450","usgsCitation":"Richardson, E., Simons, D., and Posakony, G., 1961, Sonic depth sounder for laboratory and field use: U.S. Geological Survey Circular 450, 7 p. :graphs ;27 cm., https://doi.org/10.3133/cir450.","productDescription":"7 p. :graphs ;27 cm.","costCenters":[],"links":[{"id":124420,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1961/0450/report-thumb.jpg"},{"id":30537,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1961/0450/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4b6b","contributors":{"authors":[{"text":"Richardson, E.V.","contributorId":105697,"corporation":false,"usgs":true,"family":"Richardson","given":"E.V.","email":"","affiliations":[],"preferred":false,"id":147088,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Simons, Daryl B.","contributorId":35715,"corporation":false,"usgs":true,"family":"Simons","given":"Daryl B.","affiliations":[],"preferred":false,"id":147087,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Posakony, G.J.","contributorId":13211,"corporation":false,"usgs":true,"family":"Posakony","given":"G.J.","email":"","affiliations":[],"preferred":false,"id":147086,"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":"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.
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.
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.
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.
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.
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.
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.
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.
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.
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.
","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":1165,"text":"wsp1593 - 1961 - Simplified methods for computing total sediment discharge with the modified Einstein procedure","interactions":[{"subject":{"id":55755,"text":"ofr5721 - 1957 - Simplified methods for computing total sediment discharge with the modified Einstein procedure","indexId":"ofr5721","publicationYear":"1957","noYear":false,"title":"Simplified methods for computing total sediment discharge with the modified Einstein procedure"},"predicate":"SUPERSEDED_BY","object":{"id":1165,"text":"wsp1593 - 1961 - Simplified methods for computing total sediment discharge with the modified Einstein procedure","indexId":"wsp1593","publicationYear":"1961","noYear":false,"title":"Simplified methods for computing total sediment discharge with the modified Einstein procedure"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1593","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":"1593","title":"Simplified methods for computing total sediment discharge with the modified Einstein procedure","docAbstract":"A procedure was presented in 1950 by H. A. Einstein for computing the total discharge of sediment particles of sizes that are in appreciable quantities in the stream bed. This procedure was modified by the U.S. Geological Survey and adapted to computing the total sediment discharge of a stream on the basis of samples of bed sediment, depth-integrated samples of suspended sediment, streamflow measurements, and water temperature. This paper gives simplified methods for computing total sediment discharge by the modified Einstein procedure. Each of four homographs appreciably simplifies a major step in the computations. Within the stated limitations, use of the homographs introduces much less error than is present in either the basic data or the theories on which the computations of total sediment discharge are based. The results are nearly as accurate mathematically as those that could be obtained from the longer and more complex arithmetic and algebraic computations of the Einstein procedure.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1593","usgsCitation":"Colby, B.R., and Hubbell, D.W., 1961, Simplified methods for computing total sediment discharge with the modified Einstein procedure: U.S. Geological Survey Water Supply Paper 1593, vi, 17 p. ;24 cm., https://doi.org/10.3133/wsp1593.","productDescription":"vi, 17 p. ;24 cm.","costCenters":[],"links":[{"id":137129,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1593/report-thumb.jpg"},{"id":26000,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1593/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":264358,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-1.pdf","size":"3161","linkFileType":{"id":1,"text":"pdf"}},{"id":264359,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-2.pdf","size":"2582","linkFileType":{"id":1,"text":"pdf"}},{"id":264360,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-3.pdf","size":"1606","linkFileType":{"id":1,"text":"pdf"}},{"id":264361,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-4.pdf","size":"355","linkFileType":{"id":1,"text":"pdf"}},{"id":264362,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-5.pdf","size":"1808","linkFileType":{"id":1,"text":"pdf"}},{"id":264363,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-6.pdf","size":"1599","linkFileType":{"id":1,"text":"pdf"}},{"id":264364,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-7.pdf","size":"4402","linkFileType":{"id":1,"text":"pdf"}},{"id":264365,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-8.pdf","size":"4532","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f9e4b07f02db5f38d7","contributors":{"authors":[{"text":"Colby, Bruce