Le stéréorestituteur Kelsh est un appareil de restitution à double projection basé sur le principe des anaglyphes, comme le Multiplex par exemple, mais il a une plus grande précision que ce dernier, vu que les négatifs sont utilisés directement pour la restitution, sans que l'on soit obligé de les réduire au préalable. Une telle solution devient possible lorsque l'échelle de l'image plastique (modèle) est au moins 7 fois plus grande que celle des clichés. L'appareil comprend un support reposant par 4 pieds sur la table à dessin. Sa partie supérieure porte, par l'intermédiaire de trois vis calantes, un cadre dans lequel les deux chambres de projection sont suspendues. Des leviers de commande, agissant sur les chambres, permettent d'introduire la base, le déversement et les inclinaisons transversale et longitudinale. Les clichés conjugués ou des diapositifs sont directement placés dans les chambres de projection munies d'objectifs. En projetant les deux clichés au moyen de couleurs complémentaires, l'observateur — muni de lunettes à verres colorés (couleurs complémentaires) — observe l'image plastique audessus de la table à dessin, l'orientation relative des chambres ayant été établie au préalable. Pour le report des points de l'image plastique sur la minute, l'opérateur dispose d'une tablette amovible à marque-repère lumineuse qu'il déplace à la main et dont la hauteur au-dessus de la table à dessin peut être commandée par une molette. Pour établir l'orientation absolue de l'image plastique, il suffit d'incliner convenablement le cadre de suspension à l'aide des vis calantes, l'orientation relative n'étant pas détruite par cette opération.
Les deux clichés sont éclairés par des projecteurs munis d'une suspension à la cardan et reliés à la tablette de restitution par des tiges télescopiques. Moyennant ce dispositif, l'éclairage est concentré sur deux petites régions conjuguées des clichés et l'observateur ne voit ainsi qu'une petite partie de l'image spatiale, ce qui présente l'avantage de ne pas l'éblouir.
D'autre part, les tiges télescopiques impriment, suivant l'inclinaison, un déplacement vertical plus ou moins prononcé aux objectifs de projection, ce qui permet d'éliminer les erreurs de distorsion.
Pour les travaux de triangulation aérienne, l'auteur propose d'appliquer la méthode des plaques à fontes radiales (templets). Pour le passage d'un modèle à l'autre, l'orientation spatiale des chambres de restitution est déterminée au moyen d'une nivelle placée sur les clichés. Un premier essai a été effectué sur 7 modèles (échelle des clichés 1/34000) et après compensation l'erreur probable altimétrique des douze points connus s'est élevée à 1.50 m tandis que l'erreur maximum était de 4 m.
L'erreur altimétrique des restitutions effectuées par le U.S. Forest Service en Californie avec des clichés ou 1/48000, où les différences de niveau dépassaient parfois 600 m par cliché, varie entre 1 m et 2.70 m.
","language":"French","publisher":"Elsevier","doi":"10.1016/S0031-8663(49)80041-X","usgsCitation":"Kelsh, H.T., 1949, Le stereorestituteur Kelsh: Photogrammetria, v. 6, no. C, https://doi.org/10.1016/S0031-8663(49)80041-X.","productDescription":"1 p.","startPage":"123","costCenters":[],"links":[{"id":219654,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"6","issue":"C","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a4596e4b0c8380cd67428","contributors":{"authors":[{"text":"Kelsh, H. T.","contributorId":39116,"corporation":false,"usgs":true,"family":"Kelsh","given":"H.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":357408,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":57080,"text":"ofr4817D - 1948 - Geology applied to modern highways","interactions":[{"subject":{"id":57080,"text":"ofr4817D - 1948 - Geology applied to modern highways","indexId":"ofr4817D","publicationYear":"1948","noYear":false,"chapter":"D","title":"Geology applied to modern highways"},"predicate":"IS_PART_OF","object":{"id":17787,"text":"ofr4817AE - 1948 - Translations of five French papers released","indexId":"ofr4817AE","publicationYear":"1948","noYear":false,"chapter":"A-E","title":"Translations of five French papers released"},"id":1}],"isPartOf":{"id":17787,"text":"ofr4817AE - 1948 - Translations of five French papers released","indexId":"ofr4817AE","publicationYear":"1948","noYear":false,"title":"Translations of five French papers released"},"lastModifiedDate":"2025-03-25T14:33:02.36769","indexId":"ofr4817D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1948","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":"48-17","chapter":"D","title":"Geology applied to modern highways","docAbstract":"\"Geology applied to modern highways\", by Leo Maddalena, is a study of the contribution of geologic work to the construction of a heavy-duty highway through rugged terrain in the Apennine Mountains of Italy.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr4817D","usgsCitation":"Maddalena, L., 1948, Geology applied to modern highways: U.S. Geological Survey Open-File Report 48-17, 10 p., https://doi.org/10.3133/ofr4817D.","productDescription":"10 p.","costCenters":[],"links":[{"id":184133,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1948/0017-d/report-thumb.jpg"},{"id":483776,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1948/0017-d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db683b33","contributors":{"authors":[{"text":"Maddalena, Leo","contributorId":83543,"corporation":false,"usgs":true,"family":"Maddalena","given":"Leo","email":"","affiliations":[],"preferred":false,"id":256232,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70215757,"text":"70215757 - 1948 - Some solutional features of the limestone near Lexington, Kentucky","interactions":[],"lastModifiedDate":"2020-10-28T19:58:10.057194","indexId":"70215757","displayToPublicDate":"1948-10-28T14:34:17","publicationYear":"1948","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Some solutional features of the limestone near Lexington, Kentucky","docAbstract":"Field work on the Ordovician limestones and shales of the Lexington area, Kentucky, has shown that no appreciable quantity of ground water is transmitted through interstitial openings in these rocks. Ground-water movement is restricted to joint planes and, to a lesser extent, bedding planes that have been enlarged by solution. Studies of these planes indicate that solution has been effective only to a limited depth below the land surface. The bottom of the solutional zone is an exaggerated replica of the land surface, showing a greater depth of the solutional zone below stream valleys. The greater depth is attributed to the greater accumulation of ground water, the dissolving agent, in those areas. Modifications of the ideal condition are effected by the less soluble beds and the configuration of the land surface.
The underground drainage systems of the area develop in a manner similar to rectilinear stream patterns, showing a definite alignment along the two joint sets of the area. Directional solution has taken place where one of these joint sets has been developed to the exclusion of the other.
","language":"English","publisher":"Society of Economic Geologist","doi":"10.2113/gsecongeo.43.1.39","usgsCitation":"Hamilton, D., 1948, Some solutional features of the limestone near Lexington, Kentucky: Economic Geology, v. 43, no. 1, p. 39-52, https://doi.org/10.2113/gsecongeo.43.1.39.","productDescription":"14 p.","startPage":"39","endPage":"52","costCenters":[],"links":[{"id":379896,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Kentucky","otherGeospatial":"Lexington","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -85.18798828125,\n 37.54893261064111\n ],\n [\n -83.75976562499999,\n 37.54893261064111\n ],\n [\n -83.75976562499999,\n 38.47939467327645\n ],\n [\n -85.18798828125,\n 38.47939467327645\n ],\n [\n -85.18798828125,\n 37.54893261064111\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"43","issue":"1","noUsgsAuthors":false,"publicationDate":"1948-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Hamilton, D.K.","contributorId":244110,"corporation":false,"usgs":false,"family":"Hamilton","given":"D.K.","email":"","affiliations":[],"preferred":false,"id":803313,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70215693,"text":"70215693 - 1948 - Geology and ground-water resources of Iwo Jima ","interactions":[],"lastModifiedDate":"2020-10-27T20:28:58.557427","indexId":"70215693","displayToPublicDate":"1948-10-27T15:01:22","publicationYear":"1948","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":"Geology and ground-water resources of Iwo Jima ","docAbstract":"Iwo Jima, in the western Pacific Ocean, consists of Motoyama, a broad volcanic cone, at the north, and Mt. Suribachi at the south, with an undulating isthmus between. Motoyama is largely light-gray-buff tuff. A thick andesitic lava flow under Suribachi, exposed in several places, is overlain by a thick deposit of cinder and scoria. The isthmus (called Tidorigahara by the Japanese) is underlain by more than 200 feet of loose black volcanic ash and fine cinder derived from Suribachi. Several small coral reefs are located about 340 and 110 feet above present sea level.
Iwo Jima first came into existence, probably early in Pleistocene time, with the building above sea level of the tuff cone of Motoyama. Quite late in the active life of Motoyama, volcanic activity on the southwestern flank resulted in the formation of Suribachi. This activity may have started with the welling up of the andesitic lava which underlies Suribachi. Following the major eruption of Suribachi, relative sea level changed, and the sea stood about 360 feet higher than at present. The broad cone of Motoyama was beveled; the relative sea level then dropped 240 feet, with minor halts to about 120 feet above present level. As the island rose, Suribachi burst forth in its last stage of explosive activity. Wave erosion cut deeply into the andesite flow of Suribachi, and a prominent bench level was formed 120 feet above present sea level.
The Japanese on the island were often faced with serious water shortages. Americans drilled wells and obtained moderately large supplies of usable water. The temperature of the water ranges from 105° to 179° F., and the water is somewhat mineralized. The most favorable area for ground-water development is the isthmus.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1948)59[995:GAGROI]2.0.CO;2","usgsCitation":"Swenson, F.A., 1948, Geology and ground-water resources of Iwo Jima : GSA Bulletin, v. 59, no. 10, p. 995-1008, https://doi.org/10.1130/0016-7606(1948)59[995:GAGROI]2.0.CO;2.","productDescription":"14 p.","startPage":"995","endPage":"1008","costCenters":[],"links":[{"id":379832,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Japan","otherGeospatial":"Iwo Jima","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n 141.251220703125,\n 24.693814995267424\n ],\n [\n 141.4057159423828,\n 24.693814995267424\n ],\n [\n 141.4057159423828,\n 24.85092688067188\n ],\n [\n 141.251220703125,\n 24.85092688067188\n ],\n [\n 141.251220703125,\n 24.693814995267424\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"59","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Swenson, F. A.","contributorId":71622,"corporation":false,"usgs":true,"family":"Swenson","given":"F.","email":"","middleInitial":"A.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":803152,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70215690,"text":"70215690 - 1948 - Precedence of modern plant names over names based on fossils","interactions":[],"lastModifiedDate":"2021-03-25T21:18:38.284594","indexId":"70215690","displayToPublicDate":"1948-10-27T14:24:46","publicationYear":"1948","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Precedence of modern plant names over names based on fossils","docAbstract":"No abstract available.
