Water is a fundamental geologic agent active in rock decomposition, erosion, and synthesis. Solutes in water are of particular interest to geochemists as sources of raw material for synthesis or as products of decomposition. When geochemical studies move from the laboratory into natural environment many variables relating to solute hydrology must be considered.
As a focal point there has been designed a graphical representation of solute hydrology, the solusphere, which embodies the concepts of land-water occurrence and movement on which are superimposed geologic, biologic, physical, chemical, and cultural processes affecting solutes. The solusphere is demonstrated by passing an imaginary plane through the centre of the earth. This plane intercepts concentric zones designated as rock flowage, saturation, aeration, surface activity, and atmosphere. Transport processes carry solutes within and between zones without alteration or conversion. However, whether stationary or in motion, the water's solute character is constantly subject to (1) alteration processes that change concentration by addition or subtraction of solutes or solvent without loss of solute identities, and (2) conversion processes that change the chemical state and form of solutes.
The geochemist is concerned with specific conversion processes, but he also must consider transport, alteration, and other conversion processes that are continually modifying the materials with which he is dealing in nature. The solusphere is an attempt to organize processes affecting the chemical quality of land waters into a unified field of science much like the field of marine chemistry.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(58)90083-8","usgsCitation":"Rainwater, F.H., and White, W.F., 1958, The solusphere - its inferences and study: Geochimica et Cosmochimica Acta, v. 14, no. 3, p. 244-249, https://doi.org/10.1016/0016-7037(58)90083-8.","productDescription":"6 p.","startPage":"244","endPage":"249","costCenters":[{"id":629,"text":"Water Resources Division","active":false,"usgs":true}],"links":[{"id":218830,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"14","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb045e4b08c986b324d4f","contributors":{"authors":[{"text":"Rainwater, F. H.","contributorId":41402,"corporation":false,"usgs":true,"family":"Rainwater","given":"F.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":357273,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"White, W. F.","contributorId":80259,"corporation":false,"usgs":true,"family":"White","given":"W.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":357274,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70211918,"text":"70211918 - 1958 - Reconnaissance study of erosion and deposition produced by the flood of August 1955 in Connecticut","interactions":[],"lastModifiedDate":"2020-08-11T19:16:55.176465","indexId":"70211918","displayToPublicDate":"1958-08-11T14:08:12","publicationYear":"1958","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"Reconnaissance study of erosion and deposition produced by the flood of August 1955 in Connecticut","docAbstract":"A large area in the valley bottoms in Connecticut was inundated by the flood of August 1955. Relative to the total area flooded that part permanently modified by the flow was surprisingly small. Although great in some places, the distribution of these permanent modifications of channel and flood plain was spotty. Erosion of the channel and valley bottom appears to have been most severe in narrow, steep valleys. Environments of deposition were diverse. They appeared to be related to rate and direction of flow, quantity and size of sediments locally available, and in some cases to the presence of vegetation. Most of the coarse sediment deposited in the valley appears to have been derived from local sources such as valley walls and terraces composed of glacial outwash and till and flood plains containing considerable gravel. Fine sand predominated in most of the sediment deposited. Considering the magnitude of the runoff, the quantity of fine sediment transported or deposited by the flood was small. The maximum observed concentration was 473 parts per million in Scantic River at Broad Brook. Newly deposited fine sediments are thin or absent on the flood plains of many valleys which were beneath 20 ft of slow‐moving flood waters. The paucity of deposition in such ideal depositional environments also indicates that the flow did not have a high concentration of fine sediments. A number of boulders five to seven feet in diameter were moved by flood waters in reaches in which smaller gravels were undisturbed. Severe erosion in the uplands was minor. In this reconnaissance we saw little evidence of newly formed gullies and no areas of severe sheet erosion. This was the case in both woodland and pasture land. Large amounts of subsurface flow and relatively unerodible ground are presumed to be responsible for the absence of erosion.
","language":"English","publisher":"Wiley","doi":"10.1029/TR039i001p00001","usgsCitation":"Wolman, M.G., and Eiler, J., 1958, Reconnaissance study of erosion and deposition produced by the flood of August 1955 in Connecticut: Eos, Transactions, American Geophysical Union, v. 39, no. 1, p. 1-14, https://doi.org/10.1029/TR039i001p00001.","productDescription":"14 p.","startPage":"1","endPage":"14","costCenters":[],"links":[{"id":377372,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Connecticut","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-71.799242,42.008065],[-71.797922,41.935395],[-71.797649,41.928556],[-71.794161,41.841101],[-71.794161,41.840141],[-71.792786,41.80867],[-71.792767,41.807001],[-71.791062,41.770273],[-71.789678,41.724734],[-71.789672,41.724569],[-71.786994,41.655992],[-71.787637,41.639917],[-71.789356,41.59691],[-71.789359,41.596852],[-71.797683,41.416709],[-71.81839,41.419599],[-71.839649,41.412119],[-71.842563,41.409855],[-71.843472,41.40583],[-71.842131,41.395359],[-71.833443,41.384524],[-71.831613,41.370899],[-71.837738,41.363529],[-71.835951,41.353935],[-71.829595,41.344544],[-71.839013,41.334042],[-71.860513,41.320248],[-71.859566,41.3224],[-71.868235,41.330941],[-71.886302,41.33641],[-71.91671,41.332217],[-71.922092,41.334518],[-71.923282,41.335113],[-71.936284,41.337959],[-71.945652,41.337799],[-71.956747,41.329871],[-71.970955,41.324526],[-71.979447,41.329987],[-71.982194,41.329861],[-71.988153,41.320577],[-72.021898,41.316838],[-72.084487,41.319634],[-72.094443,41.314164],[-72.09982,41.306998],[-72.11182,41.299098],[-72.134221,41.299398],[-72.16158,41.310262],[-72.173922,41.317597],[-72.177622,41.322497],[-72.184122,41.323997],[-72.191022,41.323197],[-72.201422,41.315697],[-72.203022,41.313197],[-72.204022,41.299097],[-72.212924,41.291365],[-72.225276,41.299047],[-72.235531,41.300413],[-72.248161,41.299488],[-72.251895,41.29862],[-72.250515,41.294386],[-72.251323,41.289997],[-72.261487,41.282926],[-72.31776,41.277782],[-72.327595,41.27846],[-72.333894,41.282916],[-72.34146,41.28011],[-72.348643,41.277446],[-72.348068,41.269698],[-72.386629,41.261798],[-72.398688,41.278172],[-72.40593,41.278398],[-72.451925,41.278885],[-72.472539,41.270103],[-72.485693,41.270881],[-72.499534,41.265866],[-72.506634,41.260099],[-72.51866,41.261253],[-72.521312,41.2656],[-72.529416,41.264421],[-72.533247,41.26269],[-72.536746,41.256207],[-72.537776,41.255646],[-72.546833,41.250718],[-72.547235,41.250499],[-72.570655,41.267744],[-72.571076,41.268054],[-72.571136,41.268098],[-72.583336,41.271698],[-72.585181,41.271321],[-72.585934,41.271168],[-72.586674,41.271017],[-72.587926,41.270761],[-72.589818,41.270375],[-72.590967,41.270141],[-72.598036,41.268698],[-72.607863,41.270387],[-72.610236,41.270795],[-72.617237,41.271998],[-72.617521,41.27194],[-72.617983,41.271845],[-72.631363,41.269092],[-72.641001,41.267108],[-72.641538,41.266998],[-72.642811,41.266884],[-72.650697,41.266178],[-72.653838,41.265897],[-72.653931,41.265931],[-72.654715,41.266219],[-72.662203,41.268964],[-72.662838,41.269197],[-72.667176,41.268192],[-72.671673,41.267151],[-72.672339,41.266997],[-72.674319,41.26552],[-72.684939,41.257597],[-72.685414,41.252607],[-72.685539,41.251297],[-72.689446,41.247629],[-72.690237,41.246887],[-72.690439,41.246697],[-72.693441,41.245493],[-72.694744,41.24497],[-72.69547,41.244948],[-72.701806,41.244752],[-72.706236,41.244615],[-72.707212,41.244585],[-72.708658,41.24454],[-72.708963,41.24453],[-72.709193,41.244523],[-72.710595,41.24448],[-72.710821,41.244812],[-72.713674,41.249007],[-72.711208,41.251018],[-72.71246,41.254167],[-72.722439,41.259138],[-72.732813,41.254727],[-72.754444,41.266913],[-72.757477,41.266913],[-72.786142,41.264796],[-72.818737,41.252244],[-72.819372,41.254061],[-72.826883,41.256755],[-72.847767,41.25669],[-72.85021,41.255544],[-72.854055,41.24774],[-72.861344,41.245297],[-72.881445,41.242597],[-72.895445,41.243697],[-72.900803,41.245864],[-72.904345,41.247297],[-72.905245,41.248297],[-72.903045,41.252797],[-72.902808,41.252894],[-72.894745,41.256197],[-72.89473,41.25626],[-72.893845,41.259897],[-72.89637,41.263949],[-72.903129,41.274794],[-72.907962,41.282549],[-72.9082,41.282932],[-72.916827,41.282033],[-72.917037,41.281905],[-72.920062,41.280056],[-72.920658,41.271574],[-72.920714,41.27078],[-72.920846,41.268897],[-72.931887,41.261139],[-72.933472,41.260024],[-72.935646,41.258497],[-72.956984,41.25292],[-72.959633,41.252228],[-72.961345,41.25178],[-72.962047,41.251597],[-72.983751,41.235364],[-72.985095,41.234358],[-72.986247,41.233497],[-72.997948,41.222697],[-73.003639,41.215287],[-73.007548,41.210197],[-73.013465,41.205479],[-73.013988,41.205062],[-73.014948,41.204297],[-73.020149,41.204097],[-73.020167,41.204237],[-73.020195,41.204446],[-73.02021,41.204568],[-73.020254,41.204906],[-73.020449,41.206397],[-73.022549,41.207197],[-73.024783,41.207435],[-73.045602,41.209658],[-73.05065,41.210197],[-73.054947,41.208468],[-73.05935,41.206697],[-73.07761,41.195176],[-73.07945,41.194015],[-73.09122,41.184153],[-73.092,41.1835],[-73.092147,41.183377],[-73.104328,41.17317],[-73.105483,41.172203],[-73.105493,41.172194],[-73.107987,41.168738],[-73.110352,41.159697],[-73.109952,41.156997],[-73.108352,41.153718],[-73.111052,41.150797],[-73.130253,41.146797],[-73.16437,41.158565],[-73.170074,41.160532],[-73.170701,41.164945],[-73.177774,41.166697],[-73.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\"}}]}","volume":"39","issue":"1","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Wolman, M. Gordon","contributorId":85163,"corporation":false,"usgs":true,"family":"Wolman","given":"M.","email":"","middleInitial":"Gordon","affiliations":[],"preferred":false,"id":795803,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Eiler, J.P.","contributorId":238011,"corporation":false,"usgs":false,"family":"Eiler","given":"J.P.","email":"","affiliations":[],"preferred":false,"id":795804,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5221316,"text":"5221316 - 1958 - Mass control of insects: The effects on fish and wildlife","interactions":[],"lastModifiedDate":"2023-08-30T16:28:53.825439","indexId":"5221316","displayToPublicDate":"1958-06-16T12:18:25","publicationYear":"1958","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1122,"text":"Bulletin of the Entomological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Mass control of insects: The effects on fish and wildlife","docAbstract":"The mass control of insects carried on during the past ten years has made possible the economical suppression and, in a few instances, the near eradication of pest insect populations over widespread areas. These large operations, usually featuring the use of the airplane for applying insecticides quickly and cheaply, have proven to be the means of effectuating control programs which never could have been carried on through use of the techniques and equipment of early-day economic entomology. With the development of the methods employed in modern mass control came the introduction of new toxicants, well-adapted for use against insects because of their potency, low cost and wide availability. The present-day entomologist is thus armed with the means to carry on a control task of almost any magnitude.
