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No abstract available.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr5783","usgsCitation":"Newell, T.R., 1957, Streamflow East Fork Bruneau River below Three Creek, near Three Creek, Idaho: U.S. Geological Survey Open-File Report 57-83, 42 p., https://doi.org/10.3133/ofr5783.","productDescription":"42 p.","costCenters":[],"links":[{"id":181773,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1957/0083/report-thumb.jpg"},{"id":369598,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1957/0083/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b15e4b07f02db6a4fa7","contributors":{"authors":[{"text":"Newell, Thomas R.","contributorId":106876,"corporation":false,"usgs":true,"family":"Newell","given":"Thomas","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":254743,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":56089,"text":"ofr5796 - 1957 - Surface water supply of eastern and central North Carolina","interactions":[],"lastModifiedDate":"2016-12-09T11:11:51","indexId":"ofr5796","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"57-96","title":"Surface water supply of eastern and central North Carolina","docAbstract":"None of the many factors that influence the economic growth of eastern and central North Carolina plays a more important role than water. Adequate water supply for municipal, rural domestic, industrial, and agricultural uses, is a basic need of any region.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5796","collaboration":"Prepared in cooperation with Division of Water Resources, Inlets and Coastal Waterways, North Carolina Department of Conservation and Development","usgsCitation":"Rice, E.B., 1957, Surface water supply of eastern and central North Carolina: U.S. Geological Survey Open-File Report 57-96, v, 92 p., https://doi.org/10.3133/ofr5796.","productDescription":"v, 92 p.","numberOfPages":"96","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":287409,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287408,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1957/0096/report.pdf"}],"country":"United States","state":"North 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Carolina\",\"nation\":\"USA \"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae5e4b07f02db68a5f0","contributors":{"authors":[{"text":"Rice, Edward B.","contributorId":103362,"corporation":false,"usgs":true,"family":"Rice","given":"Edward","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":254750,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39151,"text":"pp292 - 1957 - Geology of the southern Elkhorn Mountains, Jefferson and Broadwater Counties, Montana","interactions":[],"lastModifiedDate":"2018-02-23T12:32:11","indexId":"pp292","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"292","title":"Geology of the southern Elkhorn Mountains, Jefferson and Broadwater Counties, Montana","docAbstract":"

The geology of an area of about 270 square miles in the southern Elkhorn Mountains, west of Townsend in west-central Montana, is described. The mountains in the southern part of the area comprise northward-trending alternating ridges and valleys underlain principally by folded sedimentary rocks. They merge northward into the higher and more rugged main mass of the mountains, which is underlain principally by upper Cretaceous volcanic rocks. The mountaintops are 1,000 to 4,500 feet above the major valleys.

The sedimentary rocks range in age from Precambrian to Tertiary and the igneous rocks from late Cretaceous to probably middle Tertiary. The oldest rocks are varicolored mudstone, shale, and sandstone of the Belt series of late Precambrian age. They are overlain with slight unconformity by a moderately thick but incomplete section of Paleozoic rocks. The basal Paleozoic formation is the Flathead quartzite of Middle Cambrian age, which is overlain by alternating units of shale and carbonate rock : the Wolsey shale, the Meagher limestone, the Park shale, the Pilgrim dolomite, and the Red Lion formation, all of Cambrian age. A slight erosional unconformity between the Red Lion formation and the Maywood formation of late Devonian age marks a long interval of crustal stability in the area. The Maywood is overlain by the Jefferson dolomite and the Three Forks shale of Late Devonian and Mississippian age, and these in turn are conformably overlain by the Lodgepole and Mission Canyon limestones, a thick carbonate sequence of Mississippian age. A slight erosional unconformity separates the Mission Canyon limestone from the Amsden formation, which probably includes beds of both Mississippian and Pennsylvanian age. The Amsden is composed of a heterogeneous assemblage of arenaceous, argillaceous, dolomitic, and calcareous rocks and grades upward into the Quadrant formation of Pennsylvanian age, an alternation of quartzitic sandstone and dolomite. At the top of the Paleozoic section is the Phosphoria formation of Permian age, a thin unit of chert and quartzitic sandstone that contains a few thin phosphate beds.

The basal Mesozoic unit is the Swift formation of late Jurassic age, a thin calcareous marine sandstone that overlies the Phosphoria with slight erosional unconformity. It is overlain by nonmarine shale and sandstone of the Morrison formation of late Jurassic age and the Kootenai formation of Early Cretaceous age. The Kootenai is overlain, possibly with slight erosional unconformity, by the Colorado formation an assemblage of marine dark shale and siliceous mudstone and nonmarine quartz-chert sandstone. The Colorado formation as here used includes beds of both Early and Late Cretaceous age. The Colorado in places grades upwards into a sequence of feldspathic sandstone and tuff beds here named the Slim Sam formation. Elsewhere within the area, the Slim Sam formation is absent, probably in part owing to erosion and in part nondeposition. Where present, the Slim Sam grades upward into a thick sequence of andesitic and quartz latitic volcanic rocks, comprising tuffs, lapilli tuffs, breccias, welded tuffs and flows, that are here named the Elkhorn Mountains volclinics and are probably entirely of Cretaceous age. Where the Slim Sam formation is absent, the Elkhorn Mountains volcanics rest with angular unconformity on beds as old as the Morrison. 

The pre-Tertiary layered rocks, aggregating more than 15,000 feet in thickness, were folded and intruded by igneous rocks of several types, and the area was uplifted and eroded to a terrain of mature relief, similar to that of the present. During the Oligocene epoch, volcanic sediments with interbreds of nonvolcanic gravel accumulated. These beds were in turn moderately eroded, and gravel of Miocene ( ?) age was deposited in channels within them. Subsequently, probably during the Pliocene epoch, the Tertiary beds were weakly deformed locally, and a pediment was cut across the Tertiary and older rocks in the southern part of the area. Fan gravel, in part of Recent origin and in part older, blankets parts of the pediment. Glacial deposits of at least two stages of Pleistocene glaciation are present in the higher mountains in the northern part of the area.

The intrusive igneous rocks, except for a few felsite dikes of uncertain age, are divisible into two groups, primarily on the basis of structural relations and secondarily on the basis of composition and fabric. The older group of dioritic and andesitic rocks were intruded in part, if not wholly, prior to the main folding and are similar in chemical and mineralogical composition to the Elkhorn Mountains volcanics. They were probably emplaced throughout the period of volcanism that commenced in late Niobrara time and continued until late Cretaceous time. The younger group consists chiefly of quartzbearing phanerites but includes rocks ranging from gabbro to alaskitic granite and aplite. These rocks were emplaced after the main episode of folding and faulting. The Boulder batholith, composed dominantly of quartz monzonite, is the principal body of this younger group.

The older igneous rocks metamorphosed the invaded rocks only slightly. In contrast, the younger intrusive bodies, and especially the batholith, altered and recrystallized the country rock in moderately broad belts, changing them to various types of hornfels, calcsilicate rock, marble, and vitreous quartzite. Concomitantly magnetite, garnet, axinite, and other high-temperature replacement minerals formed locally as products of additive metamorphism.

