The exchange constants and regular solution constants for a number of exchange reactions involving analyzed natural and simulated natural glasses have been determined. The experimental method used provides quick and simple determination of these constants. The calculation of the internal energy differences of model ion exchange systems involving alkali and alkaline earth cations yields sequences (but not magnitudes) of selectivity that agree with the experimental results. Complex glasses such as obsidians, tektites and basaltic glasses do not in general show simple correlations between composition and ion exchange behavior.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr62136","usgsCitation":"Truesdell, A.H., 1962, Study of natural glasses through their behavior as membrane electrodes, Part 2: U.S. Geological Survey Open-File Report 62-136, 43 p., https://doi.org/10.3133/ofr62136.","productDescription":"43 p.","costCenters":[],"links":[{"id":489459,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0136/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":148764,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0136/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699ccc","contributors":{"authors":[{"text":"Truesdell, Alfred Hemingway","contributorId":106137,"corporation":false,"usgs":true,"family":"Truesdell","given":"Alfred","email":"","middleInitial":"Hemingway","affiliations":[],"preferred":false,"id":172585,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2231,"text":"wsp1599 - 1962 - Reconnaissance of ground-water resources in the Western Coal Field Region, Kentucky","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1599","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":"1599","title":"Reconnaissance of ground-water resources in the Western Coal Field Region, Kentucky","docAbstract":"In the Western Coal Field region of Kentucky, water is obtained from consolidated sedimentary rocks of Mississippian and Pennsylvanian ages and from unconsolidated sediments of Cenozoic age. Pennsylvanian rocks crop out in more than 95 percent of the area and consist of shale and sandstone interbedded with some limestone and coal. The Pennsylvanian strata are divided into five formations. They are, in ascending order: the Caseyville sandstone and the Tradewater, Carbondale, Lisman, and Henshaw formations. The Anvil Rock sandstone member of the Lisman formation and the Caseyville sandstone are the only bedrock aquifers in the region that are known to yield more than 100 gpm (gallons per minute) to wells. Most bedrock wells produce enough water for a modern domestic supply, more than 500 gpd (gallons per day), and few yield so little water as to be inadequate for hand pumps and bailers, less than 100 gpd. \r\n\r\nUnconsolidated Cenozoic deposits range from latest Pliocene(?) to Recent in age and consist of clay, silt, sand, and gravel. High gravels, tentatively considered to be late Pliocene and early Pleistacene in age by McFarlan (1950, p. 125), and loess of Pleistocene age are locally exposed, but nearly all of the alluvium is of late Pleistocene and Recent ages. The alluvium along the Ohio River generally yields from a few hundred to as much as 1,000 gpm to single vertical wells and as much as several thousand gallons per minute to wells that have multiple horizontal screens. Alluvium in the tributaries of the Ohio River generally is finer grained than that of the Ohio Valley. The highest known yield from a well in the alluvium of the tributaries is 56 gpm; other wells yield enough for domestic supplies. \r\n\r\nAvailability of ground water in the region depends on the character and thickness of the aquifer penetrated, and, where the aquifer is bedrock on the depth of the water-bearing bed, and to a certain extent on the topographic situation. Most bedrock aquifers in the Western Coal Field region are sandstone and may vary greatly in thickness and composition within short distances. The region is divided into five areas of ground-water availability. Area 1 is confined to the Ohio Valley, most of which is underlain by relatively thick sections of sand and gravel that yield at least 50 gpm to most wells at depths of less than 150 feet. In area 2 most wells yield enough water for a modern domestic supply from depths of less than 300 feet. This area includes the largest part of the bedrock outcrop in the region, some of the alluvial area along the Ohio River, and much of the alluvial areas along the larger tributaries. In area 3 most wells yield enough water from depths of less than 300 feet to supply domestic needs when a hand pump is used. This area covers the bedrock parts of the region that are underlain by shale, sandy shale, and limestone, and the section where few wells are known to yield large supplies of water. In area 4 most wells fail to supply enough water for domestic use from depths of less than 300 feet, probably because they penetrate thick sections of unfractured shale or well-cemented sandstone. In area 5 the yield of wells is unpredictable, commonly because of faulting. \r\n\r\nThe water in the shallow bedrock aquifers of the region is mostly of the sodium bicarbonate or the calcium bicarbonate type. Saline water has been encountered at depths as shallow as 100 feet, but fresh water has been obtained at depths approaching 1,000 feet. Water from the bedrock is soft to moderately hard, but it may contain undesirable amounts of iron. Most water from the alluvium is of the calcium bicarbonate type and is generally harder and contains more iron than water from the bedrock.