","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.108.2809.483","usgsCitation":"Schopf, J., 1948, Precedence of modern plant names over names based on fossils: Science, v. 108, no. 2809, https://doi.org/10.1126/science.108.2809.483.","productDescription":"1 p.","startPage":"483","costCenters":[],"links":[{"id":379830,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"108","issue":"2809","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Schopf, James M.","contributorId":94297,"corporation":false,"usgs":true,"family":"Schopf","given":"James M.","affiliations":[],"preferred":false,"id":803148,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70215681,"text":"70215681 - 1948 - Runoff from rain and snow","interactions":[],"lastModifiedDate":"2021-04-02T14:46:48.221141","indexId":"70215681","displayToPublicDate":"1948-10-27T12:31:09","publicationYear":"1948","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":"Runoff from rain and snow","docAbstract":"The basic principles of the idealized hydrologic cycle are reviewed with emphasis on storage and movement of water in the soil. A distinction is made between ground‐water runoff and overland runoff in terms of storage and lag, expressed as accumulated deviations from uniform flow over a period of several years. These functions are presented for the period 1920 through 1945 for three rivers in central Oregon: John Day, Deschutes, and Metolius, which exemplify minimum, moderate, and maximum effects, respectively, of storage and lag. The Metolius River is shown to have extremely small fluctuations in discharge from year to year, ascribed to a great portion of its flow being derived from ground‐water runoff; and its response to fluctuations in annual precipitation lags behind that of the John Day River by about five years. Specific techniques and measures for improving seasonal water supply forecasts are suggested.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR029i004p00511","usgsCitation":"Piper, A.M., 1948, Runoff from rain and snow: Eos, Transactions, American Geophysical Union, v. 29, no. 4, p. 511-524, https://doi.org/10.1029/TR029i004p00511.","productDescription":"14 p.","startPage":"511","endPage":"524","costCenters":[],"links":[{"id":379816,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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\"}}]}","volume":"29","issue":"4","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Piper, A. M.","contributorId":102865,"corporation":false,"usgs":true,"family":"Piper","given":"A.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":803140,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70215627,"text":"70215627 - 1948 - Geology and ground water of the Casablanca Basin, Chile","interactions":[],"lastModifiedDate":"2021-03-25T16:14:57.539396","indexId":"70215627","displayToPublicDate":"1948-10-26T13:32:37","publicationYear":"1948","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Geology and ground water of the Casablanca Basin, Chile","docAbstract":"\"In the uplands the Cretaceous granodiorite and granite contain water in the weathered zones, and in joints and fractures. These yield small supplies of good water to springs and to shallow domestic and stock wells. The alluvial fill of the lowlands contains a zone of saturation that is sustained by infiltration from rainfall and from the runoff of the uplands.... Where present in the zone of saturation, the coarse-grained members of the alluvial fill yield moderate to large supplies of good water to wells.\"
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.43.8.661","usgsCitation":"Taylor, G.C., 1948, Geology and ground water of the Casablanca Basin, Chile: Economic Geology, v. 73, no. 8, p. 661-674, https://doi.org/10.2113/gsecongeo.43.8.661.","productDescription":"14 p.","startPage":"661","endPage":"674","costCenters":[],"links":[{"id":379771,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Chile","otherGeospatial":"Casablanca Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -71.7791748046875,\n -34.25267611710151\n ],\n [\n -69.71923828125,\n -34.25267611710151\n ],\n [\n -69.71923828125,\n -32.65787573695528\n ],\n [\n -71.7791748046875,\n -32.65787573695528\n ],\n [\n -71.7791748046875,\n -34.25267611710151\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"73","issue":"8","noUsgsAuthors":false,"publicationDate":"1948-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Taylor, G. C. Jr.","contributorId":21628,"corporation":false,"usgs":true,"family":"Taylor","given":"G.","suffix":"Jr.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":803033,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220009,"text":"70220009 - 1948 - Batholith and associated rocks of Corona, Elsinore, and San Luis Rey quadrangles southern California","interactions":[],"lastModifiedDate":"2021-04-16T18:00:29.823768","indexId":"70220009","displayToPublicDate":"1948-06-01T12:56:33","publicationYear":"1948","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1726,"text":"GSA Memoirs","active":true,"publicationSubtype":{"id":10}},"title":"Batholith and associated rocks of Corona, Elsinore, and San Luis Rey quadrangles southern California","docAbstract":"The batholith of Southern and Lower California is exposed continuously from near Riverside, California, southward for a distance of about 350 miles. In central Lower California it is covered in part by younger rocks, but discontinuous bodies extend to the southern end of Lower California, and hence the batholith is probably over 1000 miles long. Its width is about 60 miles. A strip across the northern part of the batholith about 70 miles wide has been studied; the western half was mapped in detail, and the eastern half was covered in rapid reconnaissance.
In the area studied the batholith intrudes Triassic sediments and Jurassic(?) volcanic rocks along its western border and Paleozoic sediments along its eastern border. Screens and roof pendants are common within the batholith. The Triassic rocks are mildly metamorphosed in the western part of the area but become progressively more coarsely crystalline toward the east. The Paleozoic rocks are rather coarsely crystalline. The metamorphism in large part preceded the intrusion of the batholith, and only locally was there appreciable contact metamorphism. The batholith and older rocks are overlain by Upper Cretaceous and younger sediments. Small bodies of andesite and basalt are associated with the Tertiary sediments, and small bodies of nepheline basalt of Quaternary age are present in the area. The batholith was intruded in early Upper Cretaceous time.
The batholith in the area studied was emplaced by over 20 separate injections. Most of the resulting rock types are found in only one or a few small bodies which are confined to a small area. In the area studied in detail (Pl. 1) five types are present in many large, widely separated bodies, making up about 88 per cent of the area underlain by the batholith. In the eastern half of the batholith three more widespread types are present. In the western half of the body the rocks range fro a gabbro to granite, but in the eastern half several tonalites constitute nearly the whole of the mass. The gabbro is composed of many related rocks. Some have hornblende, some pyroxene; in some the plagioclase is anorthite, in others it is as sodic as andesine-Iabradorite. Some of the tonalites contain abundant inclusions that have been almost completely reworked by the magma and have been softened and stretched into thin discs. These inclusions are well oriented and near the contacts with older rocks they parallel the contacts, but elsewhere they strike about N. 30° W. and dip steeply to the east. One tonalite, whose feldspar is andesine, has scattered crystals with cores of bytownite, and has well-crystallized hornblende with cores of pale uralitic hornblende and remnants of augite. Hornblende and biotite are the predominant mafic minerals of the tonalites and granodiorites. The iron content of the mafic minerals of the gabbros is moderate, and it increases as the rocks become richer in silica. The norms and the modes are shown on a variation diagram (Figs. 11, 12). The chemical analyses of the rocks fall near smooth variation curves (Fig. 4).
The general strike of the structures of the area have been about N. 30° W. from Paleozoic to the present time. The Paleozoic and Triassic sediments, the orientation of the inclusions and other structures of the batholith, the elongation of the batholith and the mountain ranges, and the strike of the major faults are in about the same direction. In the batholith and the older sediments the dips are steep to the east.
The batholith must have been emplaced by stoping and not by forceful injection. Calculations show that the cooling of a large batholith is chiefly through the roof and not through the walls. Crystallization to a depth of 3 kilometers takes place in about half a million years. The different rocks of the batholith were formed from the intermediate gabbro by crystal differentiation and assimilation in depth.
In early Upper Cretaceous time diastrophism folded the older rocks and formed, in depth, a strip of gabbroic magma about 1000 miles long. A small amount of this magma was intruded nearly to the surface. The deep magma differentiated quietly until its upper part attained the composition of a tonalite. Earth movements then occurred at least five times in rapid succession and caused the injection of the different tonalites. Some of these carry abundant inclusions, indicating a widespread shattering of the wall rock shortly before final emplacement. From time to time local movements caused the injections of the different granodiorites. When the deep-seated magma reached the composition of a light-colored granodiorite, widespread diastrophism moved the main granodiorite upward. Further local movement caused the emplacement of the many local granodiorites and granites.
","language":"English","publisher":"1948","doi":"10.1130/MEM29-p1","usgsCitation":"Larsen, E.S., 1948, Batholith and associated rocks of Corona, Elsinore, and San Luis Rey quadrangles southern California: GSA Memoirs, https://doi.org/10.1130/MEM29-p1.","costCenters":[],"links":[{"id":385170,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"southern California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121.77246093750001,\n 32.62087018318113\n ],\n [\n -114.169921875,\n 32.62087018318113\n ],\n [\n -114.169921875,\n 36.98500309285596\n ],\n [\n -121.77246093750001,\n 36.98500309285596\n ],\n [\n -121.77246093750001,\n 32.62087018318113\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationDate":"1948-06-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Larsen, Esper S. Jr.","contributorId":39029,"corporation":false,"usgs":true,"family":"Larsen","given":"Esper","suffix":"Jr.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":814427,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":55539,"text":"ofr4712 - 1947 - Geologic features of dam sites in the Nehalem, Rogue, and Willamette River basins, Oregon, 1935-37","interactions":[],"lastModifiedDate":"2014-07-09T11:04:03","indexId":"ofr4712","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1947","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":"47-12","title":"Geologic features of dam sites in the Nehalem, Rogue, and Willamette River basins, Oregon, 1935-37","docAbstract":"The present report comprises brief descriptions of geologic features at 19 potential dam sites in the Nehalem, Rogue, and Willamette River basins in western Oregon. The topography of these site and of the corresponding reservoir site was mapped in 1934-36 under an allocation of funds, by the Public Works Administration for river-utilization surveys by the Conservation Branch of the United States Geological Survey. The field program in Oregon has been under the immediate charge of R. O. Helland.