The pre-Tertiary layered rocks of the southern Elkhorn Mountains are folded into northward-trending folds and are cut by many faults. The sedimentary rocks tend to be more tightly folded than the Elkhorn Mountains volcanics, although both were involved in the major folding. The principal folds of the area from east to west are : a major dome, a complex syncline with several second-order folds, and a remnant of a northward-plunging anticline, the major part of which was engulfed by the batholith. The folded rocks are cut by many faults of small to moderate displacement and by two faults of large displacement. Most of the faults were probably formed by the same forces that produced the folds. The origin of the two major faults, however, is uncertain, and may be related to igneous activity. The batholith crosscuts the folded structure and is in turn cut by small faults. Some parts of the area were elevated along steep normal faults in late Tertiary time. 

The southern part of the Elkhorn Mountains has been mountainous at least since early Oligocene time, and probably began to take form during the Cretaceous. As a consequence of long continued erosion, the modern topography reflects the structure and lithologic character of the underlying rocks except in a few areas blanketed by poorly consolidated Tertiary rocks and in the higher mountains where glaciation has been prominent.

Silver, lead, zinc, and gold have been produced, either singly or, more typically, as a combination of metals from a number of types of ore deposits. Replacement deposits in carbonate rocks are the most common type, but veins, contact metamorphic deposits, and pipelike bodies of breccia cemented by ore and gangue minerals also are present. The Elkhorn mining district has the largest number of mines and the greatest variety of types of deposits. In the Tizer Basin several narrow goldbearing veins cut andesitic volcanic rocks, and in the southern part of the area sporadic small veins and replacement deposits occur in carbonate rocks. The mines and prospects of the area are described, and some suggestions for future prospecting are outlined. The application of geochemical prospecting techniques may prove of value, judging from the results of reconnaissance soil sampling in the vicinity of the Elkhorn mine.

","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp292","usgsCitation":"Klepper, M.R., Weeks, R.A., and Ruppel, E.T., 1957, Geology of the southern Elkhorn Mountains, Jefferson and Broadwater Counties, Montana: U.S. Geological Survey Professional Paper 292, Report: iv, 82 p.; 7 Plates: 44.48 x 23.48 inches or smaller, https://doi.org/10.3133/pp292.","productDescription":"Report: iv, 82 p.; 7 Plates: 44.48 x 23.48 inches or smaller","costCenters":[],"links":[{"id":351914,"rank":9,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0292/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271139,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271143,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271144,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271145,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271146,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271138,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271141,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0292/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":165294,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0292/report-thumb.jpg"}],"scale":"31250","country":"United States","state":"Montana","county":"Broadwater County;Jefferson County","otherGeospatial":"Elkhorn Mountains","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112.92,46.12 ], [ -112.92,47.23 ], [ -111.03,47.23 ], [ -111.03,46.12 ], [ -112.92,46.12 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c79e","contributors":{"authors":[{"text":"Klepper, M. R.","contributorId":64278,"corporation":false,"usgs":true,"family":"Klepper","given":"M.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":221047,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weeks, R. A.","contributorId":75914,"corporation":false,"usgs":true,"family":"Weeks","given":"R.","middleInitial":"A.","affiliations":[],"preferred":false,"id":221048,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ruppel, E. T.","contributorId":6041,"corporation":false,"usgs":true,"family":"Ruppel","given":"E.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":221046,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":15737,"text":"ofr5887 - 1957 - Geology of the Basin Quadrangle, Montana","interactions":[{"subject":{"id":15737,"text":"ofr5887 - 1957 - Geology of the Basin Quadrangle, Montana","indexId":"ofr5887","publicationYear":"1957","noYear":false,"title":"Geology of the Basin Quadrangle, Montana"},"predicate":"SUPERSEDED_BY","object":{"id":35698,"text":"b1151 - 1963 - Geology of the Basin quadrangle: Jefferson, Lewis and Clark, and Powell Counties, Montana","indexId":"b1151","publicationYear":"1963","noYear":false,"title":"Geology of the Basin quadrangle: Jefferson, Lewis and Clark, and Powell Counties, Montana"},"id":1}],"supersededBy":{"id":35698,"text":"b1151 - 1963 - Geology of the Basin quadrangle: Jefferson, Lewis and Clark, and Powell Counties, Montana","indexId":"b1151","publicationYear":"1963","noYear":false,"title":"Geology of the Basin quadrangle: Jefferson, Lewis and Clark, and Powell Counties, Montana"},"lastModifiedDate":"2024-07-17T19:47:34.920637","indexId":"ofr5887","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"58-87","title":"Geology of the Basin Quadrangle, Montana","docAbstract":"

The Basin quadrangle, in the northern part of the Boulder Mountains between Butte and Helena, Montana, is underlain principally by igneous rocks that include Late Cretaceous quartz latitic and andesitic Elkhorn Mountains volcanics, quartz monzonite and related rocks of the Boulder batholith, Oligocene(?) quartz latitic volcanic rocks, and late Miocene(?)-early Pliocene(?) rhyolitic volcanic rocks. Sedimentary rocks of the Late Jurassic Morrison formation, the Early Cretaceous Kootenai formation, and the Early Cretaceous lower part of the Colorado formation, crop out in the northwest part of the quadrangle. The batholithic rocks include early stage quartz monzonite, intermediate or main stage quartz monzonite and granodiorite, and late stage aplite and alaskite. The rocks of the main stage are in discontinuous layers approximately conformable to the folded Elkhorn Mountains volcanics that form the roof of the batholith, and may be part of a sill-like body rather than of a batholith in the classic sense. Metamorphic changes in the roof rocks are not conspicuous except in one stratigraphic unit that probably was especially susceptible to thermal reorganization.

The batholithic rocks and Elkhorn Mountains volcanics are jointed, and are cut by faults that trend about east, north, N. 20° E., northeast, and northwest. The east-trending faults are most abundant, especially in the eastern part of the quadrangle, and cut only the batholithic and pre-batholithic rocks, whereas many of the faults of other trends cut Tertiary volcanic rocks and a few cut Pleistocene glacial deposits.

A surface of moderate relief was cut before eruption of the Oligocene(?) volcanic rocks, and the late Miocene(?)-early Pliocene(?) volcanic rocks covered a deeply weathered surface of low relief. By the Pleistocene a landscape essentially like that of today had been formed, and during the one period of Pleistocene glaciation, valley glaciers and a mountain ice sheet modified the earlier landforms and left extensive deposits of till and outwash. These deposits have been modified in many places by mass-wasting processes that have dominated post-glacial erosion.