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1599","usgsCitation":"Maxwell, B.W., and Devaul, R.W., 1962, Reconnaissance of ground-water resources in the Western Coal Field Region, Kentucky: U.S. Geological Survey Water Supply Paper 1599, vi, 34 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1599.","productDescription":"vi, 34 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":137734,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1599/report-thumb.jpg"},{"id":247195,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1599/plate-table_4.pdf","size":"791","linkFileType":{"id":1,"text":"pdf"}},{"id":27985,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1599/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27986,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1599/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27987,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1599/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27988,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1599/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a64e4b07f02db637b34","contributors":{"authors":[{"text":"Maxwell, Bruce William","contributorId":67489,"corporation":false,"usgs":true,"family":"Maxwell","given":"Bruce","email":"","middleInitial":"William","affiliations":[],"preferred":false,"id":144860,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Devaul, Robert Washburn","contributorId":84338,"corporation":false,"usgs":true,"family":"Devaul","given":"Robert","email":"","middleInitial":"Washburn","affiliations":[],"preferred":false,"id":144861,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"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":1767,"text":"wsp1499C - 1962 - Water resources of the Utica-Rome area, New York","interactions":[],"lastModifiedDate":"2021-12-13T21:17:31.346876","indexId":"wsp1499C","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":"1499","chapter":"C","title":"Water resources of the Utica-Rome area, New York","docAbstract":"The Utica-Rome area is along the Mohawk River and New York State Erie (Barge) Canal about midway between Lake Ontario and Albany. It encompasses about 390 square miles centered around the industrial cities of Utica and Rome. The Mohawk River, its tributary West Canada Creek, and a system of reservoirs and diversions to maintain the flow in the barge-canal system, assure an ample water supply for the foreseeable needs of the area. The water from these sources is generally of good chemical quality requiring little treatment, although that from the Mohawk River is only fair and may require some treatment for sensitive industrial processes. Additional surface water is available from smaller streams in the area, particularly Oriskany and Sauquoit Creeks, but the water from these sources is hard, and has a dissolved-solids content of more than 250 ppm (parts per million). Ground water is available in moderate quantities from unconsolidated sand and gravel deposits in the river valleys and buried bedrock channels, and in small quantities from bedrock formations and less permeable unconsolidated deposits. The quality of water from sand and gravel, and bedrock ranges from good to poor. However, where necessary, the quality can be improved with treatment. \r\n\r\nThe Mohawk River is the source of the largest quantity of water in the area. The flow of the stream below Delta Dam equals or exceeds 108 mgd (million gallons per day) 90 percent of the time, and at Little Falls it equals or exceeds 560 mgd 90 percent of the time. The flow between these two points is increased by additions from Oriskany, Sauquoit, and West Canada Creeks and from many smaller tributary streams. The flow is also increased by diversions from outside the area, from the Black and Chenango Rivers and West Canada Creek for improvement of navigation in the Erie (Barge) Canal, and from West Canada and East Branch Fish Creeks for the public supplies of Utica and Rome. Much of the public-supply water eventually reaches the river by way of sewerage and industrial waste-disposal systems. The total diversion from these sources averages more than 92 mgd. An estimated 18.5 mgd is withdrawn from the Mohawk River by industry, mostly for nonconsumptive uses. \r\n\r\nFloods in the Utica-Rome area are not a frequent problem owing to the use of regulatory measures. The major streams fluctuate through a narrow range in stage and generally only a narrow strip along the streams is subject to flooding. Water-bearing sand and gravel deposits in the major river valleys are the principal sources of ground water, especially where they are recharged by infiltration from streams. The most important potential source is the deposit of sand and gravel underlying the extensive plain adjacent to the Mohawk River between Delta Reservoir and Rome. Maximum sustained yields from these deposits are not known; but moderate quantities of water, 300 gpm (gallons per minute) or less from a single well, can probably be obtained from some parts of the sand plain area, particularly in the vicinity of a buried bedrock channel that extends southwestward from Delta Reservoir. Similar quantities of ground water probably can be withdrawn from some parts of the flood plain of the Mohawk River between Rome and Frankfort and from the sand and gravel deposits filling the valley of Ninemile Creek below Holland Patent. The deposits underlying the flood plain of the Mohawk River generally are fine grained but in places contain interstratified beds of coarser sand and gravel. The