\nThe 19 dam sites are distributed as follows: three on the Nehalem River, on the west or Pacific slope of the Oregon Coast range; four on Little Butte Creek and two on Evans Creek, tributaries of the Rogue River in the eastern part of the Klamath Mountains; four on the South and Middle Santiam Rivers, tributaries of the Willamette River from the west slope of the Cascade mountains; and six on tributaries of the Willamette River from the east slope of the Coast Range.
\nExcept in the Evans Creek basin, all the rocks in the districts that were studied are of comparatively late geological age. They include volcanic rocks, crystalline rocks of several types, marine and nonmarine sedimentary rocks, and recent stream deposits.
\nThe study of geologic features has sought to estimate the bearing power and water-tightness of the rocks at each dam site, also to place rather broad limits on the type of dam for which the respective sites seem best suited. It was not considered necessary to study the corresponding reservoir sites in detail for excessive leakage appears to be unlikely. Except at three of the four site in the Santiam River basin, no test pits have been dug nor exploratory holes drilled, so that geologic features have been interpreted wholly from natural outcrops and from highway and railroad cuts. Because these outcrops and cuts are few, many problems related to the construction and maintenance of dams can not be answered at the this time and all critical features of the sites should be thoroughly explored by test pits and drilled holes before any dam is designed. This applied especially to sites in the Nehalem and Willamette River basins where commonly the cover of timber and brush is dense and the rocks are rather deeply weathered.
\nOn the Middle Santiam and South Santiam Rivers, the Cascadia, Greenpeter, and Sweet Home sits have been studies intensively by the United States Engineer Department, whose work included exploration by diamond-drill holes and test pits. Their conclusions as to geologic features are given in a report by McKitrick and have been reviewed by the writer. Data from this source have been used freely in the discussion of the respective sites in this report.
\nThe probability of destructive earthquakes in the region appears to be small but is not negligible. Prudence suggests that any high dam should embody features to assure stability against moderately strong earth motions.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr4712","usgsCitation":"Piper, A.M., 1947, Geologic features of dam sites in the Nehalem, Rogue, and Willamette River basins, Oregon, 1935-37: U.S. Geological Survey Open-File Report 47-12, Report: 111 p.; 10 plates: 10.24 x 7.98 inches, https://doi.org/10.3133/ofr4712.","productDescription":"Report: 111 p.; 10 plates: 10.24 x 7.98 inches","numberOfPages":"124","temporalStart":"1935-01-01","temporalEnd":"1937-12-31","costCenters":[],"links":[{"id":289620,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":289609,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-a-1.pdf"},{"id":289611,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-a-3.pdf"},{"id":289613,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-a-4.pdf"},{"id":289614,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-a-5.pdf"},{"id":289615,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-b-1.pdf"},{"id":289608,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1947/0012/report.pdf"},{"id":289612,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-a-2.pdf"},{"id":289616,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-c-1.pdf"},{"id":289617,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-c-2.pdf"},{"id":289618,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-d.pdf"},{"id":289619,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1947/0012/sheet-unnumbered.pdf"}],"country":"United States","state":"Oregon","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -123.261389,44.48366 ], [ -123.261389,44.754742 ], [ -123.071457,44.754742 ], [ -123.071457,44.48366 ], [ -123.261389,44.48366 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a28e4b07f02db610f46","contributors":{"authors":[{"text":"Piper, A. M.","contributorId":102865,"corporation":false,"usgs":true,"family":"Piper","given":"A.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":253663,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":69019,"text":"om68 - 1947 - Structure contour map of the surface rocks of the Model anticline, Las Animas County, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:13:53","indexId":"om68","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1947","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":329,"text":"Oil and Gas Investigation Map","code":"OM","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"68","title":"Structure contour map of the surface rocks of the Model anticline, Las Animas County, Colorado","language":"ENGLISH","doi":"10.3133/om68","usgsCitation":"Bass, N., Straub, C., and Woodbury, H., 1947, Structure contour map of the surface rocks of the Model anticline, Las Animas County, Colorado: U.S. Geological Survey Oil and Gas Investigation Map 68, 1 map ;107 x 81 cm., https://doi.org/10.3133/om68.","productDescription":"1 map ;107 x 81 cm.","costCenters":[],"links":[{"id":105050,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_5428.htm","linkFileType":{"id":5,"text":"html"},"description":"5428"},{"id":191127,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"scale":"42240","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b0ee4b07f02db6a002d","contributors":{"authors":[{"text":"Bass, N. W.","contributorId":104867,"corporation":false,"usgs":true,"family":"Bass","given":"N. W.","affiliations":[],"preferred":false,"id":279396,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Straub, C.E.","contributorId":78827,"corporation":false,"usgs":true,"family":"Straub","given":"C.E.","email":"","affiliations":[],"preferred":false,"id":279394,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Woodbury, H.O.","contributorId":101752,"corporation":false,"usgs":true,"family":"Woodbury","given":"H.O.","email":"","affiliations":[],"preferred":false,"id":279395,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":57076,"text":"ofr481 - 1947 - Cobalt-copper deposits of the Blackbird district, Lemhi County, Idaho","interactions":[{"subject":{"id":57076,"text":"ofr481 - 1947 - Cobalt-copper deposits of the Blackbird district, Lemhi County, Idaho","indexId":"ofr481","publicationYear":"1947","noYear":false,"title":"Cobalt-copper deposits of the Blackbird district, Lemhi County, Idaho"},"predicate":"SUPERSEDED_BY","object":{"id":70046714,"text":"70046714 - 1948 - Cobalt-copper deposits in the Blackbird district, Lemhi County, Idaho","indexId":"70046714","publicationYear":"1948","noYear":false,"title":"Cobalt-copper deposits in the Blackbird district, Lemhi County, Idaho"},"id":1}],"supersededBy":{"id":70046714,"text":"70046714 - 1948 - Cobalt-copper deposits in the Blackbird district, Lemhi County, Idaho","indexId":"70046714","publicationYear":"1948","noYear":false,"title":"Cobalt-copper deposits in the Blackbird district, Lemhi County, Idaho"},"lastModifiedDate":"2015-01-13T12:35:21","indexId":"ofr481","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1947","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":"48-1","title":"Cobalt-copper deposits of the Blackbird district, Lemhi County, Idaho","docAbstract":"The Blackbird district is in east-central Idaho, about 20 miles west-southwest of Salmon. The area is one of deeply weathered, flat-topped upland surfaces cut by several steep-walled valleys, which are tributary to the canyon of Panther Creek. Most of the area has a heavy vegetative cover and outcrops are relatively scarce except in the walls of the steeper valleys. The rocks of the district consist mostly of metamorphosed sedimentary rocks of the pre-Cambrian Yellowjacket formation (Belt series); a part of the Cretaceous Idaho batholith cuts across the northern part of the district, and acid porphyry dikes and metamorphosed basic rocks cut the Yellowjacket rocks.
\nStructurally, the sedimentary rocks are divided by faults into three, roughly north-south blocks. The center one (Blackbird structural block) appears to have been more tightly squeezed than the others into relatively tight folds, with the development of widespread schistosity (flow cleavage). The rocks of the two outside blocks are in more open folds. In general they are nonschistose, except for the north end of the western block, where there are schistose rocks cut by several north-dipping thrust faults. The northern parts of the central and western blocks contain considerable garnet, chloritoid, and cordierite.
\nThe Blackbird structural block is cut by a number of mineralized shear zones. Those dipping moderately northeast and striking northwest, and those dipping steeply and striking north and northeast; appear to be most important. The mineralized rock contains chalcopyrite, cobaltite, pyrite, and pyrrhotite into a gangue of quartz, biotite, tourmaline, ankerite, and muscovite; the deposits were formed mostly by replacement of the shear zones. In addition, the block is cut by north-dipping thrust faults of west to northwest strike, and a number of high-angle faults.
\nThe district was first prospected about 1893; considerable developmont was done at the Brown Bear mine in 1899-1902, at the Haynes-Stellite in l917-1920, and at the Uncle Sam mine in 1938-1941, During World War II, the U.S. Bureau of Mines explored in the district with bulldozer and diamond drill., and the U.S. Geological Survey mapped the district and logged the drill cores. The Howe Sound Co. also did some diamond drilling in the district, and in 1945 the Calera Mining Co., Blackbird Division (subsidiary of Howe Sound Co.), started underground development at the Calera adit. Although the district has had very little production to the present, it is believed that a large tonnage of copper-cobalt ore exists in the district which should permit mining to be continued over a long period.
\nThe report contains brief descriptions of all the accessible workings in the district, of which the most important are Calera, Brown Bear, Uncle Sam, and Hawkeye mines. In the Calera adit, about 1,700 feet of the mineralized zone, ranging in width from 3 feet to 40 feet and averaging about 15 feet; have been explored (August 1946); the zone lies on a wide northwest-striking shear zone dipping moderately ( 60° ±) northeast. The Brown Bear adit is in a wide, mineralized, north-south shear zone in which are higher-grade pods plunging 25° to 35° north. The Uncle Sam mine explores a relatively narrow north-south shear zone in which are two or three north-plunging ore shoots. The Hawkeye mine is in a broad zone of mineralized schist in which are several north-plunging lenses of ore.