Mineral deposits in the quadrangle include deposits of disseminated auriferous pyrite, base- and precious-metal bearing quartz veins that occupy the east-trending fault zones, placer deposits of gold and tin, and a few non-metallic deposits, chiefly stone, gravel, and dumortierite. Nearly all of the metallic minerals mined in the quadrangle have come from the east-trending quartz veins and from the placer deposits.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5887","usgsCitation":"Ruppel, E.T., 1957, Geology of the Basin Quadrangle, Montana: U.S. Geological Survey Open-File Report 58-87, Report: viii, 219 p.; 7 Plates: 34.96 x 52.09 inches or smaller; 7 Tables: 23.93 x 24.44 inches or smaller, https://doi.org/10.3133/ofr5887.","productDescription":"Report: viii, 219 p.; 7 Plates: 34.96 x 52.09 inches or smaller; 7 Tables: 23.93 x 24.44 inches or smaller","costCenters":[],"links":[{"id":431191,"rank":16,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431190,"rank":15,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431189,"rank":14,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431188,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431187,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431186,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431185,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0087/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431184,"rank":9,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1958/0087/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431183,"rank":8,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431182,"rank":7,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431181,"rank":6,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431180,"rank":5,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431179,"rank":4,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431178,"rank":3,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":431177,"rank":2,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1958/0087/Table-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":146495,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1958/0087/report-thumb.jpg"}],"scale":"24000","country":"United States","state":"Montana","otherGeospatial":"Basin Quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -112.55138492319185,\n 46.59423812949282\n ],\n [\n -112.55138492319185,\n 46.03252022844208\n ],\n [\n -111.78355228633728,\n 46.03252022844208\n ],\n [\n -111.78355228633728,\n 46.59423812949282\n ],\n [\n -112.55138492319185,\n 46.59423812949282\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db6834cd","contributors":{"authors":[{"text":"Ruppel, Edward Thompson","contributorId":67066,"corporation":false,"usgs":true,"family":"Ruppel","given":"Edward","email":"","middleInitial":"Thompson","affiliations":[],"preferred":false,"id":171622,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15450,"text":"ofr5791 - 1957 - Glacial features and surficial deposits of the Malaspina district, Alaska","interactions":[{"subject":{"id":15450,"text":"ofr5791 - 1957 - Glacial features and surficial deposits of the Malaspina district, Alaska","indexId":"ofr5791","publicationYear":"1957","noYear":false,"title":"Glacial features and surficial deposits of the Malaspina district, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":66820,"text":"i271 - 1958 - Glacial features and surficial deposits of the Malaspina district, Alaska","indexId":"i271","publicationYear":"1958","noYear":false,"title":"Glacial features and surficial deposits of the Malaspina district, Alaska"},"id":1}],"supersededBy":{"id":66820,"text":"i271 - 1958 - Glacial features and surficial deposits of the Malaspina district, Alaska","indexId":"i271","publicationYear":"1958","noYear":false,"title":"Glacial features and surficial deposits of the Malaspina district, Alaska"},"lastModifiedDate":"2024-01-26T21:33:37.679674","indexId":"ofr5791","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"57-91","title":"Glacial features and surficial deposits of the Malaspina district, Alaska","docAbstract":"

The Malaspina district extends about 50 miles along the north shore of the Gulf of Alaska from Icy Bay and the Guyot Glacier on the west to Yakutat Bay and Disenchantment Bay on the east (see index map). The district includes a coastal lowland flanked on the north by a belt of rugged foothills, the higher ridges and peaks of which rise to altitudes of 1,000 to 6,000 feet. The southern front of the St. Ell as Mountains rises abruptly at the northern margin of the foothills belt, about 30 miles from the coast, culminating in Mount St. Elias (18,008 ft.).

The Malaspina Glacier, the dominant feature of the Malaspina district, has long been regarded as the type example of the piedmont glacier. This huge ice sheet covers an area of about 840 square miles of the coastal lowland, rising gradually from an altitude of 100 feet or less at the outer margin to altitudes ranging from 1,000 feet to 2,000 feet at the southern margin of the foothills belt. The Malaspina Glacier is of special interest to glaciologists because its strikingly developed morainic banding offers clues to the nature of glacier movement. The processes of wastage and deposition at the stagnant margin of Malaspina Glacier can be compared with the mode of retreat of the former continental ice sheets; much can be learned here of the origin
of the deposits formed along a stagnant ice margin.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5791","usgsCitation":"Plafker, G., and Miller, D.J., 1957, Glacial features and surficial deposits of the Malaspina district, Alaska: U.S. Geological Survey Open-File Report 57-91, Report: 13 p.; 2 Plates: 22.64 x 45.69 inches and 48.66 x 41.99 inches, https://doi.org/10.3133/ofr5791.","productDescription":"Report: 13 p.; 2 Plates: 22.64 x 45.69 inches and 48.66 x 41.99 inches","costCenters":[],"links":[{"id":149011,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1957/0091/report-thumb.jpg"},{"id":425068,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1957/0091/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":425067,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1957/0091/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":425066,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1957/0091/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"96000","country":"United States","state":"Alaska","otherGeospatial":"Malaspina district","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -141.31365442885615,\n 60.237641221178194\n ],\n [\n -141.31365442885615,\n 59.68683300309837\n ],\n [\n -139.80902050605346,\n 59.68683300309837\n ],\n [\n -139.80902050605346,\n 60.237641221178194\n ],\n [\n -141.31365442885615,\n 60.237641221178194\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac5e4b07f02db679cfb","contributors":{"authors":[{"text":"Plafker, George","contributorId":3920,"corporation":false,"usgs":false,"family":"Plafker","given":"George","email":"","affiliations":[],"preferred":false,"id":171152,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, Don John","contributorId":77120,"corporation":false,"usgs":true,"family":"Miller","given":"Don","email":"","middleInitial":"John","affiliations":[],"preferred":false,"id":171153,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":14401,"text":"ofr5760 - 1957 - Records available to September 30, 1956, on use of water in the Delaware Basin Project area","interactions":[],"lastModifiedDate":"2014-05-21T08:30:12","indexId":"ofr5760","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"57-60","title":"Records available to September 30, 1956, on use of water in the Delaware Basin Project area","docAbstract":"

The purpose of this report is to summarize data on the use of water in the Delaware Basin Project area (fig. 2) and to list the principal data sources that are available in published form. The tables and bibliography will assist Geological Survey personnel assigned to the Delaware Basin Project in evaluating the scope and deficiencies of previous studies of the basin. Information is also given on the use of water by public supplies in the New York-New Jersey region comprising the New York City Metropolitan Area and in the remaining north-central and south-eastern parts of New Jersey. These regions may depend increasingly on water from the Delaware River basin for part of their public supplies.

\n
\n

The Geological Survey has the responsibility for appraising and describing the water resources of the Nation as a guide to use, development, control, and conservation of these resources. Cooperative Federal-State water-resources investigations in the Delaware Basin States have been carried on the the Geological Survey for more than 50 years. In July 1956 the Survey began the \"Delaware Basin Project,\" a hydrologic study of the Delaware River basin in order to: 1) Determine present status and trends in water availability, quality, and use, 2) assess and improve the adequacy of the Survey's basic water data program in the basin, 3) interpret and evaluate the water-resources data in terms of past and possible future water-use and land-use practices, and 4) disseminate promptly the results of this investigation for the benefit of all interested agencies and the general public. The Geological Survey is working closely with the U.S. Corps of Engineers and other cooperating Federal and State agencies in providing water data which will contribute to the present coordinated investigation aimed at developing a plan for long-range water development in the Delaware River basin.

\n
\n

Estimates of quantities of water used are given for water withdrawn from streams and aquifers during calendar year 1955, as compiled or estimated from publications and manuscripts prepared between 1950 and 1956. All quantities are given in millions of gallons per day (mgd). The source of the water used, ground or surface, and the type of use to which is was put -- public supply, industrial supply, irrigation, or rural use -- is given. Use of water for hydroelectric power was not compiled for this report. Most tables in this report do not subdivide withdrawals into fresh and saline water; however, most supplies are fresh, except some of those withdrawn directly from the Delaware River downstream from Philadelphia, Pa. All quantities are expressed as an average rate for a full year and are lower, therefore, than rates resulting from the increased demand for water during the summer for air conditioning and supplemental irrigation.