R.","contributorId":59775,"corporation":false,"usgs":true,"family":"Colby","given":"Bruce","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143287,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hubbell, David Wellington","contributorId":88330,"corporation":false,"usgs":true,"family":"Hubbell","given":"David","email":"","middleInitial":"Wellington","affiliations":[],"preferred":false,"id":143288,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1705,"text":"wsp1475F - 1961 - Ground Water at Grant Village Site, Yellowstone National Park, Wyoming","interactions":[],"lastModifiedDate":"2012-02-10T00:10:06","indexId":"wsp1475F","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":"F","title":"Ground Water at Grant Village Site, Yellowstone National Park, Wyoming","docAbstract":"On behalf of the National Park Service, the U.S. Geological Survey during the summer of 1959 made a study of ground-water conditions in the area of the Grant Village site, along the shore of the West Thumb of Yellowstone Lake, 1 to 2 miles south of the present facilities at West Thumb. The water supply for the present development at West Thumb is obtained from Duck Lake, but the quantity of water available from this source probably will be inadequate for the planned development at Grant Village.\r\n\r\nDuring the investigation, 11 auger holes were bored and 6 test wells were drilled. Aquifer tests by pumping and bailing methods were made at two of the test wells. All material penetrated in the auger holes and test wells is of Quaternary age except the welded tuff of possible Pliocene age that was penetrated in the lower part of test well 4.\r\n\r\nSmall to moderate quantities of water were obtained from the test wells in the area. Test well 2 yielded 35 gpm (gallons per minute) at a temperature of nearly 100 deg F. Test well 6 yielded about 15 gpm at a temperature of 48 deg F. The yield of this well might be increased by perforation of additional sections of casing, followed by further development of the well. Water from the other four test wells was of inadequate quantity, too highly mineralized, or too warm to be effectively utilized.\r\n\r\nMost of the ground water sampled had high concentrations of silica and iron, and part of the water was excessively high in fluoride content. Otherwise, the ground water was of generally suitable quality for most uses.\r\n\r\nThe most favorable area for obtaining water supplies from wells is near the lakeshore, where a large part of the water pumped would be ground-water flow diverted from its normal discharge into the lake. Moderate quantities of relatively cool water of fairly good quality may be available near the lakeshore between test wells 5 and 6 and immediately east of test well 6.","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/wsp1475F","collaboration":"Prepared in cooperation with the National Park Service","usgsCitation":"Gordon, E.D., McCullough, R.A., and Weeks, E.P., 1961, Ground Water at Grant Village Site, Yellowstone National Park, Wyoming: U.S. Geological Survey Water Supply Paper 1475, 173-200 p., https://doi.org/10.3133/wsp1475F.","productDescription":"173-200 p.","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":12519,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://www.nps.gov/history/history/online_books/geology/publications/wsp/1475-F/","linkFileType":{"id":5,"text":"html"}},{"id":137092,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1475f/report-thumb.jpg"},{"id":26783,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1475f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -110.66666666666667,44.25 ], [ -110.66666666666667,44.5 ], [ -110.33333333333333,44.5 ], [ -110.33333333333333,44.25 ], [ -110.66666666666667,44.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abae4b07f02db671f58","contributors":{"authors":[{"text":"Gordon, Ellis D.","contributorId":12451,"corporation":false,"usgs":true,"family":"Gordon","given":"Ellis","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":143995,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McCullough, Richard A.","contributorId":78712,"corporation":false,"usgs":true,"family":"McCullough","given":"Richard","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":143996,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Weeks, Edwin P. epweeks@usgs.gov","contributorId":2576,"corporation":false,"usgs":true,"family":"Weeks","given":"Edwin","email":"epweeks@usgs.gov","middleInitial":"P.","affiliations":[],"preferred":true,"id":143994,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":39012,"text":"pp366 - 1961 - Ash-flow tuffs: Their origin, geologic relations, and identification","interactions":[],"lastModifiedDate":"2013-11-07T10:52:43","indexId":"pp366","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"366","title":"Ash-flow tuffs: Their origin, geologic relations, and identification","docAbstract":"Pyroclastic materials, which are