","language":"English","publisher":"Oxford Academic","doi":"10.1093/besa/4.2.52","usgsCitation":"Cope, O.B., and Springer, P.F., 1958, Mass control of insects: The effects on fish and wildlife: Bulletin of the Entomological Society of America, v. 4, no. 2, p. 52-56, https://doi.org/10.1093/besa/4.2.52.","productDescription":"5 p.","startPage":"52","endPage":"56","numberOfPages":"5","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":196945,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"4","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a19e4b07f02db605a48","contributors":{"authors":[{"text":"Cope, Oliver B.","contributorId":13290,"corporation":false,"usgs":true,"family":"Cope","given":"Oliver","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":333546,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Springer, Paul F.","contributorId":70445,"corporation":false,"usgs":true,"family":"Springer","given":"Paul","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":333547,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010541,"text":"70010541 - 1958 - A combined deamination and nitro reduction method for nitroanilines","interactions":[],"lastModifiedDate":"2013-02-23T22:06:00","indexId":"70010541","displayToPublicDate":"1958-01-01T00:00:00","publicationYear":"1958","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2408,"text":"Journal of Organic Chemistry","active":true,"publicationSubtype":{"id":10}},"title":"A combined deamination and nitro reduction method for nitroanilines","docAbstract":"The hypophosphorous acid-cuprous oxide deamination method on nitroanilines has been modified so that the nitro compounds which are formed are reduced in turn by cuprous oxide to the corresponding amines. Over-all yields of 55-65% are reported for three halogenated nitroanilines.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Journal of Organic Chemistry","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"American Chemical Society","doi":"10.1021/jo01105a006","issn":"00223263","usgsCitation":"Finger, G.C., and White, R., 1958, A combined deamination and nitro reduction method for nitroanilines: Journal of Organic Chemistry, v. 23, no. 11, p. 1612-1613, https://doi.org/10.1021/jo01105a006.","startPage":"1612","endPage":"1613","numberOfPages":"2","costCenters":[],"links":[{"id":268069,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1021/jo01105a006"},{"id":219765,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"23","issue":"11","noUsgsAuthors":false,"publicationDate":"2002-05-01","publicationStatus":"PW","scienceBaseUri":"5059e34be4b0c8380cd45f47","contributors":{"authors":[{"text":"Finger, G. C.","contributorId":89277,"corporation":false,"usgs":true,"family":"Finger","given":"G.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":359137,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"White, R.H.","contributorId":83263,"corporation":false,"usgs":true,"family":"White","given":"R.H.","email":"","affiliations":[],"preferred":false,"id":359136,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010560,"text":"70010560 - 1958 - The deuterium content of water in some volcanic glasses","interactions":[],"lastModifiedDate":"2020-11-12T20:58:57.939243","indexId":"70010560","displayToPublicDate":"1958-01-01T00:00:00","publicationYear":"1958","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"The deuterium content of water in some volcanic glasses","docAbstract":"The deuterium-hydrogen composition (relative to Lake Michigan water = 0.0) of water extractsd from coexisting perlite and obsidian from eleven different localities was determined. The water content of the obsidians is generally from 0.09 to 0.29 per cent by weight, though two samples from near Olancha, California, contain about 0.92 per cent. The relative deuterium concentration is from −4.6 to −12.3 per cent. The coexisting perlite contains from 2.0 to 3.8 per cent of water with a relative deuterium concentration of −3.1 to −16.6 per cent. The deuterium concentration in the perlites is not related to that in the enclosed obsidian. The deuterium concentration in the perlite water is related to the deuterium concentration of the modern meteoric water and the perlite water contains approximately 4 per cent less deuterium than does the groundwater of the area in which the perlites occur. The above relations hold true for perlites from northern New Mexico, east slope of the Sierra Nevada. California Coast Range, Yellowstone Park, Wyoming, and New Zealand. As the water in the obsidian is unrelated to meteoric water, but the enclosing perlite water is related, we believe that this is evidence for the secondary hydration of obsidian to form high water content perlitic glass.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(58)90059-0","usgsCitation":"Friedman, I., and Smith, R.L., 1958, The deuterium content of water in some volcanic glasses: Geochimica et Cosmochimica Acta, v. 15, no. 3, p. 218-228, https://doi.org/10.1016/0016-7037(58)90059-0.","productDescription":"12 p.","startPage":"218","endPage":"228","costCenters":[],"links":[{"id":219080,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"15","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505baaa3e4b08c986b3228e7","contributors":{"authors":[{"text":"Friedman, I.","contributorId":95596,"corporation":false,"usgs":true,"family":"Friedman","given":"I.","email":"","affiliations":[],"preferred":false,"id":359172,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Smith, R. L.","contributorId":93904,"corporation":false,"usgs":true,"family":"Smith","given":"R.","email":"","middleInitial":"L.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":359171,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010795,"text":"70010795 - 1958 - Volumes and surface areas of pendular rings","interactions":[],"lastModifiedDate":"2020-11-12T21:34:20.62453","indexId":"70010795","displayToPublicDate":"1958-01-01T00:00:00","publicationYear":"1958","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2171,"text":"Journal of Applied Physics","active":true,"publicationSubtype":{"id":10}},"title":"Volumes and surface areas of pendular rings","docAbstract":"The adult form of Triaenophorus crassus Forel, 1868 (= T. robustus Olsson, 1893; = T. tricuspidatus morpha megadentatus Wardle, 1932) occurs as an intestinal parasite in the pike, Esox lucius L., a holarctic species of wide distribution. Preliminary life-history stages include procercoid development in copepods of the genus Cyclops followed by plerocercoid development in the musculature of a variety of coregonid and salmonid fishes. The unsightly appearance of even moderate plerocercoid infections is often sufficient to render fish unacceptable for human consumption. In the prairie provinces of Canada the incidence and intensity of T. crassus infections in the commercially important whitefishes constitute a serious economic problem.