most productive part of the flood plain is at the east end near Frankfort. The deposits in Ninemile Creek valley also are generally fine grained; but where they are sufficiently thick, as over a buried bedrock valley southwest of Floyd, moderate quantities of water may be obtained. \r\n\r\nSmall to moderate quantities of water (150 gpm or less from a single well) can be obtained from sand and gravel deposits in the bottoms of Oriskany and Sauquoit Creek vall","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1499C","usgsCitation":"Halberg, H., Hunt, O.P., and Pauszek, F.H., 1962, Water resources of the Utica-Rome area, New York: U.S. Geological Survey Water Supply Paper 1499, Report: iv, 46 p.; 3 Plates: 21.00 × 17.15 inches or smaller, https://doi.org/10.3133/wsp1499C.","productDescription":"Report: iv, 46 p.; 3 Plates: 21.00 × 17.15 inches or smaller","costCenters":[],"links":[{"id":26891,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499c/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26890,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499c/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26889,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137141,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499c/report-thumb.jpg"},{"id":26892,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":392829,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24439.htm"}],"country":"United States","state":"New York","city":"Rome, Utica","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.59417724609375,\n 43.018705515824635\n ],\n [\n -75.10528564453125,\n 43.018705515824635\n ],\n [\n -75.10528564453125,\n 43.29120116988416\n ],\n [\n -75.59417724609375,\n 43.29120116988416\n ],\n [\n -75.59417724609375,\n 43.018705515824635\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dfe4b07f02db5e3376","contributors":{"authors":[{"text":"Halberg, Henry N.","contributorId":19929,"corporation":false,"usgs":true,"family":"Halberg","given":"Henry N.","affiliations":[],"preferred":false,"id":144113,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hunt, O. P.","contributorId":69116,"corporation":false,"usgs":true,"family":"Hunt","given":"O.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":144115,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pauszek, F. H.","contributorId":61399,"corporation":false,"usgs":true,"family":"Pauszek","given":"F.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144114,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1333,"text":"wsp1536E - 1962 - Theory of aquifer tests","interactions":[],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1536E","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":"1536","chapter":"E","title":"Theory of aquifer tests","docAbstract":"The development of water supplies from wells was placed on a rational basis with Darcy's development of the law governing the movement of fluids through sands and with Dupuit's application of that law to the problem of radial flow toward a pumped well. As field experience increased, confidence in the applicability of quantitative methods was gained and interest in developing solutions for more complex hydrologic problems was stimulated. An important milestone was Theis' development in 1935 of a solution for the nonsteady flow of ground water, which enabled hydrologists for the first time to predict future changes in ground-water levels resulting from pumping or recharging of wells. In the quarter century since, quantitative ground-water hydrology has been enlarging so rapidly as to discourage the preparation of comprehensive textbooks. \r\n\r\nThis report surveys developments in fluid mechanics that apply to groundwater hydrology. It emphasizes concepts and principles, and the delineation of limits of applicability of mathematical models for analysis of flow systems in the field. It stresses the importance of the geologic variable and its role in governing the flow regimen. \r\n\r\nThe report discusses the origin, occurrence, and motion of underground water in relation to the development of terminology and analytic expressions for selected flow systems. It describes the underlying assumptions necessary for mathematical treatment of these flow systems, with particular reference to the way in which the assumptions limit the validity of the treatment.","language":"ENGLISH","publisher":"U.S. Government Print. Office,","doi":"10.3133/wsp1536E","usgsCitation":"Ferris, J., Knowles, D., Brown, R.H., and Stallman, R., 1962, Theory of aquifer tests: U.S. Geological Survey Water Supply Paper 1536, vii, 105 p. :ill. ;24 cm., https://doi.org/10.3133/wsp1536E.","productDescription":"vii, 105 p. :ill. ;24 cm.","costCenters":[],"links":[{"id":12,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wsp1536-E","linkFileType":{"id":5,"text":"html"}},{"id":137382,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0de4b07f02db5fd475","contributors":{"authors":[{"text":"Ferris, J.G.","contributorId":12453,"corporation":false,"usgs":true,"family":"Ferris","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":143577,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Knowles, D.B.","contributorId":83898,"corporation":false,"usgs":true,"family":"Knowles","given":"D.B.","email":"","affiliations":[],"preferred":false,"id":143580,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brown, R. H.","contributorId":19931,"corporation":false,"usgs":false,"family":"Brown","given":"R.