\n
\n

The primary emphasis of this study was to get an over-all picture of water use throughout large parts of the basin. Therefore, publications relating to a dingle city or county, other than New York City, seldom were used; revisions and refinement based on such sources of information are best made by the field personnel most familiar with locally filed publications and published data.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington D.C.","doi":"10.3133/ofr5760","usgsCitation":"Kammerer, J., 1957, Records available to September 30, 1956, on use of water in the Delaware Basin Project area: U.S. Geological Survey Open-File Report 57-60, ii, 33 p., https://doi.org/10.3133/ofr5760.","productDescription":"ii, 33 p.","numberOfPages":"37","costCenters":[],"links":[{"id":287385,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287384,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1957/0060/report.pdf"}],"country":"United States","state":"Delaware","otherGeospatial":"Delaware Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -76.0,39.0 ], [ -76.0,42.0 ], [ -75.0,42.0 ], [ -75.0,39.0 ], [ -76.0,39.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a61e4b07f02db63579e","contributors":{"authors":[{"text":"Kammerer, John C.","contributorId":53815,"corporation":false,"usgs":true,"family":"Kammerer","given":"John C.","affiliations":[],"preferred":false,"id":169392,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1347,"text":"wsp1415 - 1957 - Water resources of the Yadkin-Pee Dee River basin, North Carolina","interactions":[],"lastModifiedDate":"2022-12-19T21:34:27.121988","indexId":"wsp1415","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1415","title":"Water resources of the Yadkin-Pee Dee River basin, North Carolina","docAbstract":"Sufficient water is available in the basin of the Yadkin and Pee Dee Rivers to meet present requirements and those for many years to come if water use increases at about the present rate. Data presented in this report show that the average annual streamflow from approximately 82 percent of the basin area during the 25-year period, 1929-53, was about 6,200 mgd, representing essentially the total available water supply. Comparison of the available water supply to the estimated withdrawal use (excluding water power) of both surface and ground water of 600 mgd indicates the relative utilization of the water resources of the basin at present. If proper pollution controls are observed and practiced so that water in the various streams may be reused several times, the potential water available is even greater than indicated by the above comparison. Preliminary studies indicate that the quantity of water now being withdrawn from ground-water reservoirs in the basin is only a fraction of the total that may be obtained from this source.\r\n\r\nTwenty-eight of the 64 municipalities having public water-supply systems use surface water; however, as the largest cities in the area use surface supplies, about 85 percent of the water used for public supplies is from surface sources.\r\n\r\nOf the 20 complete-record stream-gaging stations now in operation in this area 7 have been in operation for 24 years or longer. Periodic measurements of the rate of flow have been made at 31 additional sites on streams scattered widely over the basin. All available streamflow data including those for 1953 are summarized in either graphic or tabular form, or both. Because of the critically low flows occurring during the drought of 1954, several illustrations include data for 1954 and the early months of 1955 for comparison with the minima of previous years.\r\n\r\nAdequate water for domestic use is available from wells throughout the basin. The consolidated rocks of the Piedmont furnish water for small industries and for municipalities whose population is less than about 1,500. The yields of wells in rock range from less than 1 gpm to as much as 200 gpm with local, rather than regional, geologic factors controlling the yield. The average municipal well in consolidated rocks yields about 30 gpm. In contrast, the sands of the Coastal Plain, in the eastern part of the basin, furnish as much as 500 gpm to individual wells, and ground-water conditions are generally similar throughout that region. A cumulative deficiency in rainfall from 1953 to 1955, has caused ground-water levels to fall below the seasonal averages, but the decline is thought not to indicate a long-term trend. The most serious problem involving future use of ground water is the lack of knowledge of the characteristics of the ground-water provinces in the basin.\r\n\r\nGenerally the chemical quality of the surface waters in the Yadkin-Pee Dee River basin is good. They are low in mineral matter and soft, although some of the surface water contains excessive quantities of iron. In some local areas the streams have been polluted by municipal and industrial wastes. During periods of high runoff many of the streams transport large quantities of suspended sediment. Tributary streams in the lower eastern part of the basin are highly colored because of drainage from swampy areas.\r\n\r\nGround water from the consolidated rocks in the Piedmont region is more variable in quality than water from other areas in the basin. The dissolved solids in water from the consolidated rocks ranged from 26 to 1,480 ppm with a median of 109 ppm. Wells in the Cretaceous clay province normally yield slightly acid waters. The pH ranges from 4.7 to 7.7 with a median of 5.3. Generally ground water in this province is extremely soft and low in dissolved solids. Wells in the Cretaceous sand province yield a sodium bicarbonate type of water ranging in hardness from 2 to 130 ppm.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1415","usgsCitation":"Fish, R.E., LeGrand, H.E., and Billingsley, G., 1957, Water resources of the Yadkin-Pee Dee River basin, North Carolina: U.S. Geological Survey Water Supply Paper 1415, Report: viii, 112 p.; 4 Plates: 15.50 x 15.78 inches or smaller, https://doi.org/10.3133/wsp1415.","productDescription":"Report: viii, 112 p.; 4 Plates: 15.50 x 15.78 inches or smaller","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":26419,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1415/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137518,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1415/report-thumb.jpg"},{"id":26422,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1415/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26418,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1415/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26420,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1415/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26421,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1415/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":410738,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24369.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"North Carolina, Virginia","otherGeospatial":"Yadkin-Pee Dee River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -78.57421875,\n 33.87041555094183\n ],\n [\n -77.98095703125,\n 33.742612777346885\n ],\n [\n -77.54150390625,\n 33.96158628979907\n ],\n [\n -78.11279296875,\n 34.50655662164561\n ],\n [\n -78.77197265625,\n 34.903952965590065\n ],\n [\n -78.92578124999999,\n 35.55010533588552\n ],\n [\n -79.47509765625,\n 36.27970720524017\n ],\n [\n -79.56298828125,\n 36.56260003738545\n ],\n [\n -79.73876953125,\n 36.98500309285596\n ],\n [\n -80.15625,\n 36.77409249464195\n ],\n [\n -81.14501953125,\n 36.26199220445664\n ],\n [\n -81.67236328125,\n 36.26199220445664\n ],\n [\n -82.1337890625,\n 35.7286770448517\n ],\n [\n -81.76025390625,\n 35.7286770448517\n ],\n [\n -81.05712890625,\n 35.37113502280101\n ],\n [\n -80.79345703125,\n 34.79576153473033\n ],\n [\n -79.65087890624999,\n 34.813803317113155\n ],\n [\n -78.57421875,\n 33.87041555094183\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e5e4b07f02db5e6f7c","contributors":{"authors":[{"text":"Fish, Robert Eugene","contributorId":73982,"corporation":false,"usgs":true,"family":"Fish","given":"Robert","email":"","middleInitial":"Eugene","affiliations":[],"preferred":false,"id":143604,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"LeGrand, H. E.","contributorId":54571,"corporation":false,"usgs":true,"family":"LeGrand","given":"H.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":143603,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Billingsley, G. A.","contributorId":33694,"corporation":false,"usgs":true,"family":"Billingsley","given":"G. A.","affiliations":[],"preferred":false,"id":143602,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1222,"text":"wsp1460C - 1957 - Ground-water possibilities south of the Snake River between Twin Falls and Pocatello, Idaho","interactions":[],"lastModifiedDate":"2013-11-26T10:52:05","indexId":"wsp1460C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1460","chapter":"C","title":"Ground-water possibilities south of the Snake River between Twin Falls and Pocatello, Idaho","docAbstract":"

The Snake River Plain and tributary valleys south of the Snake River between\nTwin Falls and Pocatello, Idaho (here called the South Side area), contain about\n180,000 acres of irrigated land, of which 145,000 acres is irrigated with surface\nwater and 35,000 is irrigated wholly or partly with ground water. The area also\ncontains more than 200,000 acres of arable land that is idle or used only for grazing\nbecause it lacks irrigation water. Most of the surface-water supply is already\nused or reserved, and some land now irrigated needs supplemental water.