interpreted as having been deposited by flowage as a suspension of ash in volcanic gas, are becoming widely recognized as major geologic episodes. These may be unconsolidated, indurated by partial welding, or welded into a compact rock. Many students are working on these materials and the interest in them is so widespread that need for a coordinated treatise on them has developed. This report deals with the history of the concept of their origin; gives detailed descriptions of their character and mode of occurrence; gives criteria for their recognition; and considers their distribution and consolidation.","language":"English","publisher":"United States Government Printing Office","doi":"10.3133/pp366","usgsCitation":"Ross, C., and Smith, R.L., 1961, Ash-flow tuffs: Their origin, geologic relations, and identification: U.S. Geological Survey Professional Paper 366, vi, 80 p., https://doi.org/10.3133/pp366.","productDescription":"vi, 80 p.","numberOfPages":"87","costCenters":[],"links":[{"id":172491,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0366/report-thumb.jpg"},{"id":268972,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0366/report.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abbe4b07f02db672ba8","contributors":{"authors":[{"text":"Ross, Clarence S.","contributorId":7251,"corporation":false,"usgs":true,"family":"Ross","given":"Clarence S.","affiliations":[],"preferred":false,"id":220802,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Smith, Robert L.","contributorId":90803,"corporation":false,"usgs":true,"family":"Smith","given":"Robert","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":220803,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":13417,"text":"ofr6142 - 1961 - Geology of uranium in the Chadron area, Nebraska and South Dakota","interactions":[],"lastModifiedDate":"2012-02-02T00:06:50","indexId":"ofr6142","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":"61-42","title":"Geology of uranium in the Chadron area, Nebraska and South Dakota","docAbstract":"The Chadron area covers 375 square miles about 25 miles southeast of the Black Hills. Recurrent mild tectonic activity and erosion on the Chadron arch, a compound anticlinal uplift of regional extent, exposed 1900 feet of Upper Cretaceous rocks, mostly marine shale containing pyrite and organic matter, and 600 feet of Oligocene and Miocene rocks, mostly terrestrial fine-grained sediment containing volcanic ash. Each Cretaceous formation truncated by the sub-Oligocene unconformity is stained yellow and red, leached, kaolinized, and otherwise altered to depths as great as 55 feet. The composition and profile of the altered material indicate lateritic soil; indirect evidence indicates Eocene(?) age. In a belt through the central part of the area, the Brule formation of Oligocene age is a sequence of bedded gypsum, clay, dolomite, and limestone more than 300 feet thick.\r\n\r\nUranium in Cretaceous shale in 58 samples averages 0.002 percent, ten times the average for the earth\u0019s crust. Association with pyrite and organic matter indicates low valency. The uranium probably is syngenetic or nearly so.\r\n\r\nUranium in Eocene(?) soil in 43 samples averages 0.054 percent, ranging up to 1.12 percent. The upper part of the soil is depleted in uranium; enriched masses in the basal part of the soil consist of remnants of bedrock shale and are restricted to the highest reaches of the ancient oxidation-reduction interface. The uranium is probably in the from of a low-valent mineral, perhaps uraninite. Modern weathering of Cretaceous shale is capable of releasing as much as 0.780 ppm uranium to water. Eocene(?) weathering probably caused enrichment of the ancient soil through 1) leaching of Cretaceous shale, 2) downward migration of uranyl complex ions, and 3) reduction of hydrogen sulfide at the water table.\r\n\r\nUranium minerals occur in the basal 25 feet of the gypsum facies of the Brule formation at the two localities where the gypsum is carbonaceous; 16 samples average 0.066 percent uranium and range up to 0.43 percent. Elsewhere uranium in dolomite and limestone in the basal 25 feet of the gypsum facies in 10 samples averages 0.007 percent, ranging up to 0.12 percent. Localization of the uranium at the base of the gypsum facies suggests downward moving waters; indirect evidence that the water from which the gypsum was deposited was highly alkaline suggests that the uranium was leached from volcanic ash in Oligocene time.