","language":"English","publisher":"American Society of Parasitologists","publisherLocation":"Lawrence, KS","doi":"10.2307/3274650","usgsCitation":"Uzmann, J., and Hesselholt, M.N., 1957, New host and locality record for Triaenophorus crassus forel (Cestoda: pseudophyllidea): Journal of Parasitology, v. 43, no. 2, p. 205-208, https://doi.org/10.2307/3274650.","productDescription":"4 p.","startPage":"205","endPage":"208","numberOfPages":"4","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":654,"text":"Western Fisheries Research Center","active":true,"usgs":true}],"links":[{"id":489028,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.2307/3274650","text":"Publisher Index Page"},{"id":312715,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada, United States","state":"Alaska, British Columbia, Northwest Territories","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -168.046875,\n 54.41892996865827\n ],\n [\n -168.046875,\n 71.01695975726373\n ],\n [\n -114.60937499999999,\n 71.01695975726373\n ],\n [\n -114.60937499999999,\n 54.41892996865827\n ],\n [\n -168.046875,\n 54.41892996865827\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"43","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"567a7432e4b0a04ef490fcc7","contributors":{"authors":[{"text":"Uzmann, J. R.","contributorId":38647,"corporation":false,"usgs":true,"family":"Uzmann","given":"J. R.","affiliations":[],"preferred":false,"id":583263,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hesselholt, M. N.","contributorId":150793,"corporation":false,"usgs":false,"family":"Hesselholt","given":"M.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":583264,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":72026,"text":"tem1097 - 1957 - Uraniferous coal and carbonaceous shale in northeast Parana, Brazil","interactions":[],"lastModifiedDate":"2012-02-02T00:13:59","indexId":"tem1097","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":338,"text":"Trace Elements Memorandum","code":"TEM","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1097","title":"Uraniferous coal and carbonaceous shale in northeast Parana, Brazil","docAbstract":"Uraniferous coal has been found in northeast Parana, Brazil, in the Rio \r\nBonito formation of Pennsylvanian age. In the majority of coal samples taken the uranium oxide content ranges from 0.005 to 0.030 percent, but selected screened samples have contained as much as 0.445 percent uranium oxide. The sampled thickness of the coal seam ranges from 17 to 54 centimeters and averages 31 centimeters. Channel samples across the entire thickness of the coal zone were taken in two places. All other samples were taken as grab samples from either mine waste dumps or coal zones that had high radioactivity.\r\n\r\n\r\nSufficient information is not yet available to justify any detailed considerations of such features as geologic distribution, mode of occurrence, and radioactive equilibrium conditions of the uranium in the coal.\r\n\r\n\r\n","language":"ENGLISH","doi":"10.3133/tem1097","usgsCitation":"Haynes, D., and Pierson, C., 1957, Uraniferous coal and carbonaceous shale in northeast Parana, Brazil: U.S. Geological Survey Trace Elements Memorandum 1097, 20 p.; 1 fig.; 3 plates; 9 tables, https://doi.org/10.3133/tem1097.","productDescription":"20 p.; 1 fig.; 3 plates; 9 tables","numberOfPages":"20","costCenters":[],"links":[{"id":192593,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/tem/1097/report-thumb.jpg"},{"id":91085,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tem/1097/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dee4b07f02db5e29e7","contributors":{"authors":[{"text":"Haynes, Donald D.","contributorId":78400,"corporation":false,"usgs":true,"family":"Haynes","given":"Donald D.","affiliations":[],"preferred":false,"id":285011,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pierson, Charles T.","contributorId":28317,"corporation":false,"usgs":true,"family":"Pierson","given":"Charles T.","affiliations":[],"preferred":false,"id":285010,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":14976,"text":"ofr5772 - 1957 - Geology of possible petroleum provinces in Alaska","interactions":[{"subject":{"id":14976,"text":"ofr5772 - 1957 - Geology of possible petroleum provinces in Alaska","indexId":"ofr5772","publicationYear":"1957","noYear":false,"title":"Geology of possible petroleum provinces in Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":35230,"text":"b1094 - 1959 - Geology of possible petroleum provinces in Alaska","indexId":"b1094","publicationYear":"1959","noYear":false,"title":"Geology of possible petroleum provinces in Alaska"},"id":1}],"supersededBy":{"id":35230,"text":"b1094 - 1959 - Geology of possible petroleum provinces in Alaska","indexId":"b1094","publicationYear":"1959","noYear":false,"title":"Geology of possible petroleum provinces in Alaska"},"lastModifiedDate":"2024-05-03T22:50:46.949424","indexId":"ofr5772","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"57-72","title":"Geology of possible petroleum provinces in Alaska","docAbstract":"The history of petroleum exploration in Alaska and the geology of possible petroleum provinces in Alaska are reviewed. Maps showing Alaska's major Mesozoic and Tertiary tectonic elements, possible petroleum provinces, and indications of petrol, are included in this report. Annotated references in Geological Survey publications relating to petroleum and oil shale in Alaska are given at the end of the report.
For the purpose of appraising its petroleum possibilities, Alaska is divided into the southern, central, and northern major geologic-physiographic regions.
Southern Alaska includes the arcuate mountain chain formed by the Alaska and Aleutian Ranges and the Mentasta- Nutzotin Mountains, the coastal range and valley area to the south, and the southeastern Alaska \"panhandle\" -- an area of 185,000 square miles.
Oil seeps on the west shore of Cook Inlet in southern Alaska were known as early as 1853, and claims were staked in this region in 1882. Drilling began near the oil seeps in the Katalla district about 1901, and this started Alaska's first period of oil activity. From 1902 to 1933 the Katalla field produced 154,000 barrels of oil from fractured shale and sandstone of Tertiary age the- first and only commercial production in Alaska.
On the basis of geology, surficial indications of petroleum, and test wells drilled, six possible petroleum provinces are indicated in southern Alaska. They are Heceta Island area, Keku Islands area, Cook Inlet Mesozoic province, Gulf of Alaska Tertiary province, Cook Inlet Tertiary province, and Copper River basin.
The exposed rocks in the Heceta Island area include lower Paleozoic graywacke-type sandstone, sandstone, conglomerate, and massive limestones with reeflike structures; igneous rocks are rare or lacking in much of the area. The Kosciusko-Tuxekan-Heceta synclinorium, the main structural feature, is modified by minor folds and faults. Some of the minor folds are reported to be broad and open, with flanks dipping 20°-145°. As far as known, the Heceta Island area has not heretofore been seriously considered as a possible petroleum province.
Rocks of Silurian to Cretaceous age are exposed in the Keku Island area and include moderately folded and relatively unaltered limestone and other marine sedimentary rocks.
The Cook Inlet Mesozoic province, a land area of approximately 18,500 square miles, includes a great thickness of unmetamorphosed marine sedimentary rocks of Jurassic and Cretaceous age. At least 23 test wells were drilled or started in this province by the end of 1955. Shows of oil and gas were encountered in many of these wells. During 1955 at least ten oil companies were active in this area and by the end of 1955 about 1 1/2 million acres were included in oil and gas leases applied for or granted.
The Gulf of Alaska Tertiary province includes about 5,200 square miles in which rocks of Tertiary age are exposed or are believed to underlie Quaternary deposits. Between 1901 and the end of 1955 about 47 wells were drilled or started in this province.
The Cook Inlet Tertiary province embraces an area of about 9,500 square miles, of which about 4,100 is covered by the shallow waters of Cook Inlet. Petroleum exploration has been in that part of the area which overlaps the Cook Inlet Mesozoic province. Eocene or younger Tertiary nonmarine sedimentary rocks are believed to underlie much of the province, and marine rocks of Tertiary age may also be present.
The Copper River basin is a topographic basin underlain by unconsolidated deposits of Quaternary age. Tertiary rocks favorable for the accumulation of petroleum may underlie part of the basin but this is not believed likely. Except for some leasing activity no petroleum exploration has been recorded in the Copper River Basin to the end of 1955.
Central Alaska is a region of about 275,000 square miles and consists of an irregular assemblage of intricately dissected uplands and alluvium-floored lowland basins. Scattered peaks of resistant intrusive igneous rocks surmount most of the upland areas.
In the vast region of central Alaska only six test wells are known to have been drilled for the purpose of finding oil and gas. The maximum depth reached was 350 feet and the holes were mostly or entirely in Quaternary deposits. In recent years several oil companies have investigated some parts of the region and large areas in the Yukon-Koyukuk province are now under lease. Oil seeps, gas seeps, and other indications of petroleum have been reported from many localities; samples from two localities have been analyzed and reported to be petroleum.
The geology of central Alaska is similar in a general way to that of the area between the Rocky Mountains and Sierra-Cascade belts of the United States. Sedimentary rocks, probably equivalent to the Precambrian Belt series, and rocks of the Cambrian and all younger geologic systems have been recognized in central Alaska. The structure of the region is known to be complex, but except in local mineral districts, it has not been mapped in detail. Based on the limited amount of available information, the region cannot be regarded as distinctly favorable for significant accumulations of petroleum. However, three pre-Cenozoic provinces, the Yukon-Koyukuk, the Kobuk, and the Kandik, and several large Cenozoic basin provinces may be worthy of further investigation.
Northern Alaska includes the Brooks Range and all the treeless tundra north to the Arctic Coast, an area of about 125,000 square miles. The presence of oil seeps along the Arctic Coast has been known at least since 1900 and a description of the Cape Simpson oil seeps vas published in 1909. Since then oil and gas seeps have been described from nine localities, and oil shales and oil-bearing sandstones are known from many localities in the Arctic Foothills province. Oil and gas deposits have been discovered and geologic conditions are favorable for oil and gas accumulations in approximately half of the region.
In 1923 approximately 37,000 square miles in northern Alaska was reserved by Executive order as Naval Petroleum Reserve No. 4. In 1944 the U. S. Navy began a vast petroleum exploration program which was suspended in 1953. In the years 1945 through 1955, 37 test wells and 45 core tests were drilled on 18 structures. Three oil fields, Umiat, Simpson, and Fish Creek, and two gas fields, South Barrow and Gubik, were discovered. Total reserve estimates for all discoveries of oil to 1955 range from 30 to 100 million barrels, and for gas, from 370 billion to 900 billion cubic feet.