\n
\n

The climate of the area ranges from semiarid on the Snake River Plain to\nsubhumid on higher mountains. The average annual precipitation at lowland\nstations ranges from about 9 to 12 inches.

\n\n

The principal sources of ground water are extrusive volcanic rocks of silicic\nto intermediate composition, basalt, and sand and gravel. Ground water occurs\ncommonly under artesian conditions in the silicic to intermediate volcanic rocks\nand in sand and gravel tongues and lenses in lake beds. Basalt and alluvium\ncommonly contain unconfined water.

\n
\n

The area of this report is divided into 13 roughly defined ground-water districts,\nsome of which are further divided into subdistricts. The known geologic\nand hydrologic factors of each area are summarized and a preliminary appraisal\nis made of the ground-water resources in relation to land resources and to the\nregimen of streams. The current state of development, proposed new developments,\nand ground-water potential of each division are discussed.

\n
\n

The Dry Creek district is the most intensively irrigated area in Idaho in which\nwells furnish the water supply. Ground water occurs under both artesian and\nwater-table conditions. More than 53,000 acre-feet of ground water was pumped\nin 1954. There are large areas of undeveloped arable land in the district, but\npumping in some parts of the district currently is approaching or surpasses the\nperennial yield of the ground-water reservoirs.

\n
\n

The Golden Valley district contains considerable arable land but, owing to\nthe relatively great depth to water and the generally poor yield of wells, the\nprospects for extensive ground-water development are not promising.

\n
\n

In the Oakley district ground water is pumped from alluvium to supplement\nsurface water and to bring new land into production. The ground water will be\nfully exploited within a few years if the present rate of development by individual\nlandowners continues. The total area of nonirrigated land far exceeds the amount\nthat could be irrigated with indigenous ground water.

\n
\n

Both artesian and unconfined water occur in the Burley district. Most existing\nwells tap unconfined water in the southern part where there are still large\ntracts of idle arable land. Pumping lifts are rather high.

\n
\n

The South Walcott district contains a considerable acreage of arable land and\nis underlain by excellent aquifers. The effect that heavy pumping would have\non the flow of the Raft and Snake Rivers and on seepage from Lake Walcott is\nTaot well understood. Presumably substantial pumping would be feasible without\ndirect deleterious effects.

\n
\n

The Raft River basin, including the Elba and Almo-Yost subbasins, is the\nlargest district in the South Side area. Ground water occurs in both unconfined\nand artesian aquifers. Possibly as much as 150,000 acres of dry land is irrigable,\nbut the ground-water supply presumably is sufficient to irrigate only a few thousand\nacres in addition to the approximately 40,000 now irrigated with surface\nand ground water. Pumping of wells at some locations would deplete the base\nflow of the Raft River and would be competitive with surface-water use.

\n
\n

The United States Bureau of Reclamation has started construction of the\nMichaud Flats Irrigation Project in the Western Michaud Flats district. The\nadopted reclamation plan is to irrigate about 10,000 acres, using surface water\npumped from American Falls Reservoir and ground water pumped from wells.\nGround water in part of the district is tributary to the reservoir. Withdrawals\nof ground water will be compensated in part by the return of waste water to the\nreservoir and to the Snake River.

\n
\n

The Eastern Michaud Flats district contains more arable land and has better\naquifers than the Western Michaud Flats district, but pumping might reduce\nnoticeably the discharge of ground water to the American Falls Reservoir. The\nBureau of Indian Affairs plans to develop about 13,600 acres of Indian land with\nwater stored in Palisades and American Falls Reservoirs.

\n
\n

Virtually nothing is known about ground-water conditions in the Arbon and\nRockland Valleys and in several small areas such as the Basin district, the\nAlbion basin, and along the northern border of the Sublett Range. Preliminary\nstudies have been made in three areas, the Dry Creek, Raft River, and Western.\nMichaud Flats districts. None has been studied comprehensively. The available\ndata for each district are summarized in tabular form.

\n
\n

Further investigations in the area are needed and should include accurate\nhydrologic mapping. Studies are needed of the sources and amounts of groundwater\nrecharge, of the effects of ground-water withdrawals on the total water\nsupply, and of numerous related problems.

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1460C","collaboration":"Prepared for the United States Bureau of Reclamation with the cooperation of the Idaho Department of Reclamation","usgsCitation":"Crosthwaite, E., 1957, Ground-water possibilities south of the Snake River between Twin Falls and Pocatello, Idaho: U.S. Geological Survey Water Supply Paper 1460, iv, 47 p., https://doi.org/10.3133/wsp1460C.","productDescription":"iv, 47 p.","startPage":"99","endPage":"145","numberOfPages":"51","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":137892,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1460c/report-thumb.jpg"},{"id":26138,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1460c/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho","city":"Pocatello;Twin Falls","otherGeospatial":"Snake River Plain","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -117.2681,41.9677 ], [ -117.2681,44.9959 ], [ -110.9949,44.9959 ], [ -110.9949,41.9677 ], [ -117.2681,41.9677 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa8e4b07f02db66744f","contributors":{"authors":[{"text":"Crosthwaite, E. G.","contributorId":83098,"corporation":false,"usgs":true,"family":"Crosthwaite","given":"E. G.","affiliations":[],"preferred":false,"id":143395,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2942,"text":"wsp1384 - 1957 - Surface water supply of the United States, 1955, Part II-B, South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","interactions":[],"lastModifiedDate":"2012-02-02T00:05:33","indexId":"wsp1384","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1384","title":"Surface water supply of the United States, 1955, Part II-B, South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1384","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1957, Surface water supply of the United States, 1955, Part II-B, South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River: U.S. Geological Survey Water Supply Paper 1384, x, 388 p. :ill. ;25 cm., https://doi.org/10.3133/wsp1384.","productDescription":"x, 388 p. :ill. ;25 cm.","costCenters":[],"links":[{"id":139123,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1384/report-thumb.jpg"},{"id":29651,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1384/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fcce0","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":528045,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2113,"text":"wsp1421 - 1957 - Geology and ground-water resources of Outagamie County, Wisconsin","interactions":[],"lastModifiedDate":"2015-10-05T09:02:03","indexId":"wsp1421","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1421","title":"Geology and ground-water resources of Outagamie County, Wisconsin","docAbstract":"

Outagamie County is in east-central Wisconsin. It has no serious groundwater problem at present, but the county is important as a recharge area for the principal aquifers supplying water to Brown County and industrial Green Bay to the east.

\n

The county is covered by glacial drift and lake deposits of the Wisconsin stage of glaciation. In the northwestern quarter of the county these deposits rest upon Precambrian crystalline rocks; throughout the remainder of the county they are underlain by sandstone, limestone, dolomite, and shale of Cambrian and Ordovician age. ·where they are sufficiently thick, and where more productive formations are absent, glacial sand and gravel are an important source of ground water. The major sources, however, are the St. Peter sandstone, of Ordovician age, and the sandstones of the Upper Cambrian series. The Precambrian crystalline rocks, which underlie all the county, yield little or no water to wells.

\n

The regional dip of the Paleozoic bedrocks is 25 to 30 feet per mile eastward and southeastward. There are no major folds, but the thickness of each geologic unit may change from place to place because of predepositional or postdepositional erosion. There is no conclusive evidence of major faulting in the area.