","language":"English","doi":"10.3133/ofr481","usgsCitation":"Vhay, J.S., 1947, Cobalt-copper deposits of the Blackbird district, Lemhi County, Idaho (Superseded by: Strategic Minerals Investigations Preliminary Map 3-219): U.S. Geological Survey Open-File Report 48-1, ii, 26 p., https://doi.org/10.3133/ofr481.","productDescription":"ii, 26 p.","numberOfPages":"38","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":184048,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":297131,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/1948/0001/"},{"id":297132,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1948/0001/downloads/ofr48-1.pdf","text":"Report","size":"10.5 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Idaho","county":"Lemhi County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -115.01586914062499,\n 44.1151978766043\n ],\n [\n -115.01586914062499,\n 45.729191061299936\n ],\n [\n -112.78564453124999,\n 45.729191061299936\n ],\n [\n -112.78564453124999,\n 44.1151978766043\n ],\n [\n -115.01586914062499,\n 44.1151978766043\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Superseded by: Strategic Minerals Investigations Preliminary Map 3-219","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6ae9c9","contributors":{"authors":[{"text":"Vhay, J. S.","contributorId":78752,"corporation":false,"usgs":true,"family":"Vhay","given":"J.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":256224,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":33652,"text":"b944B - 1947 - Geology of the lead-silver deposits of the Clark Fork district, Bonner County, Idaho","interactions":[],"lastModifiedDate":"2024-09-19T18:27:24.211257","indexId":"b944B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1947","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"944","chapter":"B","title":"Geology of the lead-silver deposits of the Clark Fork district, Bonner County, Idaho","docAbstract":"This report gives the results of a reinvestigation of the lead-silver deposits of the Clark Fork district, Bonner County, Idaho, which since the late twenties have been the most important producers of lead-silver ore in northern Idaho outside of the Coeur d'Alene district, their production up to the end of 1941 having been more than $1,200,000.
The deposits closely resemble those in the Coeur d'Alene district. They are fillings and replacements along minor low-angle thrust and high-angle reverse faults, which genetically are related to the Hope fault, a great transverse earth fracture, which provides the same sort of structural background for this district that the famous Osburn fault does for the Coeur d'Alene district. The deposits are contained in the Wallace and Striped Peak formations, members of the pre-Cambrian Belt series, and are closely associated with faulting and igneous activity that is probably of early Tertiary age.
The mineralization has not been so extensive as in the Coeur d'Alene district, but the deposits, though comparatively small, are rich. Much of the ore is in compact seams and lenses a few inches thick, but stringers of ore and subordinate fractures along which grains of sulfide are disseminated extend across zones that are commonly 2 to 4 feet and exceptionally as much as 8 feet in width. The ore is mainly sulfide ore of the Coeur d'Alene type, consisting dominantly of galena, which is accompanied by lesser quantities of siderite, quartz, and sphalerite and by still smaller quantities of pyrite, arsenopyrite, tetrahedrite, and calcite. Some of the deposits, however, have been substantially enriched by the addition of hypogene silver and antimony minerals, so that much of the ore being mined has a higher silver content than any of that in the Coeur d'Alene district. The hypogene minerals include lead sulfantimonites and sulfarsenites, copper-lead sulfantimonites, and ruby silver. These minerals are absent from only one of the mines, and in one of the mines they form the bulk of the ore that is now being taken out. The high silver content of some of the ore is due in part to the presence of pyrargyrite (3Ag2S.SbS:4).
The deposits apparently were formed at moderate depths and at moderate temperatures. It is believed that the ore will persist to depths appreciably greater than those yet reached in mining. The district has not yet been adequately explored, and undiscovered ore bodies may remain hidden beneath glacial and other surface debris.
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b944B","usgsCitation":"Anderson, A., 1947, Geology of the lead-silver deposits of the Clark Fork district, Bonner County, Idaho: U.S. Geological Survey Bulletin 944, Report: v, p. 37-117; 8 Plates: 29.32 x 32.40 inches or smaller, https://doi.org/10.3133/b944B.","productDescription":"Report: v, p. 37-117; 8 Plates: 29.32 x 32.40 inches or smaller","costCenters":[],"links":[{"id":96047,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0944b/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":96046,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0944b/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":96045,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0944b/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":96044,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0944b/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":96043,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0944b/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":96042,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0944b/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":96041,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0944b/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":96040,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/0944b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":164033,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/0944b/report-thumb.jpg"},{"id":109591,"rank":11,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21183.htm","linkFileType":{"id":5,"text":"html"},"description":"21183"},{"id":96048,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/0944b/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho","county":"Bonner County","otherGeospatial":"Clark Fork district","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -117.03112507202923,\n 48.92545075150298\n ],\n [\n -117.03112507202923,\n 47.667570923980435\n ],\n [\n -116.05716289240691,\n 47.667570923980435\n ],\n [\n -116.05716289240691,\n 48.92545075150298\n ],\n [\n -117.03112507202923,\n 48.92545075150298\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c833","contributors":{"authors":[{"text":"Anderson, Alfred Leonard","contributorId":54646,"corporation":false,"usgs":true,"family":"Anderson","given":"Alfred Leonard","affiliations":[],"preferred":false,"id":211729,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70210288,"text":"70210288 - 1947 - Part 3: Volcano investigations on Umnak Island, 1946","interactions":[],"lastModifiedDate":"2022-05-24T20:32:04.864101","indexId":"70210288","displayToPublicDate":"1947-12-31T14:32:41","publicationYear":"1947","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"title":"Part 3: Volcano investigations on Umnak Island, 1946","docAbstract":"Umnak Island is a dumbbell-shaped island in the eastern part of the Aleutian Islands. The island is 70 miles long and trends northeast-southwest. During 1946 volcano investigations were begun on the island and geologic mapping of most of northeastern Umnak Island was completed.
Okmok Volcano, a large, broad volcanic mountain rising to altitudes of 3,000 to 3,500 feet, occupies the central portion of northeastern Umnak Island. Fort Glenn, and Army airbase, is situated on the eastern end of the island, approximately 9 miles east of Okmok Volcano.
The central part of Okmok Volcano is indented by Okmok caldera, a large cliff-rimmed volcanic depression, 7%, miles in maximum diameter. The floor of the caldera is 1,500 to 2,500 feet below the caldera rim. Nine large cinder cones and many small ones lie on the caldera floor, chiefly along two arcuate zones. The caldera is drained by Crater Creek, which flows through a deep gorge cut in the northeastern wall of the caldera, and into Bering Sea.
Mount Tulik (4,111 feet altitude) and Mount Idak (1,918 feet altitude) arc important centers of ancient volcanism on the flanks of Okmok Volcano.
The geologic history of Okmok Volcano falls into three stages: The first includes the upbuilding of an ancient cone—Mount Okmok—to an altitude of at least 6;500 feet on the site of the present caldera; the second encompasses the destruction in a castastrophic eruption of the summit cone and the formation of the caldera; the third comprises events since the great eruption.
The earliest activity at Mount Okmok probably dates hack to the late Tertiary period. A composite cone, concave-sided in profile, was built by the alternate eruption of ash, coarse pyroclastics, and basalt flows. During the late Pleistocene, volcanic activity at Mount Okmok was greatly reduced and a topography of late youth was carved on the lower slopes by streams and valley glaciers. The summit of Mount Okmok was upwarped and dikes and necks were injected into the resulting fractures.
A large volcano at the site of Mount Idak was active during part of the period of upbuilding at Mount Okmok but became extinct during the middle Pleistocene. A parasitic vent, Mount Tulik, became active during the late Pleistocene and built a steep-sided cone before it became extinct, shortly before the formation of Okmok caldera.
A cataclysmic eruption terminated the period of dissection at Mount Okmok, 10,000 or more years ago. Part of the summit was blown away by the explosive violence of this eruption. Nuees ardentes (glowing clouds) and mudflows deposited tuff-breccia and agglomerate in the glacial valleys; later phases of the eruption blanketed the landscape with ash. Near the end of the eruption, the remaining upper part of the volcano collapsed along arcuate fractures: large blocks subsided several thousand feet and are now concealed in the caldera Poor beneath later deposits. A large arcuate fault block which subsided less than other blocks stands above the floor in the northeastern part of the caldera.
After the eruption, water collected in the caldera, forming a lake. Small but frequently active cones built islands in the lake and covered its bottom with pyroclastic debris. The lake eventually overflowed the lowest point in the rim of the caldera, and Crater Creek Gorge was carved, draining the lake and dissecting its deposits. Renewed movement along faults at the head of Crater Creek Gorge later raised a harrier which temporarily dammed the drainage and formed a second caldera lake.
Readjustments among subsided blocks in the caldera floor resulted in the folding of postcaldera deposits at several localities.
Much of the caldera floor has been covered by lava flows extruded from several cones since the draining of the first caldera lake. In general, however, volcanic activity seems to have declined since the great caldera-forming eruption. Seven eruptions from cones on the caldera floor have been recorded since 1817; the latest occurred in 1945.
As part of the geochemical program for the study of Okmok Volcano, temperatures of fumaroles were measured and samples of the products of the volcanic activity were analyzed. Average temperatures of fumaroles at one source of the 1945 lava low dropped from 320° C. on July 19 to 90° C. on September 5. The temperatures of fumaroles associated with the crater vents on both Cones A and C ranged from 95° C. to 97\" C., which is slightly below the condensation point of steam, indicating the presence of minor quantities of gases other than steam. The magmatic gases of fumaroles on Cone A consisted of carbon dioxide and sulfur dioxide in about equal amounts. The lack of halogen acid gases in the fumaroles and the steadily dropping temperatures arc interpreted as indicating that the present quiescence of Cone A will continue for many months. Solid reaction products from areas of fumarolic activity on Cone A are sulfates of sodium, calcium, and iron. The presence of hydrogen sulfide as the dominant sulfur gas at Cone C is interpreted as indicating the dying stages of the present cycle of activity of Cone C.
Thermal springs along the north base of Cone D have a total discharge of 115 cubic feet per second. Their average temperature is approximately 7° C. above the annual mean. From these figures it is calculated that about 21,000 kilogram calories per second are being given off by Cone D. The spring waters contain minute quantities of boron which is indicative of a magmatic source for a small part of the water. Hence, Cone D though quiescent is not extinct. Evidence is presented to show that most of the spring water from Cone D is meteoric in origin.