All northern Alaska, with the exception of the Brooks Range, can be considered a possible petroleum province, but the region can be subdivided into provinces of somewhat different potentialities. These subdivisions roughly correspond with the geomorphic provinces and sections, which in turn reflect differences in geology. The known oil-bearing beds are of Mesozoic age, primarily Cretaceous, and thus the possible petroleum provinces could be designated as Mesozoic. However, Paleozoic and Cenozoic rocks with favorable reservoir characteristics are exposed in the region and possibly underlie, in favorable structural situations, some of the areas as yet not tested.
The Arctic Coastal Plain province includes gently folded and flat-lying Mesozoic beds that overlie a basement complex of Paleozoic and early Mesozoic age. Near the southern edge of this province the basement rocks are at depths of at least 20,000 feet, and to the north these rocks rise to within 2,500 feet of the surface.
The Teshukpuk Lake section of the Arctic Coastal plain includes many of the known oil seeps; it is the most accessible to sea transportation, and lies almost completely within NPR 4. Thirteen test wells and 35 core tests have been drilled here; one gas field and two (at present, noncommercial) oil fields have been discovered. The possibility of further discoveries may depend largely on locating porous sandstones in stratigraphic rather than anticlinal traps.
The White Hills section is distinguished topographically from the Teshukpruk section by its white-gravel-covered hills and fever lakes, and geologically by the presence of Tertiary rocks, including 2,000 feet of nonmarine beds in the west and at least 7,000 feet of marine beds to the east, in the vicinity of Carter Creek. This section appears to be more complex structurally. No test wells have been drilled in the White Hills section.
The Northern Foothills section includes many closed anticlines. Twenty-four test wells and ten core tests have been drilled on 11 structures and two discoveries have been made -the Umiat oil field and the Gubik gas field. All these tests have been drilled in Cretaceous rocks.
The Southern Foothills section is structurally similar to the Alberta Foothills and to the northern part of the Brooks Range. Great thicknesses of marine shale of Lover Cretaceous, Jurassic, and Triassic age are exposed. The outcropping Mesozoic sandstones are generally poorly sorted, nonporous, and impermeable. To the south the section is bordered by mountainous exposures of Mississippian limestone, which probably underlie at least part of this section.
The rocks that underlie the deeply eroded complex structures of the Brooks Range include schist, slate, argillite, and limestone. Some exposed limestones have a strong petroleum-like odor and contain traces of petroleum residues.
We live in an age of social and economic evolution--evolution so deep reaching and rapid it constitutes ad revolution in numerous fields of human concern. Long-standing concepts of what is appropriate and orderly face drastic modification if they are to survive. To this situation the principles of applied hydrology and the tenets of water law are no exceptions. Their common ground, incomplete in the past, becomes tenuous when projected into the future.
\nTo hydrologists it is common knowledge that the Nation has some trouble spots tin water supply, occasioned by burgeoning population, by standards of living that seem luxurious to other peoples if not to us, and by tremendously dynamic industry whose voracious thirst for water seems insatiable. Seldom is the \"trouble\" a mere lack of water in a quantity sufficient to serve all real needs; rather, water usually is available only part of the time, at greater-than-customary cost, or under competition among several potential uses. We can expect only that such spots will increase in number and in geographic reach.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5790","usgsCitation":"Piper, A., and Thomas, H.E., 1957, Hydrology and water law: what is their future common ground?: U.S. Geological Survey Open-File Report 57-90, 33 p., https://doi.org/10.3133/ofr5790.","productDescription":"33 p.","numberOfPages":"34","costCenters":[],"links":[{"id":287407,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287406,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1957/0090/report.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e871","contributors":{"authors":[{"text":"Piper, Arthur M.","contributorId":65060,"corporation":false,"usgs":true,"family":"Piper","given":"Arthur M.","affiliations":[],"preferred":false,"id":254748,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Thomas, Harold E.","contributorId":36116,"corporation":false,"usgs":true,"family":"Thomas","given":"Harold","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":254747,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":39151,"text":"pp292 - 1957 - Geology of the southern Elkhorn Mountains, Jefferson and Broadwater Counties, Montana","interactions":[],"lastModifiedDate":"2018-02-23T12:32:11","indexId":"pp292","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"292","title":"Geology of the southern Elkhorn Mountains, Jefferson and Broadwater Counties, Montana","docAbstract":"The geology of an area of about 270 square miles in the southern Elkhorn Mountains, west of Townsend in west-central Montana, is described. The mountains in the southern part of the area comprise northward-trending alternating ridges and valleys underlain principally by folded sedimentary rocks. They merge northward into the higher and more rugged main mass of the mountains, which is underlain principally by upper Cretaceous volcanic rocks. The mountaintops are 1,000 to 4,500 feet above the major valleys.
The sedimentary rocks range in age from Precambrian to Tertiary and the igneous rocks from late Cretaceous to probably middle Tertiary. The oldest rocks are varicolored mudstone, shale, and sandstone of the Belt series of late Precambrian age. They are overlain with slight unconformity by a moderately thick but incomplete section of Paleozoic rocks. The basal Paleozoic formation is the Flathead quartzite of Middle Cambrian age, which is overlain by alternating units of shale and carbonate rock : the Wolsey shale, the Meagher limestone, the Park shale, the Pilgrim dolomite, and the Red Lion formation, all of Cambrian age. A slight erosional unconformity between the Red Lion formation and the Maywood formation of late Devonian age marks a long interval of crustal stability in the area. The Maywood is overlain by the Jefferson dolomite and the Three Forks shale of Late Devonian and Mississippian age, and these in turn are conformably overlain by the Lodgepole and Mission Canyon limestones, a thick carbonate sequence of Mississippian age. A slight erosional unconformity separates the Mission Canyon limestone from the Amsden formation, which probably includes beds of both Mississippian and Pennsylvanian age. The Amsden is composed of a heterogeneous assemblage of arenaceous, argillaceous, dolomitic, and calcareous rocks and grades upward into the Quadrant formation of Pennsylvanian age, an alternation of quartzitic sandstone and dolomite. At the top of the Paleozoic section is the Phosphoria formation of Permian age, a thin unit of chert and quartzitic sandstone that contains a few thin phosphate beds.
The basal Mesozoic unit is the Swift formation of late Jurassic age, a thin calcareous marine sandstone that overlies the Phosphoria with slight erosional unconformity. It is overlain by nonmarine shale and sandstone of the Morrison formation of late Jurassic age and the Kootenai formation of Early Cretaceous age. The Kootenai is overlain, possibly with slight erosional unconformity, by the Colorado formation an assemblage of marine dark shale and siliceous mudstone and nonmarine quartz-chert sandstone. The Colorado formation as here used includes beds of both Early and Late Cretaceous age. The Colorado in places grades upwards into a sequence of feldspathic sandstone and tuff beds here named the Slim Sam formation. Elsewhere within the area, the Slim Sam formation is absent, probably in part owing to erosion and in part nondeposition. Where present, the Slim Sam grades upward into a thick sequence of andesitic and quartz latitic volcanic rocks, comprising tuffs, lapilli tuffs, breccias, welded tuffs and flows, that are here named the Elkhorn Mountains volclinics and are probably entirely of Cretaceous age. Where the Slim Sam formation is absent, the Elkhorn Mountains volcanics rest with angular unconformity on beds as old as the Morrison.
The pre-Tertiary layered rocks, aggregating more than 15,000 feet in thickness, were folded and intruded by igneous rocks of several types, and the area was uplifted and eroded to a terrain of mature relief, similar to that of the present. During the Oligocene epoch, volcanic sediments with interbreds of nonvolcanic gravel accumulated. These beds were in turn moderately eroded, and gravel of Miocene ( ?) age was deposited in channels within them. Subsequently, probably during the Pliocene epoch, the Tertiary beds were weakly deformed locally, and a pediment was cut across the Tertiary and older rocks in the southern part of the area. Fan gravel, in part of Recent origin and in part older, blankets parts of the pediment. Glacial deposits of at least two stages of Pleistocene glaciation are present in the higher mountains in the northern part of the area.
The intrusive igneous rocks, except for a few felsite dikes of uncertain age, are divisible into two groups, primarily on the basis of structural relations and secondarily on the basis of composition and fabric. The older group of dioritic and andesitic rocks were intruded in part, if not wholly, prior to the main folding and are similar in chemical and mineralogical composition to the Elkhorn Mountains volcanics. They were probably emplaced throughout the period of volcanism that commenced in late Niobrara time and continued until late Cretaceous time. The younger group consists chiefly of quartzbearing phanerites but includes rocks ranging from gabbro to alaskitic granite and aplite. These rocks were emplaced after the main episode of folding and faulting. The Boulder batholith, composed dominantly of quartz monzonite, is the principal body of this younger group.
The older igneous rocks metamorphosed the invaded rocks only slightly. In contrast, the younger intrusive bodies, and especially the batholith, altered and recrystallized the country rock in moderately broad belts, changing them to various types of hornfels, calcsilicate rock, marble, and vitreous quartzite. Concomitantly magnetite, garnet, axinite, and other high-temperature replacement minerals formed locally as products of additive metamorphism.
The pre-Tertiary layered rocks of the southern Elkhorn Mountains are folded into northward-trending folds and are cut by many faults. The sedimentary rocks tend to be more tightly folded than the Elkhorn Mountains volcanics, although both were involved in the major folding. The principal folds of the area from east to west are : a major dome, a complex syncline with several second-order folds, and a remnant of a northward-plunging anticline, the major part of which was engulfed by the batholith. The folded rocks are cut by many faults of small to moderate displacement and by two faults of large displacement. Most of the faults were probably formed by the same forces that produced the folds. The origin of the two major faults, however, is uncertain, and may be related to igneous activity. The batholith crosscuts the folded structure and is in turn cut by small faults. Some parts of the area were elevated along steep normal faults in late Tertiary time.