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143578,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Stallman, R.H.","contributorId":55800,"corporation":false,"usgs":true,"family":"Stallman","given":"R.H.","email":"","affiliations":[],"preferred":false,"id":143579,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":2605,"text":"wsp1536F - 1962 - A formula for computing transmissibility causing maximum possible drawdown due to pumping","interactions":[],"lastModifiedDate":"2012-02-02T00:05:27","indexId":"wsp1536F","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":"1536","chapter":"F","title":"A formula for computing transmissibility causing maximum possible drawdown due to pumping","docAbstract":"By modifying the Theis nonequilibrium formula a relation is found in which the maximum possible drawdown is expressed in terms of a unique value for the aquifer coefficient of transmissibility. The relation is valid for any specified period and rate of pumping, for a given aquifer coefficient of storage, and for ,any desired radial distance from the center of pumping.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1536F","usgsCitation":"Robinson, G., and Skibitzke, H.E., 1962, A formula for computing transmissibility causing maximum possible drawdown due to pumping: U.S. Geological Survey Water Supply Paper 1536, p. 175-180 :ill. ;24 cm., https://doi.org/10.3133/wsp1536F.","productDescription":"p. 175-180 :ill. ;24 cm.","costCenters":[],"links":[{"id":138704,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1536f/report-thumb.jpg"},{"id":28888,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1536f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6ae57b","contributors":{"authors":[{"text":"Robinson, G.M.","contributorId":68710,"corporation":false,"usgs":true,"family":"Robinson","given":"G.M.","email":"","affiliations":[],"preferred":false,"id":145483,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Skibitzke, Herbert E.","contributorId":32142,"corporation":false,"usgs":true,"family":"Skibitzke","given":"Herbert","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":145482,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":61965,"text":"mr23 - 1962 - Manganese in the United States, exclusive of Alaska and Hawaii","interactions":[{"subject":{"id":46031,"text":"ofr6139 - 1961 - Manganese in the United States","indexId":"ofr6139","publicationYear":"1961","noYear":false,"title":"Manganese in the United States"},"predicate":"SUPERSEDED_BY","object":{"id":61965,"text":"mr23 - 1962 - Manganese in the United States, exclusive of Alaska and Hawaii","indexId":"mr23","publicationYear":"1962","noYear":false,"title":"Manganese in the United States, exclusive of Alaska and Hawaii"},"id":1}],"lastModifiedDate":"2025-05-22T17:03:19.184597","indexId":"mr23","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":"23","title":"Manganese in the United States, exclusive of Alaska and Hawaii","docAbstract":"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":52271,"text":"ofr62107 - 1962 - Hydraulic model studies--stream gaging control structure for Carrizo-Corduroy Project, Arizona","interactions":[],"lastModifiedDate":"2013-08-01T15:16:00","indexId":"ofr62107","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"62-107","title":"Hydraulic model studies--stream gaging control structure for Carrizo-Corduroy Project, Arizona","language":"ENGLISH","doi":"10.3133/ofr62107","usgsCitation":"Richardson, E., 1962, Hydraulic model studies--stream gaging control structure for Carrizo-Corduroy Project, Arizona: U.S. Geological Survey Open-File Report 62-107, 42 p., https://doi.org/10.3133/ofr62107.","productDescription":"42 p.","costCenters":[],"links":[{"id":179396,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0107/report-thumb.jpg"},{"id":275860,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0107/report.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db62a1f4","contributors":{"authors":[{"text":"Richardson, E.V.","contributorId":105697,"corporation":false,"usgs":true,"family":"Richardson","given":"E.V.","email":"","affiliations":[],"preferred":false,"id":245066,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":52276,"text":"ofr62115 - 1962 - Geology of the Williston basin, North Dakota, Montana, and South Dakota, with reference to subsurface disposal of radioactive wastes","interactions":[],"lastModifiedDate":"2012-02-02T00:11:20","indexId":"ofr62115","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"62-115","title":"Geology of the Williston basin, North Dakota, Montana, and South Dakota, with reference to subsurface disposal of radioactive wastes","docAbstract":"The southern Williston basin, which underlies about 110,000 square miles #n North Dakota, South Dakota, and eastern Montana, is part of a large structural and sedimentary basin. Its surface is a flat to gently rolling plain, standing about 1,500 to 3,500 feet above sea level and locally studded by a few high buttes. The sedimentary sequence that fills the basin has a maximum thickness of about 16,700 feet and rests on Precambrian metamorphic rocks at depths of 500 to 13,900 feet below sea level. It contains rocks of every geologic system, from Cambrian to Quaternary. Rocks of Middle Cambrian through Middle Ordovician age are largely shale and sandstone, as much as 1,200 feet thick; rocks of Late Ordovician through Pennsylvanian age are largely limestone and dolomite, as much as 7,500 feet thick; and rocks of Permian through Tertiary age are predominantly shale and siltstone, as much as 8,000 feet thick. Pleistocene glacial drift mantles the northern and eastern parts of the area. Rocks of the Williston