Thermal waters in the southwestern part of Umnak Island at Hot Springs Cove and south of Geyser Bight contain lithium, boron, arsenic, and antimony in solution. These elements are regarded as derived from underlying magmas that are in an advanced state of crystallization and hence not likely to give rise in the near future to large-scale volcanic activity.
Three portable seismographs were placed on the flanks of Okmok Volcano and were in operation during most of the period from June 1 to October 1. During this period several slight tremors and one moderate tremor, all of distant origin, were registered, but no tremors attributable to Okmok Volcano were recorded. The lack of tremor records, however, may have been due more to the insensitivity of the instruments than to the absence of tremors.
Earth-current investigations were carried on during August and September by comparison of records obtained from a base station at Fort Glenn with those from a station 1 V2 miles southwest of Mount Tulik. The records obtained indicate that no difference in magnitude or direction of earth currents existed between the Fort Glenn and Mount Tulik areas. The similarity of record obtained is indicative of the absence of a disturbing factor such as a large body of live magma beneath Okmok Volcano.
Future eruptions of Okmok Volcano are expected to he of mild to moderate intensity, and will he chiefly in the form of ash falls from vents inside the caldera. There would be a great menace—in the form of lava flows, nuees ardentes, and mudflows—to installations at Fort Glenn if a new center of volcanism came into existence on the east slope of Okmok Volcano. Small postcaldera cones now exposed there indicate that extra-caldera eruptions have occurred in the recent past and can be expected in the future. The possibility of another catastrophic eruption of the caldera-forming type, however, is remote.
Okmok Volcano should be kept under close observation, partly because of its possible threat to Fort Glenn and partly because it is a readily accessible locale for accumulating information on details of volcanic processes, applicable to other volcanoes in the Aleutian arc and elsewhere.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Alaskan Volcano Investigations Report No. 2","largerWorkSubtype":{"id":6,"text":"USGS Unnumbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/70210288","usgsCitation":"Byers, F., Hopkins, D., Wier, K.L., and Fisher, B., 1947, Part 3: Volcano investigations on Umnak Island, 1946, 35 p., https://doi.org/10.3133/70210288.","productDescription":"35 p.","startPage":"19","endPage":"53","costCenters":[],"links":[{"id":401002,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70210288/report.pdf"},{"id":396452,"rank":1,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_93423.htm"},{"id":396453,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70210288/report-thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Umnak Island","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -168.84063720703125,\n 52.855864177853974\n ],\n [\n -167.81341552734375,\n 53.38824275010831\n ],\n [\n -167.772216796875,\n 53.533778184257805\n ],\n [\n -167.98095703125,\n 53.571307377413326\n ],\n [\n -168.4039306640625,\n 53.48477702972815\n ],\n [\n -168.4423828125,\n 53.31282653094477\n ],\n [\n -168.60992431640625,\n 53.28984728016674\n ],\n [\n -168.82415771484375,\n 53.15665305315798\n ],\n [\n -168.85162353515625,\n 53.04616682440388\n ],\n [\n -169.04937744140625,\n 52.908902047770255\n ],\n [\n -169.11529541015625,\n 52.82434224121616\n ],\n [\n -168.84063720703125,\n 52.855864177853974\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Byers, F. M. Jr.","contributorId":270390,"corporation":false,"usgs":false,"family":"Byers","given":"F. M.","suffix":"Jr.","affiliations":[],"preferred":false,"id":835996,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hopkins, D.M.","contributorId":103646,"corporation":false,"usgs":true,"family":"Hopkins","given":"D.M.","email":"","affiliations":[],"preferred":false,"id":835997,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wier, K. L.","contributorId":106864,"corporation":false,"usgs":true,"family":"Wier","given":"K.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":835998,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Fisher, Bernard","contributorId":280071,"corporation":false,"usgs":false,"family":"Fisher","given":"Bernard","email":"","affiliations":[],"preferred":false,"id":835999,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70214504,"text":"70214504 - 1947 - Chemical analyses and calculated modes of the Oliverian magma series, Mt. Washington Quadrangle, New Hampshire ","interactions":[],"lastModifiedDate":"2020-09-28T18:27:42.269761","indexId":"70214504","displayToPublicDate":"1947-09-28T13:18:23","publicationYear":"1947","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":"Chemical analyses and calculated modes of the Oliverian magma series, Mt. Washington Quadrangle, New Hampshire ","docAbstract":"Complete chemical analyses, including the spectrographic determination of 44 trace elements, have been made of six representative specimens from each of the six map units constituting the Oliverian magma series in the Mt. Washington quadrangle of New Hampshire. Potash is systematically higher than soda. An increase in silica, which ranges from 56 to 75 per cent, is accompanied by the usual variation of the other principal oxides; lime, magnesia, and total iron decrease in the more siliceous rocks, whereas potash and soda increase at first and then decline. Potash is 1.5 to 3 per cent higher than soda throughout the series.
With increasing silica content Cr2O3, NiO, SrO, V2O5, and BaO decrease, but ZnO increases. Comparisons with other parts of the world, especially northwestern Europe, suggest some systematic differences from New Hampshire, but the data are insufficient to justify any definite conclusions.
The calculation of modes from the chemical analyses necessitates a discussion of the methods involved and the possible errors. It is believed that in these rocks the modes can be calculated with relatively small errors. An unexplained excess of alumina in the modes, ranging from 0.0 to 1.0 per cent, may be due to more sericite and clay minerals in the rocks than the content of water suggests.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1947)58[573:CAACMO]2.0.CO;2","usgsCitation":"Billings, M., and Rabbitt, J., 1947, Chemical analyses and calculated modes of the Oliverian magma series, Mt. Washington Quadrangle, New Hampshire : GSA Bulletin, v. 58, no. 7, p. 573-596, https://doi.org/10.1130/0016-7606(1947)58[573:CAACMO]2.0.CO;2.","productDescription":"24 p.","startPage":"573","endPage":"596","costCenters":[],"links":[{"id":378820,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Hampsire","otherGeospatial":"Mt. Washington Quadrangle","volume":"58","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Billings, M.P.","contributorId":42948,"corporation":false,"usgs":true,"family":"Billings","given":"M.P.","email":"","affiliations":[],"preferred":false,"id":799750,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rabbitt, J.C.","contributorId":83998,"corporation":false,"usgs":true,"family":"Rabbitt","given":"J.C.","email":"","affiliations":[],"preferred":false,"id":799751,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70214503,"text":"70214503 - 1947 - Geology of the Borah Peak quadrangle, Idaho ","interactions":[],"lastModifiedDate":"2021-05-16T14:51:55.897612","indexId":"70214503","displayToPublicDate":"1947-09-28T13:00:33","publicationYear":"1947","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":"Geology of the Borah Peak quadrangle, Idaho ","docAbstract":"This report is on result of a long program of geologic investigation in south-central Idaho, undertaken as an aid in the development of the mineral resources of the region. This quadrangle was examined because of the exceptional opportunities for the study of stratigraphy and structure afforded by the Lost River Range, which is the highest in Idaho and contains comparatively few intrusive igneous rocks.
The Borah Peak quadrangle differs from the region to the west and northwest in that it contains parts of two sharply defined, narrow ranges elongated in a north-westerly direction, instead of broad, irregular mountain masses, in which the trends of most local topographic units are ill-defined. These ranges, the Lost River and the Lemhi, are flanked by intermontane valleys sparsely populated by stock ranchers.
The Lemhi and Swauger quartzites, regarded as of Belt (pre-Cambrian) age, are named. The two Cambrian (?) formations of the Bayhorse region are not recognized in this quadrangle. The Ramshorn slate (Lower Ordovician), widespread and thick there, does not appear to be exposed anywhere in the Borah Peak quadrangle with the possible exception of small areas east of the Elkhorn Ranch, where relations are obscure. The higher Paleozoic formations, named in order of decreasing age, are the Kinnikinic quartzite, Saturday Mountain formation, Laketown dolomite, Jefferson dolomite, Grand View dolomite, Three Forks limestone, Milligen formation, Brazer limestone, and Wood River formation. The Three Forks limestone, nowhere much over 250 feet thick, is the only one of these not recognized farther west. It provides substantial aid in the interpretation of upper Paleozoic stratigraphy. Equivalent beds to the west are presumably grouped with the Milligen. The grit that introduced uncertainties into the correlation of the Wood River and Milligen formations in the southeastern part of the Bayhorse quadrangle is absent here, and both formations have close lithologic resemblances to those in the type localities in the Wood River region. Wood River strata (Pennsylvanian) crop out only in the southwest corner of the quadrangle, and the Brazer may have been the last Paleozoic unit to be deposited over most of the area. Certainly it can have had comparatively little cover over it throughout the Mesozoic. The Brazer is regarded as Mississippian, but some of the fossils in it have Pennsylvania affinities. The carbonate rocks in the Three Forks and later formations are dominantly calcareous, while those in earlier units are dolomitic. Carbonaceous matter is present in most of the formations but is abundant only in the Milligen.
The Challis volcanics (Oligocene or Miocene) constitute the first stratified unit to be laid down after Paleozoic deposition ceased, although there was a little intrusive activity late in the Mesozoic. The volcanics were once widely distributed on the flanks of the mountains and are still plentiful in the northwestern corner of the quadrangle, near the head of the valley of the Pahsimeroi, and in smaller areas. They are neither so abundant nor so diversified as they are farther west. They are locally succeeded by an alluvial formation, here termed the Donkey fanglomerate, of possible Pliocene age. Abundant Quaternary glacial and alluvial deposits are present in the larger valleys.