\n

Ground water in Outagamie County occurs under both water-table (unconfined) and artesian (confined) conditions. The source of the ground water is precipitation which falls on the surface and percolates downward into the underlying permeable materials. Regional movement of ground water in the eastern third of the county is controlled by the bedrock structure, and the discharge is toward the east and south. Throughout the rest of the county the movement of water is controlled mainly by bedrock and surface topography, and the water moves toward the streams and bedrock valleys.

\n

Water-level :fluctuations follow definite patterns. Where the effects of pumping are at a minimum, water levels reach a high in April or May, decline through the summer months owing to natural discharge, and lack of recharge, and do not begin to recover until after the ground thaws in the spring. In areas of heavy pumping where this pattern is distorted, the lowest water levels occur in the early fall and recoveries begin in October or November after the period of heaviest pumping.

\n

Pumpage in the county was estimated to be about 9.0 million gallons per day (mgd) in 1951 and 1952. Nearly half of this was for industrial, commercial, and public-supply use along the Fox River. Wells, most of which are drilled by the cable-tool method, range in diameter from 3 to 16 inches and in depth from 10 or 20 feet to 804 feet. In the alluvium and glacial drift 1~- to 2¥2-inch driven wells are common.

\n

Pumping tests were made to determine the hydraulic characteristics of the aquifers at Seymour, Appleton, and Hortonville. The average coefficient of transmissibility at Seymour is about 18,000 gpd per foot; at Appleton it is about 19,000 gpd per foot. The coefficients of storage are 0.00022 and 0.00015 at Seymour and Appleton, respectively. Movement of ground water out of the county, assuming an average transmissibility of 18,000 gpd per foot, was calculated to be more than 10 mgd toward the southeast.

\n

The ground water differs greatly in chemical quality from well to well, but it is generally a very hard calcium magnesium bicarbonate water, some of it high in iron. To aid in determining the source of well waters, 22 chemical analyses were plotted on a logarithmic diagram to obtain characteristic patterns for waters from several geologic sources.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1421","usgsCitation":"LeRoux, E.F., 1957, Geology and ground-water resources of Outagamie County, Wisconsin: U.S. Geological Survey Water Supply Paper 1421, Report: 57 p.; 7 Plates: 26.60 x 19.80 inches or smaller, https://doi.org/10.3133/wsp1421.","productDescription":"Report: 57 p.; 7 Plates: 26.60 x 19.80 inches or smaller","numberOfPages":"57","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":138327,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1421/report-thumb.jpg"},{"id":27696,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1421/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27695,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1421/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27689,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1421/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27693,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1421/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27694,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1421/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27690,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1421/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27691,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1421/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27692,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1421/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","county":"Outagamie County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-88.6062,44.5903],[-88.4889,44.5894],[-88.3671,44.5875],[-88.2453,44.5846],[-88.2203,44.5858],[-88.1908,44.5864],[-88.1918,44.5016],[-88.1921,44.4167],[-88.1921,44.3871],[-88.1919,44.3288],[-88.193,44.2421],[-88.2536,44.2432],[-88.2835,44.243],[-88.3754,44.2443],[-88.4041,44.244],[-88.4966,44.2443],[-88.5247,44.2441],[-88.6185,44.2438],[-88.6453,44.2435],[-88.7397,44.2432],[-88.7381,44.3307],[-88.7365,44.4164],[-88.7368,44.5021],[-88.7371,44.5906],[-88.6152,44.5903],[-88.6062,44.5903]]]},\"properties\":{\"name\":\"Outagamie\",\"state\":\"WI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db6859f8","contributors":{"authors":[{"text":"LeRoux, E. F.","contributorId":29795,"corporation":false,"usgs":true,"family":"LeRoux","given":"E.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":144693,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2368,"text":"wsp1330D - 1957 - Water requirements of the rayon- and acetate-fiber industry","interactions":[{"subject":{"id":2368,"text":"wsp1330D - 1957 - Water requirements of the rayon- and acetate-fiber industry","indexId":"wsp1330D","publicationYear":"1957","noYear":false,"chapter":"D","title":"Water requirements of the rayon- and acetate-fiber industry"},"predicate":"IS_PART_OF","object":{"id":70188911,"text":"wsp1330 - 1955 - Water requirements of selected industries","indexId":"wsp1330","publicationYear":"1955","noYear":false,"title":"Water requirements of selected industries"},"id":1}],"isPartOf":{"id":70188911,"text":"wsp1330 - 1955 - Water requirements of selected industries","indexId":"wsp1330","publicationYear":"1955","noYear":false,"title":"Water requirements of selected industries"},"lastModifiedDate":"2017-06-27T14:04:40","indexId":"wsp1330D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1330","chapter":"D","title":"Water requirements of the rayon- and acetate-fiber industry","docAbstract":"

Water is required for several purposes in the manufacture of rayon and acetate fiber. These water requirements, as indicated by a survey of the water used by the plants operating in 1953, are both quantitative and qualitative.

About 300 mgd (million gallons per day) of water was used in 1953 in the preparation of purified wood cellulose and cotton linters, the basic material from which the rayon and acetate fiber is made. An additional 620 mgd was used in the process of converting the cellulose to rayon and acetate fiber. The total, 920 mgd, is about 1 percent of the total estimated withdrawals of industrial water in the United States in 1953.

The rayon- and acetate-fiber plants are scattered through eastern United States and generally are located in small towns or rural areas where there are abundant supplies of clean, soft water. Water use at a typical rayon-fiber plant was about 9 mgd, and at a typical acetate-fiber plant about 38 mgd.

About 110 gallons of water was used to produce a pound of rayon fiber 32 gallons per pound was process water and the remainder was used largely for cooling in connection with power production and air conditioning. For the manufacture of a pound of acetate fiber about 170 gallons of water was used. However, the field survey on which this report is based indicated a wide range in the amount of water used per pound of product. For example, in the manufacture of viscose rayon, the maximum unit water use was 8 times the minimum unit water use. Water use in summer was about 22 percent greater than average annual use. About 8 mgd of water was consumed by evaporation in the manufacture of rayon and acetate fiber.

More than 90 percent of the water used by the rayon and acetate industry was withdrawn from surface-water sources, about 8 percent from ground water, and less than 2 percent from municipal water supplies.

All available analyses of the untreated waters used by the rayon and acetate industry were collected and studied. The untreated waters were generally cool, low in content of calcium and magnesium, and very low in iron and manganese. At many plants, water was obtained from more than one source, and thus had different quality characteristics. Dissolved solids in all the untreated waters analyzed ranged between 14 and 747 ppm (parts per million) but in those waters used in processing the dissolved solids content was less than 200 ppm.

The cooling water used by the industry is also generally of very high quality, principally because the requirements for a high-quality process water necessitate location of the plants in areas where such water is available.