basin are gently folded and regional dips are 1? or less from the margins to the basin center. Dips on the flanks of the major anticlinal folds, the Nesson and cedar Creek anticlines and the Poplar and Bowdoin domes, generally are about 1? to 3? except on the steep west limb of the Cedar Creek anticline. The basin was shaped by Laramide orogeny during latest Cretaceous and early Tertiary time. Most of the present structural features, however, were initiated during the Precambrian and reactivated by several subsequent orogenies, of which the latest was the Laramide. The most important mineral resource of the area is oil, which is produced predominantly from the Paleozoic carbonate sequence and largely on three of the major anticlinal folds, and lignite, which is present near the surface in Paleocene rocks. \r\n\r\nThe subsurface disposal of radioactive wastes at some places in the Williston basin appears to be geographically and geologically feasible. Many sites, at which large quantities of wastes might be injected with minimal danger of contamination of fresh-water aquifers and-oil-producing strata, are available.. The strata and types of reservoirs that deserve primary consideration for waste disposal are the Winnipeg Formation of Middle Ordovician age as a deep salaquifer, the Permian to Jurassic salt beds as moderately deep-units in which solution cavities might be created for storage, the thick Upper Cretaceous shale beds as shallow hydraulically fractured shale reservoirs, and the Newcastle Sandstone of Early Cretaceous age as a shallow shale-enclosed sandstone reservoir.","language":"ENGLISH","doi":"10.3133/ofr62115","usgsCitation":"Sandberg, C.A., 1962, Geology of the Williston basin, North Dakota, Montana, and South Dakota, with reference to subsurface disposal of radioactive wastes: U.S. Geological Survey Open-File Report 62-115, 148 p., https://doi.org/10.3133/ofr62115.","productDescription":"148 p.","costCenters":[],"links":[{"id":179401,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0115/report-thumb.jpg"},{"id":86779,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0115/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86780,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0115/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86781,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0115/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86782,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0115/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c950","contributors":{"authors":[{"text":"Sandberg, C. A.","contributorId":86016,"corporation":false,"usgs":true,"family":"Sandberg","given":"C.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":245071,"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":32761,"text":"pp417A - 1962 - Relation between ground water and surface water in Brandywine Creek basin, Pennsylvania","interactions":[],"lastModifiedDate":"2017-06-20T09:58:32","indexId":"pp417A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"417","chapter":"A","title":"Relation between ground water and surface water in Brandywine Creek basin, Pennsylvania","docAbstract":"The relation between ground water and surface water was studied in Brandywine Creek basin, an area of 287 square miles in the Piedmont physiographic province in southeastern Pennsylvania. Most of the basin is underlain by crystalline rocks that yield only small to moderate supplies of water to wells, but the creek has an unusually well-sustained base flow. Streamflow records for the Chadds Ford, Pa., gaging station were analyzed; base flow recession curves and hydrographs of base flow were defined for the calendar years 1928-31 and 1952-53. Water budgets calculated for these two periods indicate that about two-thirds of the runoff of Brandywine Creek is base flow--a significantly higher proportion of base flow than in streams draining most other types of consolidated rocks in the region and almost as high as in streams in sandy parts of the Coastal Plain province in New Jersey and Delaware.\r\n\r\n Ground-water levels in 16 observation wells were compared with the base flow of the creek for 1952-53. The wells are assumed to provide a reasonably good sample of average fluctuations of the water table and its depth below the land surface.\r\n\r\n Three of the wells having the most suitable records were selected as index wells to use in a more detailed analysis. A direct, linear relation between the monthly average ground-water stage in the index wells and the base flow of the creek in winter months was found.\r\n\r\n The average ground-water discharge in the basin for 1952-53 was 489 cfs (316 mgd), of which slightly less than one-fourth was estimated to be loss by evapotranspiration. However, the estimated evapotranspiration from ground water, and consequently the estimated total ground-water discharge, may be somewhat high.\r\n\r\n The average gravity yield (short-term coefficient of storage) of the zone of water-table fluctuation was calculated by two methods. The first method, based on the ratio of change in ground-water storage as calculated from a witner base-flow recession curve is seasonal change in ground-water stage in the observation wells, gave values of about 7 percent using 16 wells) and 7 1/2 percent (using 3 index wells). The second method, in which the change in ground water storage is based on a hypothetical base-flow recession curve (derived from the observed linear relation between ground-water stage in the index wells and base flow), gave a value of about 10 1/2 percent. The most probable value of gravity yield is between 7 1/2 and 10 percent, but this estimate may require modification when more information on the average magnitude of water-table fluctuation and the sources of base flow of the creek become available.