The Lemhi and Swauger quartzites were broadly folded before Paleozoic sedimentation began. Apparently the later deformation affected them only enough to render the more impure beds somewhat schistose. The Paleozoic rocks have been folded into closely spaced, asymmetric anticlines, locally broken by thrusts at and near their crests. These folds approximately parallel the trends of the present range, whereas those in the old rocks strike more nearly north. Later deformation twisted some of the folds and produced thrusts of lower dip and greater extent. The folded rocks in the Lost River Range have been arched into an anticlinorium. The original, tight folds may have preceded the emplacement of the Idaho batholith farther west, while the anticlinorium and the late twists and low thrusts result from deformation during the long period in which the batholith came to place and adjusted itself. Local intricately contorted beds in the Brazer limestone are interpreted as the effects of flowage in calcareous material subjected to tangential pressure under comparatively light supercumbent load.
The quadrangle contains numerous normal faults of diverse trends. Most of those that can be conclusively demonstrated strike transverse to the trends of the ranges, but especially along parts of the southwest front of the Lemhi Range normal faults along the range fronts may have helped locally to guide erosion of the mountains. Some of the faults have displacements of thousands of feet and are thought to have originated in connection with the low-angle thrusts. Most of these, as well as minor breaks of diverse trends, affect also the Challis volcanics, which shows that renewed movement occurred in Tertiary time.
The present mountain masses and broad intermontane valleys are in about the positions occupied by similar features in the early Tertiary. Several incomplete erosion cycles since then have greatly modified the topography but have not obliterated the influence of these ancient land forms. The results of early episodes in the development of the topography are much obscured by the rugged forms that result from active Pleistocene glaciation and later vigorous stream erosion, but modified remnants of the post-Challis and Donkey Hills surfaces can be clearly distinguished. Several less widespread remnants mark intermediate steps in the process. Exceptionally abundant and permeable, coarse alluvial and glacial deposits floor intermontane valleys and choke the larger mountain gorges to such an extent as to interfere with normal erosion and make the surface-water supplies even scantier than might be expected from the climate of the region, which is moderately humid in the mountains and semiarid in the valleys. Active erosion in the high mountains and comparatively static conditions on fans at the range borders result in striking contrasts.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1947)58[1085:GOTBPQ]2.0.CO;2","usgsCitation":"Ross, C.P., 1947, Geology of the Borah Peak quadrangle, Idaho : GSA Bulletin, v. 58, no. 12, p. 1085-1160, https://doi.org/10.1130/0016-7606(1947)58[1085:GOTBPQ]2.0.CO;2.","productDescription":"76 p.","startPage":"1085","endPage":"1160","costCenters":[],"links":[{"id":385661,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Idaho","otherGeospatial":"Borah Peak","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -114.98291015625,\n 43.54854811091286\n ],\n [\n -112.994384765625,\n 43.54854811091286\n ],\n [\n -112.994384765625,\n 45.359865333959746\n ],\n [\n -114.98291015625,\n 45.359865333959746\n ],\n [\n -114.98291015625,\n 43.54854811091286\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"58","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Ross, C. P.","contributorId":91545,"corporation":false,"usgs":true,"family":"Ross","given":"C.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":799749,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70206576,"text":"70206576 - 1947 - Geology and ground-water resources of Puerto Rico","interactions":[],"lastModifiedDate":"2024-09-24T18:39:51.739246","indexId":"70206576","displayToPublicDate":"1947-09-01T09:29:09","publicationYear":"1947","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Geology and ground-water resources of Puerto Rico","docAbstract":"Puerto Rico, the easternmost and smallest of the Greater Antilles, has an axis of deformed and metamorphosed volcanic rocks of Upper Cretaceous age, intruded by dioritic rocks during the Antillean revolution. The hard-rock core is flanked on the north and south by limestones and clastic rocks of late Oligocene and early Miocene age, which have been gently arched and uplifted. Similar rocks were deposited in late Miocene or early Pliocene time along the west coast. During the Quaternary the island has been separated from the other major Antillean islands by faulting and has been arched, uplifted, and tilted to the northeast. Alluvium and littoral deposits have partially filled the valleys and have formed coastal plains on the north and south. The Upper Cretaceous volcanic and associated rocks yield small supplies of water to wells in most places. The Tertiary limestones yield large supplies in some places on the north, south, and west coasts. The Quaternary sands and gravels are the most important aquifers. They yield about 200 million gallons a day to wells in the main south coastal plain alone. The water is used largely for irrigation. A total of perhaps 250 to 300 million gallons a day is pumped from wells in the island, and moderate to large additional supplies are available in some places.
","language":"English","publisher":"GeoScience World","doi":"10.2113/gsecongeo.42.6.563","usgsCitation":"McGuinness, C.L., 1947, Geology and ground-water resources of Puerto Rico: Economic Geology, v. 42, no. 6, p. 563-571, https://doi.org/10.2113/gsecongeo.42.6.563.","productDescription":"9 p.","startPage":"563","endPage":"571","costCenters":[],"links":[{"id":369106,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Puerto 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Rico\",\"nation\":\"USA \"}}]}","volume":"42","issue":"6","noUsgsAuthors":false,"publicationDate":"1947-09-01","publicationStatus":"PW","contributors":{"authors":[{"text":"McGuinness, Charles Lee","contributorId":101249,"corporation":false,"usgs":true,"family":"McGuinness","given":"Charles","email":"","middleInitial":"Lee","affiliations":[],"preferred":false,"id":775030,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220013,"text":"70220013 - 1947 - Radioactivity of the rocks of the batholith of southern California","interactions":[],"lastModifiedDate":"2021-04-16T18:06:53.0774","indexId":"70220013","displayToPublicDate":"1947-06-01T13:01:57","publicationYear":"1947","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":"Radioactivity of the rocks of the batholith of southern California","docAbstract":"Determination of radioactivity has been made on 43 rocks, carefully selected from the different mapped units of the complex Cretaceous batholith of Southern California; they range from gabbro to granite. The activity of the gabbro averages about 0.3 alphas/mg./hr., that of the tonalites, 0.8, the granodiorite 1.3, and the granites over 2.0. The activity of the average rock of the batholith is about 0.9 alphas/mg./hr. Most of the rocks have been analyzed, and modal compositions are given. The radioactivity and the percentages of K2O, SiO2 and PbO are plotted on a variation diagram. The variation curve for activity nearly parallels that for K2O, and the ratio of activity to K2O is about 0.5. The radioactivities of some rocks fall far from the variation curve, and degree of activity correlates with K2O content. A less-marked correlation between activity SiO2 and PbO was also noted. The K2O, SiO2, PbO, and radioactivity concentrate in the residual liquid during crystallization and differentiation. PbO follows K2O closely, as it is concentrated in the K2O minerals, but radioactivity is very low in the K2O minerals and is greatly concentrated in the accessory minerals.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1947)58[483:ROTROT]2.0.CO;2","usgsCitation":"Larsen, E.S., and Keevil, N., 1947, Radioactivity of the rocks of the batholith of southern California: GSA Bulletin, v. 58, no. 6, p. 483-494, https://doi.org/10.1130/0016-7606(1947)58[483:ROTROT]2.0.CO;2.","productDescription":"12 p.","startPage":"483","endPage":"494","costCenters":[],"links":[{"id":385171,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"southern California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121.77246093750001,\n 32.62087018318113\n ],\n [\n -114.169921875,\n 32.62087018318113\n ],\n [\n -114.169921875,\n 36.98500309285596\n ],\n [\n -121.77246093750001,\n 36.98500309285596\n ],\n [\n -121.77246093750001,\n 32.62087018318113\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"58","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Larsen, Esper S. Jr.","contributorId":39029,"corporation":false,"usgs":true,"family":"Larsen","given":"Esper","suffix":"Jr.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":814428,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Keevil, N.B.","contributorId":257511,"corporation":false,"usgs":false,"family":"Keevil","given":"N.B.","email":"","affiliations":[],"preferred":false,"id":814429,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70207425,"text":"70207425 - 1947 - Petrology and structure of the Moa Chromite district, Oriente Province, Cuba","interactions":[],"lastModifiedDate":"2019-12-19T10:02:19","indexId":"70207425","displayToPublicDate":"1947-04-30T10:00:04","publicationYear":"1947","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":"Petrology and structure of the Moa Chromite district, Oriente Province, Cuba","docAbstract":"Chromite deposits In the Moa district, on the north coast of Oriente Province, Cuba, form one facies of the ultramafic complex in which they occur. Two planar structures, one a compositional layering due to variations in the relative proportions of olivine, pyroxene, plagioclase feldspar, and chromite, and the other a foliation caused by the orientation of pyroxene crystals in peridotite, are in general parallel, but diverge in a few places. Dips are fairly constant, being moderate to the northwest over most of the area, but sharp reversals occur immediately adjacent to irregularities in the chromite deposits. Two prominent joint sets are present: (1) Cross joints striking parallel to the strike of the foliation and dipping approximately at right angles to it; and (2) longitudinal joints striking parallel to the direction of dip of the foliation and nearly vertical. Gabbro dikes follow the first set, chrysotlle veins the second. Within the ore bodies dikes are commonly coarser‐grained, larger, and far more abundant than in peridotite; they enclose coarse, angular fragments of chromite. ©1947. American Geophysical Union. All Rights Reserved.