The southern part of the Elkhorn Mountains has been mountainous at least since early Oligocene time, and probably began to take form during the Cretaceous. As a consequence of long continued erosion, the modern topography reflects the structure and lithologic character of the underlying rocks except in a few areas blanketed by poorly consolidated Tertiary rocks and in the higher mountains where glaciation has been prominent.
Silver, lead, zinc, and gold have been produced, either singly or, more typically, as a combination of metals from a number of types of ore deposits. Replacement deposits in carbonate rocks are the most common type, but veins, contact metamorphic deposits, and pipelike bodies of breccia cemented by ore and gangue minerals also are present. The Elkhorn mining district has the largest number of mines and the greatest variety of types of deposits. In the Tizer Basin several narrow goldbearing veins cut andesitic volcanic rocks, and in the southern part of the area sporadic small veins and replacement deposits occur in carbonate rocks. The mines and prospects of the area are described, and some suggestions for future prospecting are outlined. The application of geochemical prospecting techniques may prove of value, judging from the results of reconnaissance soil sampling in the vicinity of the Elkhorn mine.
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp292","usgsCitation":"Klepper, M.R., Weeks, R.A., and Ruppel, E.T., 1957, Geology of the southern Elkhorn Mountains, Jefferson and Broadwater Counties, Montana: U.S. Geological Survey Professional Paper 292, Report: iv, 82 p.; 7 Plates: 44.48 x 23.48 inches or smaller, https://doi.org/10.3133/pp292.","productDescription":"Report: iv, 82 p.; 7 Plates: 44.48 x 23.48 inches or smaller","costCenters":[],"links":[{"id":351914,"rank":9,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0292/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271139,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271143,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271144,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271145,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271146,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271138,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271141,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":165294,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0292/report-thumb.jpg"}],"scale":"31250","country":"United States","state":"Montana","county":"Broadwater County;Jefferson County","otherGeospatial":"Elkhorn Mountains","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112.92,46.12 ], [ -112.92,47.23 ], [ -111.03,47.23 ], [ -111.03,46.12 ], [ -112.92,46.12 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c79e","contributors":{"authors":[{"text":"Klepper, M. R.","contributorId":64278,"corporation":false,"usgs":true,"family":"Klepper","given":"M.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":221047,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weeks, R. A.","contributorId":75914,"corporation":false,"usgs":true,"family":"Weeks","given":"R.","middleInitial":"A.","affiliations":[],"preferred":false,"id":221048,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ruppel, E. T.","contributorId":6041,"corporation":false,"usgs":true,"family":"Ruppel","given":"E.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":221046,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":39736,"text":"pp274L - 1957 - Volcanic rocks of the El Modeno area, Orange County, California","interactions":[],"lastModifiedDate":"2012-02-02T00:10:36","indexId":"pp274L","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"274","chapter":"L","title":"Volcanic rocks of the El Modeno area, Orange County, California","language":"ENGLISH","doi":"10.3133/pp274L","usgsCitation":"Yerkes, R.F., 1957, Volcanic rocks of the El Modeno area, Orange County, California: U.S. Geological Survey Professional Paper 274, p. 313-334, https://doi.org/10.3133/pp274L.","productDescription":"p. 313-334","costCenters":[],"links":[{"id":104413,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4250.htm","linkFileType":{"id":5,"text":"html"},"description":"4250"},{"id":121757,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0274l/report-thumb.jpg"},{"id":67509,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0274l/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67510,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0274l/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67511,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0274l/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0de4b07f02db5fd90f","contributors":{"authors":[{"text":"Yerkes, R. F.","contributorId":24754,"corporation":false,"usgs":true,"family":"Yerkes","given":"R.","middleInitial":"F.","affiliations":[],"preferred":false,"id":222058,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39154,"text":"pp294D - 1957 - Stromatolites of the Belt Series in Glacier National Park and Vicinity, Montana","interactions":[],"lastModifiedDate":"2017-12-14T10:59:51","indexId":"pp294D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"294","chapter":"D","title":"Stromatolites of the Belt Series in Glacier National Park and Vicinity, Montana","docAbstract":"Eight zones of Precambrian stromatolites that are useful for local correlation are recognized in the Belt series of the Glacier National Park region, Montana. The zones vary in composition, thickness, and areal extent. Some are widespread and extend into neighboring regions, and others occur only in small areas. Their names are taken from the dominant species that occurs in each zone. The zones are, from youngest to oldest -\r\n\r\nConophyton zone 2 \r\n Missoula group \r\nCollenia symmetrica zone 2 \r\nCollenia undosa zone 2 \r\nCollenia multiflabella zone \r\n Piegan group \r\nConophyton zone 1 \r\nCollenia symmetrica zone 1 \r\nCollenia undosa zone 1 \r\n Ravalli group \r\nCollenia frequens zone \r\n\r\nOnly the Conophyton zones have been mapped in the park area.\r\n\r\nThe present study uses a classification based upon the three criteria of (1) mode of growth, (2) gross form of the colony, and (3) nature and orientation of the laminae. The scheme of classification also seems applicable to Paleozoic and later stromatolites. Possibly a consistent pattern of form-genera and form-species may be developed. Four form-genera and seven form-species are recognized in the Belt series of the park region. These are Cryptozoon occidentale Dawson, Collenia undosa Walcott, C. frequens Walcott, C. symmetrica Fenton and Fenton, Newlandia sp., and Conophyton inclinatum n. sp.\r\n\r\nIt is realized that these structures should not be classified according to biological nomenclature. However, biological names are here applied to the structures until a suitable system of classification can be devised.\r\n\r\nComparisons of the stromatolites of the Belt series with modern stromatolites on Andros Island, Bahama Islands, and Pleistocene stromatolites from Lake Lahonton, Nev., reveal similarities in structure that appear to be significant as to physical mode of origin.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Shorter Contributions to General Geology 1956","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp294D","usgsCitation":"Rezak, R., 1957, Stromatolites of the Belt Series in Glacier National Park and Vicinity, Montana: U.S. Geological Survey Professional Paper 294, p. 127-154, https://doi.org/10.3133/pp294D.","productDescription":"p. 127-154","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":66671,"rank":399,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0294d/plate-1.pdf","text":"Plate 25","linkFileType":{"id":1,"text":"pdf"}},{"id":66672,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0294d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124864,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0294d/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b15e4b07f02db6a4c02","contributors":{"authors":[{"text":"Rezak, Richard","contributorId":48963,"corporation":false,"usgs":true,"family":"Rezak","given":"Richard","email":"","affiliations":[],"preferred":false,"id":221052,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15737,"text":"ofr5887 - 1957 - Geology of the Basin Quadrangle, Montana","interactions":[{"subject":{"id":15737,"text":"ofr5887 - 1957 - Geology of the Basin Quadrangle, Montana","indexId":"ofr5887","publicationYear":"1957","noYear":false,"title":"Geology of the Basin Quadrangle, Montana"},"predicate":"SUPERSEDED_BY","object":{"id":35698,"text":"b1151 - 1963 - Geology of the Basin quadrangle: Jefferson, Lewis and Clark, and Powell Counties, Montana","indexId":"b1151","publicationYear":"1963","noYear":false,"title":"Geology of the Basin quadrangle: Jefferson, Lewis and Clark, and Powell Counties, Montana"},"id":1}],"supersededBy":{"id":35698,"text":"b1151 - 1963 - Geology of the Basin quadrangle: Jefferson, Lewis and Clark, and Powell Counties, Montana","indexId":"b1151","publicationYear":"1963","noYear":false,"title":"Geology of the Basin quadrangle: Jefferson, Lewis and Clark, and Powell Counties, Montana"},"lastModifiedDate":"2024-07-17T19:47:34.920637","indexId":"ofr5887","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"58-87","title":"Geology of the Basin Quadrangle, Montana","docAbstract":"The Basin quadrangle, in the northern part of the Boulder Mountains between Butte and Helena, Montana, is underlain principally by igneous rocks that include Late Cretaceous quartz latitic and andesitic Elkhorn Mountains volcanics, quartz monzonite and related rocks of the Boulder batholith, Oligocene(?) quartz latitic volcanic rocks, and late Miocene(?)-early Pliocene(?) rhyolitic volcanic rocks. Sedimentary rocks of the Late Jurassic Morrison formation, the Early Cretaceous Kootenai formation, and the Early Cretaceous lower part of the Colorado formation, crop out in the northwest part of the quadrangle. The batholithic rocks include early stage quartz monzonite, intermediate or main stage quartz monzonite and granodiorite, and late stage aplite and alaskite. The rocks of the main stage are in discontinuous layers approximately conformable to the folded Elkhorn Mountains volcanics that form the roof of the batholith, and may be part of a sill-like body rather than of a batholith in the classic sense. Metamorphic changes in the roof rocks are not conspicuous except in one stratigraphic unit that probably was especially susceptible to thermal reorganization.
The batholithic rocks and Elkhorn Mountains volcanics are jointed, and are cut by faults that trend about east, north, N. 20° E., northeast, and northwest. The east-trending faults are most abundant, especially in the eastern part of the quadrangle, and cut only the batholithic and pre-batholithic rocks, whereas many of the faults of other trends cut Tertiary volcanic rocks and a few cut Pleistocene glacial deposits.