\r\n\r\n Rough estimates were made of the average coefficient of transmissibility of the rocks in the basin by use of the estimated total ground-water discharge for the period 1952-53, approximate values of length of discharge areas, and average water-table gradients adjacent to the discharge areas. The estimated average coefficient of transmissibility for 1952-53 is roughly 1,000 gpd per foot. The transmissibility is variable, decreasing with decreasing ground-water stage.\r\n\r\n The seeming inconsistency between the small to moderate ground-water yield to wells and the high yield to streams is explained in terms of the deep permeable soils, the relatively high gravity yield of the zone of water-table fluctuation, the steep water-table gradients toward the streams, the relatively low transmissibility of the rocks, and the rapid decreases in gravity yield below the lower limit of water-table fluctuation. It is concluded that no simple relation exists between the amount of natural ground-water discharge in an area and all the proportion of this discharge that can be diverted to wells.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp417A","usgsCitation":"Olmsted, F.H., and Hely, A., 1962, Relation between ground water and surface water in Brandywine Creek basin, Pennsylvania: U.S. Geological Survey Professional Paper 417, p. A1-A21, https://doi.org/10.3133/pp417A.","productDescription":"p. A1-A21","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":124990,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0417a/report-thumb.jpg"},{"id":60694,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0417a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c32c","contributors":{"authors":[{"text":"Olmsted, F. H.","contributorId":24765,"corporation":false,"usgs":true,"family":"Olmsted","given":"F.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":209114,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hely, A. G.","contributorId":14401,"corporation":false,"usgs":true,"family":"Hely","given":"A. G.","affiliations":[],"preferred":false,"id":209113,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":38877,"text":"pp500A - 1962 - The concept of entropy in landscape evolution","interactions":[],"lastModifiedDate":"2017-03-24T14:29:26","indexId":"pp500A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"500","chapter":"A","title":"The concept of entropy in landscape evolution","docAbstract":"The concept of entropy is expressed in terms of probability of various states. Entropy treats of the distribution of energy. The principle is introduced that the most probable condition exists when energy in a river system is as uniformly distributed as may be permitted by physical constraints. From these general considerations equations for the longitudinal profiles of rivers are derived that are mathematically comparable to those observed in the field. The most probable river profiles approach the condition in which the downstream rate of production of entropy per unit mass is constant.
Hydraulic equations are insufficient to determine the velocity, depths, and slopes of rivers that are themselves authors of their own hydraulic geometries. A solution becomes possible by introducing the concept that the distribution of energy tends toward the most probable. This solution leads to a theoretical definition of the hydraulic geometry of river channels that agrees closely with field observations.
The most probable state for certain physical systems can also be illustrated by random-walk models. Average longitudinal profiles and drainage networks were so derived and these have the properties implied by the theory. The drainage networks derived from random walks have some of the principal properties demonstrated by the Horton analysis; specifically, the logarithms of stream length and stream numbers are proportional to stream order.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Theoretical papers in the hydrologic and geomorphic sciences (Professional Paper 500)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp500A","usgsCitation":"Leopold, L.B., and Langbein, W.B., 1962, The concept of entropy in landscape evolution: U.S. Geological Survey Professional Paper 500, iii, 21 p., https://doi.org/10.3133/pp500A.","productDescription":"iii, 21 p.","startPage":"A1","endPage":"A20","numberOfPages":"26","costCenters":[],"links":[{"id":120295,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0500a/report-thumb.jpg"},{"id":65878,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0500a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668a4c","contributors":{"authors":[{"text":"Leopold, Luna Bergere","contributorId":93884,"corporation":false,"usgs":true,"family":"Leopold","given":"Luna","email":"","middleInitial":"Bergere","affiliations":[],"preferred":false,"id":220592,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Langbein, Walter Basil","contributorId":40581,"corporation":false,"usgs":true,"family":"Langbein","given":"Walter","email":"","middleInitial":"Basil","affiliations":[],"preferred":false,"id":220593,"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":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. 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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}]}} ]}