","language":"English","doi":"10.1029/TR028i002p00218","issn":"00028606","usgsCitation":"Guild, P.W., 1947, Petrology and structure of the Moa Chromite district, Oriente Province, Cuba: Eos, Transactions, American Geophysical Union, v. 28, no. 2, p. 218-246, https://doi.org/10.1029/TR028i002p00218.","productDescription":"29 p.","startPage":"218","endPage":"246","costCenters":[],"links":[{"id":370468,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Cuba ","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-82.26815,23.18861],[-81.40446,23.11727],[-80.61877,23.10598],[-79.67952,22.7653],[-79.28149,22.3992],[-78.34743,22.51217],[-77.9933,22.27719],[-77.14642,21.65785],[-76.52382,21.20682],[-76.19462,21.22057],[-75.59822,21.01662],[-75.67106,20.73509],[-74.9339,20.69391],[-74.17802,20.28463],[-74.29665,20.05038],[-74.96159,19.92344],[-75.63468,19.87377],[-76.32366,19.95289],[-77.75548,19.85548],[-77.08511,20.41335],[-77.49265,20.67311],[-78.13729,20.73995],[-78.48283,21.02861],[-78.71987,21.59811],[-79.285,21.55918],[-80.21748,21.82732],[-80.51753,22.03708],[-81.82094,22.19206],[-82.16999,22.38711],[-81.795,22.63696],[-82.7759,22.68815],[-83.49446,22.16852],[-83.9088,22.15457],[-84.05215,21.91058],[-84.54703,21.80123],[-84.97491,21.89603],[-84.44706,22.20495],[-84.23036,22.56575],[-83.77824,22.78812],[-83.26755,22.98304],[-82.51044,23.07875],[-82.26815,23.18861]]]},\"properties\":{\"name\":\"Cuba\"}}]}","volume":"28","issue":"2","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Guild, P. W.","contributorId":39039,"corporation":false,"usgs":true,"family":"Guild","given":"P.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":777963,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":55598,"text":"ofr4616 - 1946 - Copper deposits at the Rush and Brown mine and Venus prospect, Prince of Wales Island, southeastern Alaska","interactions":[{"subject":{"id":55598,"text":"ofr4616 - 1946 - Copper deposits at the Rush and Brown mine and Venus prospect, Prince of Wales Island, southeastern Alaska","indexId":"ofr4616","publicationYear":"1946","noYear":false,"title":"Copper deposits at the Rush and Brown mine and Venus prospect, Prince of Wales Island, southeastern Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":36144,"text":"b1090 - 1961 - Iron and copper deposits of Kasaan Peninsula, Prince of Wales Island, southeastern Alaska","indexId":"b1090","publicationYear":"1961","noYear":false,"title":"Iron and copper deposits of Kasaan Peninsula, Prince of Wales Island, southeastern Alaska"},"id":1}],"supersededBy":{"id":36144,"text":"b1090 - 1961 - Iron and copper deposits of Kasaan Peninsula, Prince of Wales Island, southeastern Alaska","indexId":"b1090","publicationYear":"1961","noYear":false,"title":"Iron and copper deposits of Kasaan Peninsula, Prince of Wales Island, southeastern Alaska"},"lastModifiedDate":"2024-04-24T20:18:29.03505","indexId":"ofr4616","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1946","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":"46-16","title":"Copper deposits at the Rush and Brown mine and Venus prospect, Prince of Wales Island, southeastern Alaska","docAbstract":"The Rush and Brown mine and the Venus prospect are near the head of Kasaan Bay about 10 miles northwest of the village of Kasaan and about 45 miles northwest of Ketchikan, the nearest port. (See fig. 1.) They are in an area of moderate relief in in which some hills are a little more than 500 feet high. Much of the area is covered with glacial drift and dense vegetation. Muskegs are numerous. Outcrops are scarce and are confined mostly to steep slopes, stream beds, and places where development work has been done on the ore deposits. Topographic, geologic, and magnetic surveys of the vicinities of the ore deposits were made by the Geological Survey in 1943, and a brief examination of a portion of the underground workings at the Rush and Brown mine was made in 1944.
The area is underlain principally by greenstone which has been intruded by bodies of pyroxenite, gabbro, and diorite. Foliation in the greenstone is obscure. post of the intrusive bodies trend northwesterly.
The principal ore deposits are veins containing chiefly pyrite, chalcopyrite, and pyrrhotite. A few deposits of copper-bearing magnetite have been found. Most of these are small, but a larger one at the Rush and Brown mine has been mined for its copper and precious metals.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr4616","usgsCitation":"Warner, L., Ray, R., and Flint, G., 1946, Copper deposits at the Rush and Brown mine and Venus prospect, Prince of Wales Island, southeastern Alaska: U.S. Geological Survey Open-File Report 46-16, Report: 21 p.; 1 Plate: 19.68 x 17.88 inches, https://doi.org/10.3133/ofr4616.","productDescription":"Report: 21 p.; 1 Plate: 19.68 x 17.88 inches","costCenters":[],"links":[{"id":428094,"rank":3,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1946/0016/figure-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":174114,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1946/0016/report-thumb.jpg"},{"id":428093,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1946/0016/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Alaska","otherGeospatial":"Prince of Wales Island, southeastern Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -133.80060829362583,\n 56.444493872044745\n ],\n [\n -133.80060829362583,\n 54.50933441146077\n ],\n [\n -131.62667263754602,\n 54.50933441146077\n ],\n [\n -131.62667263754602,\n 56.444493872044745\n ],\n [\n -133.80060829362583,\n 56.444493872044745\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db686367","contributors":{"authors":[{"text":"Warner, L.A.","contributorId":99611,"corporation":false,"usgs":true,"family":"Warner","given":"L.A.","email":"","affiliations":[],"preferred":false,"id":253792,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ray, R.G.","contributorId":60664,"corporation":false,"usgs":true,"family":"Ray","given":"R.G.","email":"","affiliations":[],"preferred":false,"id":253790,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Flint, G.M. Jr.","contributorId":79942,"corporation":false,"usgs":true,"family":"Flint","given":"G.M.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":253791,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70210409,"text":"70210409 - 1946 - Stratigraphy and structure of the area of the Killik, Chandler, Anaktuvuk, and Colville Rivers, Alaska","interactions":[],"lastModifiedDate":"2022-05-31T20:05:30.42295","indexId":"70210409","displayToPublicDate":"1946-12-31T14:53:04","publicationYear":"1946","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":5963,"text":"Geological Investigations, Naval Petroleum Reserve No. 4, Alaska","active":false,"publicationSubtype":{"id":6}},"seriesNumber":"1","title":"Stratigraphy and structure of the area of the Killik, Chandler, Anaktuvuk, and Colville Rivers, Alaska","docAbstract":"This report deals with results of field and laboratory studies carried out to May 1946 by the Geological Survey, largely as part of the Navy Department's program of petroleum investigations in northern Alaska. The immediate purpose of the work has been to collect and interpret stratigraphic and structural data pertinent to drilling in the Umiat area.
Field studies were made during the summers of 1944 and 1945 in the drainage areas of the Colville, Killik, Chandler, and. Anaktuvuk Rivers (fig. 1). Paleontologic and microlithologic studies, together with stratigrahica1 and structural analysis of the areas, were carried out in the petroleum laboratory in Fairbanks. This work led. to preparation of a preliminary report submitted. in December, 1945.
Additional detailed studies, in the Survey laboratories and offices in Washington, D. C., have resulted in some modification of earlier conclusions and changes in illustrations. The changes are minor and have no significant bearing on drilling in the Umiat area.
The present report is accompanied. by revised conies of figures 1, 2, 3 (sheet 1) and. 5. These illustrations should be substituted for the comparable figures of the preliminary report. Figures 3 (sheet 2), 4, and. 6 of the earlier report stand unchanged and should, be added to the illustrations accompanying the present report.
It is believed that work to date has revealed the general geologic picture of the area and. that the sequence of Upper Cretaceous rocks is established. The section of rocks in Umiat Test No. 1 has been approximately located within the sequence.
This report, and the work on which it is based was done under the supervision of George O. Gates, who has contributed. much to the study.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/70210409","usgsCitation":"Payne, T., Warner, L., Kirschner, C.E., Gryc, G., Stefansson, K., Webber, E.J., Fellows, R.E., Chapman, R.M., and Bressler, C.T., 1946, Stratigraphy and structure of the area of the Killik, Chandler, Anaktuvuk, and Colville Rivers, Alaska: Geological Investigations, Naval Petroleum Reserve No. 4, Alaska 1, Report: 32 p.; 12 Figures: 40.32 x 70.08 inches or smaller, https://doi.org/10.3133/70210409.","productDescription":"Report: 32 p.; 12 Figures: 40.32 x 70.08 inches or smaller","costCenters":[],"links":[{"id":401069,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70210409/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":375254,"rank":1,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_74593.htm","linkFileType":{"id":5,"text":"html"}},{"id":396523,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70210409/report-thumb.jpg"},{"id":401081,"rank":15,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-8.pdf","text":"Figure 8","linkFileType":{"id":1,"text":"pdf"}},{"id":401080,"rank":14,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-7.pdf","text":"Figure 7","linkFileType":{"id":1,"text":"pdf"}},{"id":401079,"rank":13,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-6.pdf","text":"Figure 6","linkFileType":{"id":1,"text":"pdf"}},{"id":401078,"rank":12,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-5-2.pdf","text":"Figure 5 Sheet 2","linkFileType":{"id":1,"text":"pdf"}},{"id":401077,"rank":11,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-5-1.pdf","text":"Figure 5 Sheet 1","linkFileType":{"id":1,"text":"pdf"}},{"id":401076,"rank":10,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-4-south.pdf","text":"Figure 4 South","linkFileType":{"id":1,"text":"pdf"}},{"id":401075,"rank":9,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-4-north.pdf","text":"Figure 4 North","linkFileType":{"id":1,"text":"pdf"}},{"id":401074,"rank":8,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-3-2.pdf","text":"Figure 3 Sheet 2","linkFileType":{"id":1,"text":"pdf"}},{"id":401073,"rank":7,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-3-1.pdf","text":"Figure 3 Sheet 1","linkFileType":{"id":1,"text":"pdf"}},{"id":401072,"rank":6,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-2-2.pdf","text":"Figure 2 Sheet 2","linkFileType":{"id":1,"text":"pdf"}},{"id":401071,"rank":5,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-2-1.pdf","text":"Figure 2 Sheet 1","linkFileType":{"id":1,"text":"pdf"}},{"id":401070,"rank":4,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70210409/figure-1.pdf","text":"Figure 1","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Alaska","otherGeospatial":"Anaktuvuk River, Chandler River, Colville River, River, Killik River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -154,\n 68\n ],\n [\n -151,\n 68\n ],\n [\n -151,\n 69.5\n ],\n [\n -154,\n 69.5\n ],\n [\n -154,\n 68\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Payne, T. G.","contributorId":284853,"corporation":false,"usgs":false,"family":"Payne","given":"T. G.","affiliations":[],"preferred":false,"id":836273,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Warner, L.A.","contributorId":99611,"corporation":false,"usgs":true,"family":"Warner","given":"L.A.","email":"","affiliations":[],"preferred":false,"id":836274,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kirschner, C. E.","contributorId":116415,"corporation":false,"usgs":true,"family":"Kirschner","given":"C.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":836275,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Gryc, George","contributorId":23942,"corporation":false,"usgs":true,"family":"Gryc","given":"George","affiliations":[],"preferred":false,"id":836276,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Stefansson, Karl","contributorId":61296,"corporation":false,"usgs":true,"family":"Stefansson","given":"Karl","email":"","affiliations":[],"preferred":false,"id":836277,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Webber, Edward J.","contributorId":25583,"corporation":false,"usgs":true,"family":"Webber","given":"Edward","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":836278,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Fellows, R. E.","contributorId":91919,"corporation":false,"usgs":true,"family":"Fellows","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":836279,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Chapman, R. M.","contributorId":47380,"corporation":false,"usgs":true,"family":"Chapman","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":836280,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Bressler, C. T.","contributorId":70053,"corporation":false,"usgs":true,"family":"Bressler","given":"C.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":836281,"contributorType":{"id":1,"text":"Authors"},"rank":9}]}} ,{"id":70215042,"text":"70215042 - 1946 - A portable differential thermal analysis unit for bauxite exploration","interactions":[],"lastModifiedDate":"2020-10-06T18:49:46.321638","indexId":"70215042","displayToPublicDate":"1946-10-06T13:30:32","publicationYear":"1946","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"A portable differential thermal analysis unit for bauxite exploration","docAbstract":"A small differential thermal analysis unit that embodies the fundamental features of larger laboratory models is designed for field exploration for bauxite and related materials. The apparatus, requiring only a source of electrical power, combines portability with ease of operation and rapid analysis. The portable unit is suitable for quantitative work and has been successfully applied in bauxite exploration on the island of Hispaniola.