","largerWorkTitle":"Water requirements of selected industries","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1330D","usgsCitation":"Mussey, O.D., 1957, Water requirements of the rayon- and acetate-fiber industry: U.S. Geological Survey Water Supply Paper 1330, vi, 39 p., https://doi.org/10.3133/wsp1330D.","productDescription":"vi, 39 p.","startPage":"141","endPage":"179","costCenters":[],"links":[{"id":28307,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1330d/report.pdf","text":"Report","size":"867.98 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":137742,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1330d/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e47c8e4b07f02db4ab9b1","contributors":{"authors":[{"text":"Mussey, Orville Durey","contributorId":45688,"corporation":false,"usgs":true,"family":"Mussey","given":"Orville","email":"","middleInitial":"Durey","affiliations":[],"preferred":false,"id":145088,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2941,"text":"wsp1383 - 1957 - Surface water supply of the United States, 1955, Part II-A, South Atlantic slope and eastern Gulf of Mexico basins, James River to Savannah River","interactions":[],"lastModifiedDate":"2012-02-02T00:05:30","indexId":"wsp1383","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1383","title":"Surface water supply of the United States, 1955, Part II-A, South Atlantic slope and eastern Gulf of Mexico basins, James River to Savannah River","language":"ENGLISH","publisher":"U.S. Government Printing Office,","doi":"10.3133/wsp1383","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1957, Surface water supply of the United States, 1955, Part II-A, South Atlantic slope and eastern Gulf of Mexico basins, James River to Savannah River: U.S. Geological Survey Water Supply Paper 1383, viii, 314 p. : tables ;25 cm., https://doi.org/10.3133/wsp1383.","productDescription":"viii, 314 p. : tables ;25 cm.","costCenters":[],"links":[{"id":138684,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1383/report-thumb.jpg"},{"id":29650,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1383/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afbe4b07f02db69605e","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":528044,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":14976,"text":"ofr5772 - 1957 - Geology of possible petroleum provinces in Alaska","interactions":[{"subject":{"id":14976,"text":"ofr5772 - 1957 - Geology of possible petroleum provinces in Alaska","indexId":"ofr5772","publicationYear":"1957","noYear":false,"title":"Geology of possible petroleum provinces in Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":35230,"text":"b1094 - 1959 - Geology of possible petroleum provinces in Alaska","indexId":"b1094","publicationYear":"1959","noYear":false,"title":"Geology of possible petroleum provinces in Alaska"},"id":1}],"supersededBy":{"id":35230,"text":"b1094 - 1959 - Geology of possible petroleum provinces in Alaska","indexId":"b1094","publicationYear":"1959","noYear":false,"title":"Geology of possible petroleum provinces in Alaska"},"lastModifiedDate":"2024-05-03T22:50:46.949424","indexId":"ofr5772","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"57-72","title":"Geology of possible petroleum provinces in Alaska","docAbstract":"

The history of petroleum exploration in Alaska and the geology of possible petroleum provinces in Alaska are reviewed. Maps showing Alaska's major Mesozoic and Tertiary tectonic elements, possible petroleum provinces, and indications of petrol, are included in this report. Annotated references in Geological Survey publications relating to petroleum and oil shale in Alaska are given at the end of the report.

For the purpose of appraising its petroleum possibilities, Alaska is divided into the southern, central, and northern major geologic-physiographic regions.

Southern Alaska includes the arcuate mountain chain formed by the Alaska and Aleutian Ranges and the Mentasta- Nutzotin Mountains, the coastal range and valley area to the south, and the southeastern Alaska \"panhandle\" -- an area of 185,000 square miles.

Oil seeps on the west shore of Cook Inlet in southern Alaska were known as early as 1853, and claims were staked in this region in 1882. Drilling began near the oil seeps in the Katalla district about 1901, and this started Alaska's first period of oil activity. From 1902 to 1933 the Katalla field produced 154,000 barrels of oil from fractured shale and sandstone of Tertiary age the- first and only commercial production in Alaska.

On the basis of geology, surficial indications of petroleum, and test wells drilled, six possible petroleum provinces are indicated in southern Alaska. They are Heceta Island area, Keku Islands area, Cook Inlet Mesozoic province, Gulf of Alaska Tertiary province, Cook Inlet Tertiary province, and Copper River basin.

The exposed rocks in the Heceta Island area include lower Paleozoic graywacke-type sandstone, sandstone, conglomerate, and massive limestones with reeflike structures; igneous rocks are rare or lacking in much of the area. The Kosciusko-Tuxekan-Heceta synclinorium, the main structural feature, is modified by minor folds and faults. Some of the minor folds are reported to be broad and open, with flanks dipping 20°-145°. As far as known, the Heceta Island area has not heretofore been seriously considered as a possible petroleum province.

Rocks of Silurian to Cretaceous age are exposed in the Keku Island area and include moderately folded and relatively unaltered limestone and other marine sedimentary rocks.

The Cook Inlet Mesozoic province, a land area of approximately 18,500 square miles, includes a great thickness of unmetamorphosed marine sedimentary rocks of Jurassic and Cretaceous age. At least 23 test wells were drilled or started in this province by the end of 1955. Shows of oil and gas were encountered in many of these wells. During 1955 at least ten oil companies were active in this area and by the end of 1955 about 1 1/2 million acres were included in oil and gas leases applied for or granted.

The Gulf of Alaska Tertiary province includes about 5,200 square miles in which rocks of Tertiary age are exposed or are believed to underlie Quaternary deposits. Between 1901 and the end of 1955 about 47 wells were drilled or started in this province.

The Cook Inlet Tertiary province embraces an area of about 9,500 square miles, of which about 4,100 is covered by the shallow waters of Cook Inlet. Petroleum exploration has been in that part of the area which overlaps the Cook Inlet Mesozoic province. Eocene or younger Tertiary nonmarine sedimentary rocks are believed to underlie much of the province, and marine rocks of Tertiary age may also be present.

The Copper River basin is a topographic basin underlain by unconsolidated deposits of Quaternary age. Tertiary rocks favorable for the accumulation of petroleum may underlie part of the basin but this is not believed likely. Except for some leasing activity no petroleum exploration has been recorded in the Copper River Basin to the end of 1955.

Central Alaska is a region of about 275,000 square miles and consists of an irregular assemblage of intricately dissected uplands and alluvium-floored lowland basins. Scattered peaks of resistant intrusive igneous rocks surmount most of the upland areas.

In the vast region of central Alaska only six test wells are known to have been drilled for the purpose of finding oil and gas. The maximum depth reached was 350 feet and the holes were mostly or entirely in Quaternary deposits. In recent years several oil companies have investigated some parts of the region and large areas in the Yukon-Koyukuk province are now under lease. Oil seeps, gas seeps, and other indications of petroleum have been reported from many localities; samples from two localities have been analyzed and reported to be petroleum.

The geology of central Alaska is similar in a general way to that of the area between the Rocky Mountains and Sierra-Cascade belts of the United States. Sedimentary rocks, probably equivalent to the Precambrian Belt series, and rocks of the Cambrian and all younger geologic systems have been recognized in central Alaska. The structure of the region is known to be complex, but except in local mineral districts, it has not been mapped in detail. Based on the limited amount of available information, the region cannot be regarded as distinctly favorable for significant accumulations of petroleum. However, three pre-Cenozoic provinces, the Yukon-Koyukuk, the Kobuk, and the Kandik, and several large Cenozoic basin provinces may be worthy of further investigation.

Northern Alaska includes the Brooks Range and all the treeless tundra north to the Arctic Coast, an area of about 125,000 square miles. The presence of oil seeps along the Arctic Coast has been known at least since 1900 and a description of the Cape Simpson oil seeps vas published in 1909. Since then oil and gas seeps have been described from nine localities, and oil shales and oil-bearing sandstones are known from many localities in the Arctic Foothills province. Oil and gas deposits have been discovered and geologic conditions are favorable for oil and gas accumulations in approximately half of the region.

In 1923 approximately 37,000 square miles in northern Alaska was reserved by Executive order as Naval Petroleum Reserve No. 4. In 1944 the U. S. Navy began a vast petroleum exploration program which was suspended in 1953. In the years 1945 through 1955, 37 test wells and 45 core tests were drilled on 18 structures. Three oil fields, Umiat, Simpson, and Fish Creek, and two gas fields, South Barrow and Gubik, were discovered. Total reserve estimates for all discoveries of oil to 1955 range from 30 to 100 million barrels, and for gas, from 370 billion to 900 billion cubic feet.