A surface of moderate relief was cut before eruption of the Oligocene(?) volcanic rocks, and the late Miocene(?)-early Pliocene(?) volcanic rocks covered a deeply weathered surface of low relief. By the Pleistocene a landscape essentially like that of today had been formed, and during the one period of Pleistocene glaciation, valley glaciers and a mountain ice sheet modified the earlier landforms and left extensive deposits of till and outwash. These deposits have been modified in many places by mass-wasting processes that have dominated post-glacial erosion.
Mineral deposits in the quadrangle include deposits of disseminated auriferous pyrite, base- and precious-metal bearing quartz veins that occupy the east-trending fault zones, placer deposits of gold and tin, and a few non-metallic deposits, chiefly stone, gravel, and dumortierite. Nearly all of the metallic minerals mined in the quadrangle have come from the east-trending quartz veins and from the placer deposits.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5887","usgsCitation":"Ruppel, E.T., 1957, Geology of the Basin Quadrangle, Montana: U.S. Geological Survey Open-File Report 58-87, Report: viii, 219 p.; 7 Plates: 34.96 x 52.09 inches or smaller; 7 Tables: 23.93 x 24.44 inches or smaller, https://doi.org/10.3133/ofr5887.","productDescription":"Report: viii, 219 p.; 7 Plates: 34.96 x 52.09 inches or smaller; 7 Tables: 23.93 x 24.44 inches or smaller","costCenters":[],"links":[{"id":431191,"rank":16,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431190,"rank":15,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431189,"rank":14,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431188,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431187,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431186,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431185,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431184,"rank":9,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1958/0087/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431183,"rank":8,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431182,"rank":7,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431181,"rank":6,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431180,"rank":5,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431179,"rank":4,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431178,"rank":3,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431177,"rank":2,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":146495,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1958/0087/report-thumb.jpg"}],"scale":"24000","country":"United States","state":"Montana","otherGeospatial":"Basin Quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -112.55138492319185,\n 46.59423812949282\n ],\n [\n -112.55138492319185,\n 46.03252022844208\n ],\n [\n -111.78355228633728,\n 46.03252022844208\n ],\n [\n -111.78355228633728,\n 46.59423812949282\n ],\n [\n -112.55138492319185,\n 46.59423812949282\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db6834cd","contributors":{"authors":[{"text":"Ruppel, Edward Thompson","contributorId":67066,"corporation":false,"usgs":true,"family":"Ruppel","given":"Edward","email":"","middleInitial":"Thompson","affiliations":[],"preferred":false,"id":171622,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15450,"text":"ofr5791 - 1957 - Glacial features and surficial deposits of the Malaspina district, Alaska","interactions":[{"subject":{"id":15450,"text":"ofr5791 - 1957 - Glacial features and surficial deposits of the Malaspina district, Alaska","indexId":"ofr5791","publicationYear":"1957","noYear":false,"title":"Glacial features and surficial deposits of the Malaspina district, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":66820,"text":"i271 - 1958 - Glacial features and surficial deposits of the Malaspina district, Alaska","indexId":"i271","publicationYear":"1958","noYear":false,"title":"Glacial features and surficial deposits of the Malaspina district, Alaska"},"id":1}],"supersededBy":{"id":66820,"text":"i271 - 1958 - Glacial features and surficial deposits of the Malaspina district, Alaska","indexId":"i271","publicationYear":"1958","noYear":false,"title":"Glacial features and surficial deposits of the Malaspina district, Alaska"},"lastModifiedDate":"2024-01-26T21:33:37.679674","indexId":"ofr5791","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"57-91","title":"Glacial features and surficial deposits of the Malaspina district, Alaska","docAbstract":"The Malaspina district extends about 50 miles along the north shore of the Gulf of Alaska from Icy Bay and the Guyot Glacier on the west to Yakutat Bay and Disenchantment Bay on the east (see index map). The district includes a coastal lowland flanked on the north by a belt of rugged foothills, the higher ridges and peaks of which rise to altitudes of 1,000 to 6,000 feet. The southern front of the St. Ell as Mountains rises abruptly at the northern margin of the foothills belt, about 30 miles from the coast, culminating in Mount St. Elias (18,008 ft.).
The Malaspina Glacier, the dominant feature of the Malaspina district, has long been regarded as the type example of the piedmont glacier. This huge ice sheet covers an area of about 840 square miles of the coastal lowland, rising gradually from an altitude of 100 feet or less at the outer margin to altitudes ranging from 1,000 feet to 2,000 feet at the southern margin of the foothills belt. The Malaspina Glacier is of special interest to glaciologists because its strikingly developed morainic banding offers clues to the nature of glacier movement. The processes of wastage and deposition at the stagnant margin of Malaspina Glacier can be compared with the mode of retreat of the former continental ice sheets; much can be learned here of the origin
of the deposits formed along a stagnant ice margin.
The Bruneau-Grand View area is part of an artesian basin in northern Owyhee \nCounty, Idaho. The area described in this report comprises about 600 square \nmiles, largely of undeveloped public domain, much of which is open, or may be \nopened, for desert-entry filing. Many irrigation-entry applications to the Federal \nGovernment are pending, and information about ground-water geology is needed \nby local citizens and well drillers, by Federal agencies that have custody of the \nland, and by local and State agencies that administer water rights. The areal \ngeology and ground-water conditions in the Bruneau-Grand View area seemingly \ntypify several basins in southwestern Idaho, and this study is a step toward \ndefinition and analysis of regional problems in ground-water geology and the \noccurrence and availability of ground water for irrigation or other large-scale \nuses.
\nOwyhee County is subdivided physiographically into a plateau area, the Owyhee uplift, and the Snake River valley. The Bruneau-Grand View area is largely \nwithin the Snake River valley. The climate is arid and irrigation is essential \nfor stable agricultural development. Nearly all usable indigenous surface water \nin the area is appropriated, including freshet flow in the Bruneau River, which \nis used for power generation at the C. J. Strike Dam. However, with storage \nfacilities additional land could be irrigated, and some land may be irrigated with \nSnake River water if suitable reclamation projects are constructed.
\nSedimentary and igneous rocks exposed in the area range in age from Miocene \nto Recent. The igneous rocks include silicic and basic intrusive and extrusive \nbodies, and the sedimentary rocks are compacted stream and lake sediments. \nThe rocks contain economically important artesian aquifers; the principal ones \nare volcanic rocks in which ground water is imperfectly confined beneath sediments of the Idaho formation, thus forming a leaky artesian system. The altitude \nof the piezometric surface of the artesian water does not exceed about 2,700 \nfeet above mean sea level. In some areas, where the land surface is below \nthat altitude, the artesian system discharges water through springs and seeps \nand locally causes waterlogging and development of alkali soil.
\nIn chemical quality much of the water is unsuitable for irrigation and domestic \nuse. The water contains a relatively moderate amount of dissolved solids, but \nthe percent sodium and the concentration of fluoride are excessive for some \nuses. The quality of the water for irrigation ranges from excellent in the southern part of the artesian system to unsuitable in the northern part. All the \nartesian ground water that was sampled contained excessive amounts of fluoride.