","language":"English","publisher":"Society of Economic Geologist","doi":"10.2113/gsecongeo.41.1.64","usgsCitation":"Hendricks, S.B., and Nelson, R.A., 1946, A portable differential thermal analysis unit for bauxite exploration: Economic Geology, v. 41, no. 1, p. 64-76, https://doi.org/10.2113/gsecongeo.41.1.64.","productDescription":"13 p.","startPage":"64","endPage":"76","costCenters":[],"links":[{"id":379099,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"41","issue":"1","noUsgsAuthors":false,"publicationDate":"1946-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Hendricks, S. B.","contributorId":50202,"corporation":false,"usgs":true,"family":"Hendricks","given":"S.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":800618,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nelson, R. A.","contributorId":96727,"corporation":false,"usgs":true,"family":"Nelson","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":800619,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70214507,"text":"70214507 - 1946 - Hydrothermal alteration in the Castle Dome copper deposit, Arizona","interactions":[],"lastModifiedDate":"2020-09-28T19:20:35.98503","indexId":"70214507","displayToPublicDate":"1946-09-28T14:12:53","publicationYear":"1946","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Hydrothermal alteration in the Castle Dome copper deposit, Arizona","docAbstract":"Hydrothermal alteration of the quartz monzonite host rock in the Castle Dome copper deposit consists of three phases. Very weak propylitic alteration of biotite and plagioclase occurs in the marginal part of the mineralized area. Where mineralization is stronger most of the plagioclase and some of the orthoclase and biotite are replaced by a montmorillonitetype clay, resembling beidellite, and hydrous mica. The third phase is localized along quartz-pyrite veins where the wall rock, commonly as much as an inch from the vein, is replaced by quartz and seriate. In contrast to the localization of quartz-sericite alteration along the veins, clay alteration is general and can be seen between the veins wherever the rock is not completely sericitized. Thus these two types of alteration cannot be separated areally. The most intense clay alteration together with moderate quartz-sericite alteration occurs in the ore body, whereas the strongest quartz-sericite alteration, where pyrite veins are largest and most numerous, is in a zone along the north side of the ore body.
","language":"English","publisher":"Society of Economic Geologist","doi":"10.2113/gsecongeo.41.8.820","usgsCitation":"Peterson, N.P., Gilbert, C., and Quick, G., 1946, Hydrothermal alteration in the Castle Dome copper deposit, Arizona: Economic Geology, v. 41, no. 8, p. 820-840, https://doi.org/10.2113/gsecongeo.41.8.820.","productDescription":"21 p.","startPage":"820","endPage":"840","costCenters":[],"links":[{"id":378823,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.4453125,\n 32.79651010951669\n ],\n [\n -110.621337890625,\n 32.79651010951669\n ],\n [\n -110.621337890625,\n 33.578014746143985\n ],\n [\n -111.4453125,\n 33.578014746143985\n ],\n [\n -111.4453125,\n 32.79651010951669\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"41","issue":"8","noUsgsAuthors":false,"publicationDate":"1946-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Peterson, Nels P.","contributorId":85252,"corporation":false,"usgs":true,"family":"Peterson","given":"Nels","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":799757,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gilbert, Charles","contributorId":44418,"corporation":false,"usgs":true,"family":"Gilbert","given":"Charles","affiliations":[],"preferred":false,"id":799758,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Quick, G.L.","contributorId":102126,"corporation":false,"usgs":true,"family":"Quick","given":"G.L.","email":"","affiliations":[],"preferred":false,"id":799759,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70010902,"text":"70010902 - 1945 - Determination of fluoride in water. A modified zirconium-alizarin method","interactions":[],"lastModifiedDate":"2025-01-02T17:14:18.994486","indexId":"70010902","displayToPublicDate":"1945-01-01T00:00:00","publicationYear":"1945","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1986,"text":"Industrial and Engineering Chemistry","active":true,"publicationSubtype":{"id":10}},"title":"Determination of fluoride in water. A modified zirconium-alizarin method","docAbstract":"A convenient, rapid colorimetric procedure using the zirconium-alizarin indicator acidified with sulfuric acid for the determination of fluoride in water is described. Since this acid indicator is stable indefinitely, it is more useful than other zirconium-alizarin reagents previously reported. The use of sulfuric acid alone in acidifying the zirconium-alizarin reagent makes possible the maximum suppression of the interference of sulfate. Control of the pH of the samples eliminates errors due to the alkalinity of the samples. The fluoride content of waters containing less than 500 parts per million of sulfate and less than 1000 p.p.m. of chloride may be determined within a limit of 0.1 p.p.m. when a 100-ml. sample is used.","language":"English","publisher":"ACS Publications","doi":"10.1021/i560139a007","issn":"00964484","usgsCitation":"Lamar, W., 1945, Determination of fluoride in water. A modified zirconium-alizarin method: Industrial and Engineering Chemistry, v. 17, no. 3, p. 148-149, https://doi.org/10.1021/i560139a007.","productDescription":"2 p.","startPage":"148","endPage":"149","numberOfPages":"2","costCenters":[],"links":[{"id":221412,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"17","issue":"3","noUsgsAuthors":false,"publicationDate":"2002-05-01","publicationStatus":"PW","scienceBaseUri":"5059ffa7e4b0c8380cd4f2ef","contributors":{"authors":[{"text":"Lamar, W.L.","contributorId":52549,"corporation":false,"usgs":true,"family":"Lamar","given":"W.L.","email":"","affiliations":[],"preferred":false,"id":359870,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1276,"text":"wsp918 - 1944 - Summary of records of surface waters at base stations in Colorado River Basin, 1891-1938","interactions":[],"lastModifiedDate":"2018-12-17T10:44:32","indexId":"wsp918","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1944","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":"918","title":"Summary of records of surface waters at base stations in Colorado River Basin, 1891-1938","docAbstract":"Collection by the Geological Survey of records of stream flow in the Colorado River Basin was begun in August 1889, when three gaging stations were established in Arizona, on' the Gila, Salt, and Verde Rivers. In 1894-95 the work was extended to include 15 gaging stations, on tributary streams at points in the basin where irrigation development was most intensive, and by 1910 the number had increased to 109. In 1938 there were 262 gaging stations, located to advantage throughout the basin.
The earliest known records of discharge in the Colorado River Basin were individual measurements of the main river, made by engineers of the United States Army, 1 at Stone's Ferry near Boulder Canyon August 12, 1875, at Camp Mohave September 2, 1875, and at Fort Yuma March 20, 1876. In the summer of 1876, the Southern Pacific Co. established a gage near the railroad bridge over Colorado River at Yuma, and daily gage readings at that point, now available, are continuous since January 1, 1878.
Modern irrigation, using surface waters diverted from various streams in the basin, was begun many years before the first continuous records of discharge Had been obtained. As developments for irrigation and other purposes increased in size and number, became more systematized, and required greater knowledge of water supply, the collection of records of stream flow was substantially augmented through the assistance of many interested parties and agencies, both private and public.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp918","usgsCitation":"Dickinson, W., 1944, Summary of records of surface waters at base stations in Colorado River Basin, 1891-1938: U.S. Geological Survey Water Supply Paper 918, Report: iv, 274 p.; Plate: 20.69 x 27.73 inches, https://doi.org/10.3133/wsp918.","productDescription":"Report: iv, 274 p.; Plate: 20.69 x 27.73 inches","numberOfPages":"292","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true},{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":26236,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/0918/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":265377,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/0918/plate-1.pdf"},{"id":137522,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/0918/report-thumb.jpg"}],"country":"United States","otherGeospatial":"Colorado River Basin","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b03e4b07f02db698f62","contributors":{"authors":[{"text":"Dickinson, W.E.","contributorId":91468,"corporation":false,"usgs":true,"family":"Dickinson","given":"W.E.","email":"","affiliations":[],"preferred":false,"id":143484,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}