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6142","usgsCitation":"Dunham, R.J., 1961, Geology of uranium in the Chadron area, Nebraska and South Dakota: U.S. Geological Survey Open-File Report 61-42, viii, 243 p. :ill., maps ;29 cm., https://doi.org/10.3133/ofr6142.","productDescription":"viii, 243 p. :ill., maps ;29 cm.","costCenters":[],"links":[{"id":146083,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1961/0042/report-thumb.jpg"},{"id":41852,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1961/0042/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41853,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1961/0042/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c700","contributors":{"authors":[{"text":"Dunham, Robert Jacob","contributorId":74387,"corporation":false,"usgs":true,"family":"Dunham","given":"Robert","email":"","middleInitial":"Jacob","affiliations":[],"preferred":false,"id":167777,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39780,"text":"pp387A - 1961 - Botanical Evidence of the Modern History of Nisqually Glacier, Washington","interactions":[],"lastModifiedDate":"2012-02-10T00:10:09","indexId":"pp387A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"387","chapter":"A","title":"Botanical Evidence of the Modern History of Nisqually Glacier, Washington","docAbstract":"A knowledge of the areas once occupied by mountain glaciers reveals at least part of the past behavior of these glaciers. From this behavior, inferences of past climate can be drawn. The maximum advance of Nisqually Glacier in the last thousand years was located, and retreat from this point is believed to have started about 1840. The maximum downvalley position of the glacier is marked by either a prominent moraine or by a line of difference between stands of trees of strikingly different size and significantly different age. The thousand-year age of the forest beyond the moraine or line between abutting stands represents the minimum time since the surface was glaciated. This age is based on the age of the oldest trees, plus an estimated interval required for the formation of humus, plus evidence of an ancient fire, plus an interval of deposition of pyroclastics. The estimate of the date when Nisqually Glacier began to retreat from its maximum advance is based upon the ages of the oldest trees plus an interval of 5 years estimated as the time required for the establishment of trees on stable moraines. This interval was derived from a study of the ages of trees growing at locations of known past positions of the glacier.\r\n\r\nReconnaissance studies were made on moraines formed by Emmons and Tahoma Glaciers. Preliminary analyses of these data suggest that Emmons Glacier started to recede from its maximum advance in about 1745. Two other upvalley moraines mark positions from which recession started about 1849 and 1896. Ages of trees near Tahoma Glacier indicate that it started to recede from its position of maximum advance in about 1635. About 1835 Tahoma Glacier started to recede again from another moraine formed by a readvance that ter minated near the 1635 position.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/pp387A","usgsCitation":"Sigafoos, R.S., and Hendricks, E.L., 1961, Botanical Evidence of the Modern History of Nisqually Glacier, Washington: U.S. Geological Survey Professional Paper 387, p. A1-A20, https://doi.org/10.3133/pp387A.","productDescription":"p. A1-A20","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":124576,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0387a/report-thumb.jpg"},{"id":12475,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://www.nps.gov/history/history/online_books/geology/publications/pp/387-a/index.htm","linkFileType":{"id":5,"text":"html"}},{"id":67649,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0387a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -122,46.666666666666664 ], [ -122,47 ], [ -121.25,47 ], [ -121.25,46.666666666666664 ], [ -122,46.666666666666664 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e7276","contributors":{"authors":[{"text":"Sigafoos, Robert S.","contributorId":82379,"corporation":false,"usgs":true,"family":"Sigafoos","given":"Robert","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":222150,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hendricks, E. L.","contributorId":50126,"corporation":false,"usgs":true,"family":"Hendricks","given":"E.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":222149,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"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":"A total-intensity profile was obtained on a 500-mile flight by a U. S. Geological Survey airplane from Anchorage to Nome, Alaska, on May 4, 1954. The average flight altitude was 6,000 ft above sea level except over the Alaska Range where the flight altitude was 9,000 ft. This profile crossed eight of the major tectonic elements of Alaska 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 profile 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 profile 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 profile. The Matanuska geosyncline to the east is represented by a 25-mile section of sloping profile consistent with a thick sedimentary section but indicating that the geosyncline is comparatively narrow near Anchorage. The 200-mile central magnetic segment is relatively free from all but very minor anomalies. This segment includes the Alaska 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 profile 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 profile 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 profile 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 profile 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 profile, 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 Alaska 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.
","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}]}} ]}