\nThere is a substantial supply of undeveloped artesian water in the area, but\nsustained use of the water for irrigation may not be feasible unless provisions \ncan be made for adequate soil drainage and soil amendment, because of the high \npercentage of sodium in the water. Detailed hydrologic and geologic study of \nthe area should precede development.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States, 1956-59","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1460D","collaboration":"Prepared in cooperation with the Idaho State Department of Reclamation","usgsCitation":"Littleton, R.T., and Crosthwaite, E., 1957, Ground-water geology of the Bruneau–Grand View area, Owyhee County, Idaho: U.S. Geological Survey Water Supply Paper 1460, iv, 52 p., https://doi.org/10.3133/wsp1460D.","productDescription":"iv, 52 p.","numberOfPages":"56","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":27735,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1460d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":394537,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24389.htm"},{"id":137776,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1460d/report-thumb.jpg"}],"country":"United States","state":"Idaho","county":"Owyhee County","otherGeospatial":"Bruneau River, Snake River Valley","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -116.262,42.757 ], [ -116.262,43.757 ], [ -115.6310,43.757 ], [ -115.6310,42.757 ], [ -116.262,42.757 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaae4b07f02db668e08","contributors":{"authors":[{"text":"Littleton, Robert Thomas","contributorId":87912,"corporation":false,"usgs":true,"family":"Littleton","given":"Robert","email":"","middleInitial":"Thomas","affiliations":[],"preferred":false,"id":144718,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Crosthwaite, E. G.","contributorId":83098,"corporation":false,"usgs":true,"family":"Crosthwaite","given":"E. G.","affiliations":[],"preferred":false,"id":144717,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2562,"text":"wsp1377 - 1957 - Geology and ground-water resources of Goshen County Wyoming with a section on chemical quality of the ground water","interactions":[{"subject":{"id":51788,"text":"ofr54322 - 1954 - Geology and groundwater resources of the North Platte Irrigation Project area in Goshen County, Wyoming","indexId":"ofr54322","publicationYear":"1954","noYear":false,"title":"Geology and groundwater resources of the North Platte Irrigation Project area in Goshen County, Wyoming"},"predicate":"SUPERSEDED_BY","object":{"id":2562,"text":"wsp1377 - 1957 - Geology and ground-water resources of Goshen County Wyoming with a section on chemical quality of the ground water","indexId":"wsp1377","publicationYear":"1957","noYear":false,"title":"Geology and ground-water resources of Goshen County Wyoming with a section on chemical quality of the ground water"},"id":1}],"lastModifiedDate":"2022-02-17T20:03:36.844362","indexId":"wsp1377","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"1377","title":"Geology and ground-water resources of Goshen County Wyoming with a section on chemical quality of the ground water","docAbstract":"Goshen County, which has an area of 2,186 square miles, lies in southeastern Wyoming. The purpose of this study was to evaluate the ground-water resources of the county by determining the character, thickness, and extent of the waterbearing materials; the source, occurrence, movement, quantity, and quality of the ground water; and the possibility of developing additional ground water. The rocks exposed in the area are sedimentary and range in age from Precambrian to Recent. A map that shows the areas of outcrop and a generalized section that summarizes the age, thickness, physical character, and water supply of these formations are included in the report. Owing to the great depths at which they lie beneath most of the county, the formations older than the Lance formation of Late Cretaceous age are not discussed in detail. The Lance formation, of Late Cretaceous age, which consists mainly of beds of fine-grained sandstone and shale, has a maximum thickness of about 1,400 feet. It yields water, which usually is under artesian pressure, to a large number of domestic and stock wells in the south-central part of the county. Tertiary rocks in the area include the Chadron and Brule formations of Oligocene age, the Arikaree formation of Miocene age, and channel deposits of Pliocene age. The Chadron formation is made up of two distinct units: a lower unit of highly variegated fluviatile deposits that has been found only in the report area; and an upper unit that is typical of the formation as it occurs in adjacent areas. The lower unit, which ranges in thickness from a knife edge to about 95 feet, is not known to yield water to wells, but its coarse-grained channel deposits probably would yield small quantities of water to wells. The upper unit, which ranges in thickness from a knife edge to about 150 feet, yields sufficient quantities of water for domestic and stock uses from channel deposits of sandstone under artesian pressure. The Brule formation, which is mainly a siltstone, ranges in thickness from a knife edge to about 450 feet and yields water to domestic and stock wells from fractures and from lenses of sandstone. The Arikaree formation ranges in thickness from a knife edge to about 1,000 feet, and yields water to several domestic and stock wells in the northwestern part of the area. The Pliocene channel deposits, which probably do not exceed 25 feet in thickness, are not a source of water for wells in Goshen County. The upland deposits, which are mainly of Pleistocene age, generally are dry and do not serve as aquifers; however, test drilling revealed several deep, buried channels occupied by deposits which probably would yield moderate quantities of water to wells if a sufficient saturated thickness were penetrate The deposits of the third terrace, which are of Pleistocene age, range in thickness from a knife edge to about 210 feet and yield water to a large number of irrigation wells in the area. The flood-plain deposits, which are of Pleistocene and Recent age, range in thickness from a knife edge to about 200 feet. Those in the valley of the North Platte River yield abundant water to many large supply wells. The flood-plain deposits along the valley of Rawhide Creek consist mainly of fine-grained materials and yield large supplies of water to well only in the lower stretches of the creek valley near its confluence with the valley of the North Platte River. The deposits along the valleys of Horse and Bear Creeks generally are relatively thin and fine grained. In the vicinity of Ls grange, however, the deposits, which are about 45 feet thick, yield moderate, supplies of water to several irrigation wells. Other Recent deposits in the area--dune sand, loesslike deposits, and slope wash--generally are fine grained and relatively thin and, hence, are not important sources of ground water. The unconsolidated sand and gravel of the flood-plain and terrace deposits are the principal aquifers in the area.
","language":"English","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1377","usgsCitation":"Rapp, J.R., Visher, F.N., Littleton, R., and Durum, W.H., 1957, Geology and ground-water resources of Goshen County Wyoming with a section on chemical quality of the ground water: U.S. Geological Survey Water Supply Paper 1377, Report: vi, 145 p.; 4 Plates: 30.00 × 51.00 inches or smaller, https://doi.org/10.3133/wsp1377.","productDescription":"Report: vi, 145 p.; 4 Plates: 30.00 × 51.00 inches or smaller","costCenters":[],"links":[{"id":28825,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1377/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109940,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24359.htm","linkFileType":{"id":5,"text":"html"},"description":"24359"},{"id":28824,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1377/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28823,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1377/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28822,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1377/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28821,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1377/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138658,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1377/report-thumb.jpg"}],"country":"United States","state":"Wyoming","county":"Goshen County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-104.0525,42.6128],[-104.0525,42.0879],[-104.0525,42.0024],[-104.0525,41.998],[-104.0522,41.7004],[-104.0522,41.6975],[-104.0521,41.5654],[-104.6491,41.5656],[-104.6506,41.651],[-104.6513,41.8418],[-104.6544,42.2159],[-104.6546,42.5228],[-104.6516,42.61],[-104.616,42.6105],[-104.5967,42.6104],[-104.4777,42.6104],[-104.3598,42.6117],[-104.1247,42.6113],[-104.0525,42.6128]]]},\"properties\":{\"name\":\"Goshen\",\"state\":\"WY\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685b7f","contributors":{"authors":[{"text":"Rapp, J. R.","contributorId":29394,"corporation":false,"usgs":true,"family":"Rapp","given":"J.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":145399,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Visher, F. N.","contributorId":52554,"corporation":false,"usgs":true,"family":"Visher","given":"F.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":145400,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Littleton, R. T.","contributorId":25136,"corporation":false,"usgs":true,"family":"Littleton","given":"R. T.","affiliations":[],"preferred":false,"id":145398,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Durum, W. H.","contributorId":78311,"corporation":false,"usgs":true,"family":"Durum","given":"W.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":145401,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":55765,"text":"ofr5740 - 1957 - Water quality: a factor in Arkansas River development","interactions":[],"lastModifiedDate":"2019-06-11T15:26:25","indexId":"ofr5740","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"57-40","title":"Water quality: a factor in Arkansas River development","docAbstract":"One of the first requisites for intelligent planning of the utilization and control of water and for the administration of laws relating to its use, is data on the quantity, quality, and mode of occurrence of water supplies. The collections, evaluation, interpretation, and publication of such data constitute the primary function of the Water Resources Division of the United States Geological Survey. Since 1895 the Congress has made appropriations to this agency for investigations of the water resources of the Nation. In 1929 the Congress adopted the policy of dollar-for-dollar cooperation with State and local governmental agencies for water-resources investigations. The Geological Survey's Federal-State cooperative program of quality-of-water investigations in Oklahoma was started in 1944 in cooperation with the Oklahoma Planning and Resources Board. Since July of this year the program has been carried on cooperatively with the newly created Oklahoma Water Resources Board.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr5740","usgsCitation":"Dover, T., 1957, Water quality: a factor in Arkansas River development: U.S. Geological Survey Open-File Report 57-40, 14 p., https://doi.org/10.3133/ofr5740.","productDescription":"14 p.","numberOfPages":"17","costCenters":[],"links":[{"id":287375,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287374,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1957/0040/report.pdf"}],"country":"United States","state":"Oklahoma","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.0025,33.6158 ], [ -103.0025,37.0023 ], [ -94.4307,37.0023 ], [ -94.4307,33.6158 ], [ -103.0025,33.6158 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dfe4b07f02db5e3ab3","contributors":{"authors":[{"text":"Dover, T.B.","contributorId":90293,"corporation":false,"usgs":true,"family":"Dover","given":"T.B.","email":"","affiliations":[],"preferred":false,"id":254212,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39064,"text":"pp314B - 1957 - Bathygalea, a genus of moderately deep-water and deep-water Miocene to Recent cassids","interactions":[],"lastModifiedDate":"2012-02-02T00:09:59","indexId":"pp314B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"314","chapter":"B","title":"Bathygalea, a genus of moderately deep-water and deep-water Miocene to Recent cassids","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Shorter contributions to general geology, 1957","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"ENGLISH","doi":"10.3133/pp314B","usgsCitation":"Woodring, W., and Olsson, A., 1957, Bathygalea, a genus of moderately deep-water and deep-water Miocene to Recent cassids: U.S. Geological Survey Professional Paper 314, p. 21-26, https://doi.org/10.3133/pp314B.","productDescription":"p. 21-26","costCenters":[],"links":[{"id":120002,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0314b/report-thumb.jpg"},{"id":66325,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0314b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66326,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0314b/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6fe4b07f02db640aed","contributors":{"authors":[{"text":"Woodring, W. P.","contributorId":48230,"corporation":false,"usgs":true,"family":"Woodring","given":"W. P.","affiliations":[],"preferred":false,"id":220883,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Olsson, A.A.","contributorId":103929,"corporation":false,"usgs":true,"family":"Olsson","given":"A.A.","email":"","affiliations":[],"preferred":false,"id":220884,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":13905,"text":"ofr5840 - 1957 - Pegmatite geology of the Shelby district, North Carolina","interactions":[],"lastModifiedDate":"2012-02-02T00:06:44","indexId":"ofr5840","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"58-40","title":"Pegmatite geology of the Shelby district, North Carolina","docAbstract":"The Shelby district is divided into a northwestern and a southeastern province. The rocks in the southeastern province include various units in the Battleground schist formation and the Yorkville granodiorite. Those in the northwestern province include the Carolina gneiss, with its Shelby gneiss member, and the Toluca quartz monzonite. The Cherryville quartz monzonite forms a batholith that is just west of the boundary between the two provinces. Pegmatites related to both the Toluca and the Cherryville quartz monzonites lie in the Carolina gneiss and many dikes of pegmatite that are related to the Cherryville quartz monzonite are in the tin-spodumene belt that lies along the boundary between provinces. The rocks of the southeastern province have been bent into steep isoclinal folds; those of the northwestern province were bent into open folds and gently-dipping isoclinal folds. The rocks to the southeast have been metamorphosed in the epidote-amphibolite facies whereas the rocks to the northwest represent the amphibolite or granulite facies.\r\n\r\nThe pegmatites related to the Toluca quartz monzonite form sills, dikes, and concordant lenses in the Carolina gneiss, as well as dikes in the Toluca quartz monzonite. The bodies are unzoned and consist mainly of gneissic microcline-plagioclase-quartz pegmatite. The pegmatites related to the Cherryville quartz monzonite form dikes and disconformable lenses in the Carolina gneiss and the Toluca quartz monzonite. These pegmatites range widely in composition and many are zoned. The dikes west of the Cherryville batholith are rich in muscovite and plagioclase and may contain no microcline or only a moderate amount of microcline. Quartz cores and microcline-rich intermediate zones are common. Similar pegmatite forms dikes along the west edge of the tin-spodumene belt. The tin-spodumene belt containes albite-microcline-spodumene-quartz pegmatite. These dikes of albitic pegmatite are largest and most nearly parallel to one another south of Kings Mountain. Farther north they lie in fractures of several sets.\r\n\r\nThe main factors that affected the development of zones in the pegmatite dikes are composition of magma, temperatures of magma and wall rock, and deformation during crystallization. For best development of zones and the growth of the largest muscovite books the rate of cooling and the rate of crystal growth must be rather fast. Complete consolidation probably was reached in most dikes within a gew years after the start of crystallization.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr5840","usgsCitation":"Griffitts, W.R., 1957, Pegmatite geology of the Shelby district, North Carolina: U.S. Geological Survey Open-File Report 58-40, 123 p. ill., maps (1 col.) ;28 cm., https://doi.org/10.3133/ofr5840.","productDescription":"123 p. ill., maps (1 col.) ;28 cm.","costCenters":[],"links":[{"id":145384,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1958/0040/report-thumb.jpg"},{"id":42544,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0040/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42545,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0040/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42546,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0040/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42547,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1958/0040/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e47a3e4b07f02db496619","contributors":{"authors":[{"text":"Griffitts, Wallace R.","contributorId":103260,"corporation":false,"usgs":true,"family":"Griffitts","given":"Wallace","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":168612,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70207235,"text":"70207235 - 1957 - Notes on the structural geology of Puerto Rico","interactions":[],"lastModifiedDate":"2020-07-16T19:10:26.156538","indexId":"70207235","displayToPublicDate":"1957-12-31T14:33:44","publicationYear":"1957","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Notes on the structural geology of Puerto Rico","docAbstract":"Two major structural and stratigraphic rock units occur in Puerto Rico: the older complex, ranging in known age from Late Cretaceous to late Paleocene or early Eocene and the middle Tertiary sequence, ranging from late Oligocene possibly to late Miocene. The former rocks are eugeosynclinal in character and are very badly faulted but for the most part apparently only moderately folded. With the exception of a large, partly low-angle thrust, the writer has not recognized evidence of strong tangential stresses. Intra-formational folding in the older complex is interpreted as caused by submarine sliding (slump structure). Except in the vicinity of the larger plutonic intrusions and in the northeastern and southwestern corners of the island, the main strike alignment of the older complex is northwestward. The plutons are roughtly concordant with the structure of the country rock and show varying degrees of differentiation. Their average composition seems to be more acidic than that of the volcanic and volcanogenetic rocks into which they are intruded. The middle Tertiary sequence is nonvolcanic, made up dominantly of calcareous marine sediments. It crops out on the north and south sides of the island and in structural troughs on the west coast. On the north coast the beds dip gently to the north, and, except for slight terracings and a flexure at the northwestern corner of the island, are not folded. The middle Tertiary sequence on the south side of the island is somewhat folded. Seismic-reflection studies of the north coast indicate, however, a pronounced northward thickening, possibly some folding, and unconformities at depth. Unconformities which may be local have also been noted at several places on the surface. Several large faults in the middle Tertiary sequence have been recognized in both the north- and south-coast belts. The pattern of master joints that is inferred in the north-coast middle Tertiary belt from topographic alignments seems to indicate (1) control by fades contacts, (2) possible downwarping associated with the sinking of an arm of the Puerto Rican Trench, and (3) tension during upwarping along the island axis. The dates of the major diastrophic events that are decipherable from the Puerto Rican data are: (1) early Tertiary (possibly late Paleocene, but more probably Eocene), when the older complex was deformed; (2) Miocene, when the middle Tertiary sequence was deformed; (3) late Pliocene and possibly early Pleistocene, when block faulting on a large scale produced the present topographic relief. Remnants of the fault scarps resulting from the latter deformation occur widely. Quaternary marine deposits and marine terraces suggest that Puerto Rico has been relatively unaffected by crustal movement at least since the late Pleistocene.
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A.","contributorId":6003,"corporation":false,"usgs":true,"family":"Kaye","given":"C.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":777384,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70206668,"text":"70206668 - 1957 - Lithofacies of the salt wash member of the Morrison Formation, Colorado plateau","interactions":[],"lastModifiedDate":"2019-11-15T06:59:33","indexId":"70206668","displayToPublicDate":"1957-12-31T06:54:03","publicationYear":"1957","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}},"displayTitle":"Lithofacies of the salt wash member of the Morrison Formation, Colorado plateau","title":"Lithofacies of the salt wash member of the Morrison Formation, Colorado plateau","docAbstract":"The Salt Wash is the basal member of the Upper Jurassic Morrison Formation in parts of Utah, Colorado, Arizona, and New Mexico. Deposited by streams, it comprises lenticular beds of cross-laminated sandstone irregularly interbedded with mudstone, siltstone, claystone, and horizontally laminated sandstone. The term \"lithofacies,\" as used in this paper, denotes lithologic aspect. The specific lithofacies of the Salt Wash member at a given locality is determined by the thickness, proportion, and continuity of the stream and flood-plain deposits that make up the Salt Wash. Stream deposits include all rocks interpreted as deposited from moving water; flood-plain deposits include all rocks interpreted as deposited from slack water. Regional differences in lithofacies show that the Salt Wash member is a fan-shaped wedge of sedimentary rocks whose apex is in south-central Utah. Within the wedge, the thickness of the Salt Wash and the thickness, proportion, and continuity of the contained stream deposits decrease relatively uniformly to the north, northeast, and southeast of the apex. Interpretation of the regional differences in lithofacies indicates deposition by a distributary stream system whose apex was in south-central Utah and which spread sediments to the north, east, and southeast over a nearly flat plain. Irregularities on this plain near the Four Corners area and in west-central Colorado modified the distributary system, and therefore the wedge is not symmetrical. Most uranium-vanadium ore deposits in the Salt Wash member occur in a lithofacies near the center of the wedge. This may be a genetic relation and can be explained as a function of transmissibility of the particular lithofacies. The ore deposits, however, are concentrated in a relatively small part of the central lithofacies. Because local geologic features such as structure or igneous intrusions might control the localization of ore deposits in the small area, the high degree of correlation of ore deposits and a certain lithofacies may be coincidental. © 1957, The Geological Society of America, Inc.
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E.","contributorId":34573,"corporation":false,"usgs":true,"family":"Mullens","given":"T.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":775317,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Freeman, V. L.","contributorId":52958,"corporation":false,"usgs":true,"family":"Freeman","given":"V.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":775318,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70213490,"text":"70213490 - 1957 - Discussion of “Application of the modified einstein procedure for computation of total sediment load”","interactions":[],"lastModifiedDate":"2020-09-17T20:50:43.190691","indexId":"70213490","displayToPublicDate":"1957-10-01T15:48:38","publicationYear":"1957","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"Discussion of “Application of the modified einstein procedure for computation of total sediment load”","docAbstract":"Basically, any theory consists of a set of assumptions and various conclusions which are logically derived therefrom. An assumption, as the term is to be used here, may be based on an observed fact or relationship, a definition, an undefined (but generally accepted and understood) concept; or it may be based on a postulated relationship which has not been observed and may not even be directly observable. The conclusions of a theory in the physical sciences are, of course, intended to agree with and to predict observable facts. If a theory does not thus coincide with reality, it is eminently proper to examine the assumptions and the logical structure of the theory and, if possible, to modify the assumptions or correct the logic so that the conclusions do agree with observed facts.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR038i005p00768","usgsCitation":"Schroeder, K.B., and Hembree, C., 1957, Discussion of “Application of the modified einstein procedure for computation of total sediment load”: Eos, Transactions, American Geophysical Union, v. 38, no. 5, p. 768-773, https://doi.org/10.1029/TR038i005p00768.","productDescription":"6 p.","startPage":"768","endPage":"773","costCenters":[],"links":[{"id":378547,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"38","issue":"5","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Schroeder, K. B.","contributorId":240920,"corporation":false,"usgs":false,"family":"Schroeder","given":"K.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":799134,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hembree, C. H.","contributorId":106866,"corporation":false,"usgs":true,"family":"Hembree","given":"C. H.","affiliations":[],"preferred":false,"id":799135,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}