All northern Alaska, with the exception of the Brooks Range, can be considered a possible petroleum province, but the region can be subdivided into provinces of somewhat different potentialities. These subdivisions roughly correspond with the geomorphic provinces and sections, which in turn reflect differences in geology. The known oil-bearing beds are of Mesozoic age, primarily Cretaceous, and thus the possible petroleum provinces could be designated as Mesozoic. However, Paleozoic and Cenozoic rocks with favorable reservoir characteristics are exposed in the region and possibly underlie, in favorable structural situations, some of the areas as yet not tested.

The Arctic Coastal Plain province includes gently folded and flat-lying Mesozoic beds that overlie a basement complex of Paleozoic and early Mesozoic age. Near the southern edge of this province the basement rocks are at depths of at least 20,000 feet, and to the north these rocks rise to within 2,500 feet of the surface.

The Teshukpuk Lake section of the Arctic Coastal plain includes many of the known oil seeps; it is the most accessible to sea transportation, and lies almost completely within NPR 4. Thirteen test wells and 35 core tests have been drilled here; one gas field and two (at present, noncommercial) oil fields have been discovered. The possibility of further discoveries may depend largely on locating porous sandstones in stratigraphic rather than anticlinal traps.

The White Hills section is distinguished topographically from the Teshukpruk section by its white-gravel-covered hills and fever lakes, and geologically by the presence of Tertiary rocks, including 2,000 feet of nonmarine beds in the west and at least 7,000 feet of marine beds to the east, in the vicinity of Carter Creek. This section appears to be more complex structurally. No test wells have been drilled in the White Hills section.

The Northern Foothills section includes many closed anticlines. Twenty-four test wells and ten core tests have been drilled on 11 structures and two discoveries have been made -the Umiat oil field and the Gubik gas field. All these tests have been drilled in Cretaceous rocks.

The Southern Foothills section is structurally similar to the Alberta Foothills and to the northern part of the Brooks Range. Great thicknesses of marine shale of Lover Cretaceous, Jurassic, and Triassic age are exposed. The outcropping Mesozoic sandstones are generally poorly sorted, nonporous, and impermeable. To the south the section is bordered by mountainous exposures of Mississippian limestone, which probably underlie at least part of this section.

The rocks that underlie the deeply eroded complex structures of the Brooks Range include schist, slate, argillite, and limestone. Some exposed limestones have a strong petroleum-like odor and contain traces of petroleum residues.



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p.; Plate 1: 37.65 inches x 30.80 inches; Plate 2: 34.68 inches x 27.29 inches, https://doi.org/10.3133/tem1053.","productDescription":"Report 3 p.; Plate 1: 37.65 inches x 30.80 inches; Plate 2: 34.68 inches x 27.29 inches","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":284752,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/1053/plate-1.pdf"},{"id":284753,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/1053/plate-2.pdf"},{"id":284754,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tem/1053/report.pdf"},{"id":278710,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"South Dakota","county":"Fall River County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.5625,43.291667 ], [ -103.5625,43.333333 ], [ 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https://doi.org/10.3133/tem1059.","productDescription":"Report: 2 p.; Plate: 36.30 inches x 31.78 inches","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":278857,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":284775,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/1059/plate-1.pdf"},{"id":284776,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tem/1059/report.pdf"}],"country":"United States","state":"South Dakota","county":"Fall River County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.9375,43.416667 ], [ -103.9375,43.458333 ], [ -103.8750,43.458333 ], [ -103.8750,43.416667 ], [ -103.9375,43.416667 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd6d37e4b0b29085105085","contributors":{"authors":[{"text":"Schnabel, R. 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The Salt Wash is the basal member of the Upper Jurassic Morrison Formation in parts of Utah, Colorado, Arizona, and New Mexico. Deposited by streams, it comprises lenticular beds of cross-laminated sandstone irregularly interbedded with mudstone, siltstone, claystone, and horizontally laminated sandstone. The term \"lithofacies,\" as used in this paper, denotes lithologic aspect. The specific lithofacies of the Salt Wash member at a given locality is determined by the thickness, proportion, and continuity of the stream and flood-plain deposits that make up the Salt Wash. Stream deposits include all rocks interpreted as deposited from moving water; flood-plain deposits include all rocks interpreted as deposited from slack water. Regional differences in lithofacies show that the Salt Wash member is a fan-shaped wedge of sedimentary rocks whose apex is in south-central Utah. Within the wedge, the thickness of the Salt Wash and the thickness, proportion, and continuity of the contained stream deposits decrease relatively uniformly to the north, northeast, and southeast of the apex. Interpretation of the regional differences in lithofacies indicates deposition by a distributary stream system whose apex was in south-central Utah and which spread sediments to the north, east, and southeast over a nearly flat plain. Irregularities on this plain near the Four Corners area and in west-central Colorado modified the distributary system, and therefore the wedge is not symmetrical. Most uranium-vanadium ore deposits in the Salt Wash member occur in a lithofacies near the center of the wedge. This may be a genetic relation and can be explained as a function of transmissibility of the particular lithofacies. The ore deposits, however, are concentrated in a relatively small part of the central lithofacies. Because local geologic features such as structure or igneous intrusions might control the localization of ore deposits in the small area, the high degree of correlation of ore deposits and a certain lithofacies may be coincidental. © 1957, The Geological Society of America, Inc.

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\"}}]}","volume":"68","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Mullens, T. E.","contributorId":34573,"corporation":false,"usgs":true,"family":"Mullens","given":"T.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":775317,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Freeman, V. L.","contributorId":52958,"corporation":false,"usgs":true,"family":"Freeman","given":"V.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":775318,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70197728,"text":"70197728 - 1957 - Franciscan group in Coast Ranges and its equivalents in Sacramento Valley, California","interactions":[],"lastModifiedDate":"2023-02-01T14:44:20.871456","indexId":"70197728","displayToPublicDate":"1957-12-31T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":701,"text":"American Association of Petroleum Geologists Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Franciscan group in Coast Ranges and its equivalents in Sacramento Valley, California","docAbstract":"

The Franciscan group is an assemblage of detrital and chemical sedimentary and volcanic rocks that crops out discontinuously in a structurally complex, northwesterly trending belt along the Coast Ranges of Cahfornia. On the east, along the west side of the Sacramento Valley, a thick section of detrital sedimentary rocks has been subdivided into the Knoxville, Paskenta, and Horsetown forma tions of Late Jurassic and Early Cretaceous age, and several units of early Late Cretaceous age. The Sacramento Valley section represents deposition during most of the time from Late Jurassic to early Late Cretaceous.

The Franciscan group is widely held to be restricted to Late Jurassic age, the Knoxville formation to be an upper shaly phase of the Franciscan group, and the two to be overlain unconformably by detrital strata of Cretaceous age. Sparse paleontologic evidence indicates this view to be incorrect. Rather, the Franciscan group seems mainly to have been deposited contemporaneously with the Knoxville, Paskenta, Horsetown, and lower Upper Cretaceous strata, as fossils ranging from Late Jurassic to early Late Cretaceous in age have been found in the Franciscan group. The Franciscan group and strata of the Sacramento Valley section therefore may represent two fades of the same stratigraphic section.

","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/0BDA598D-16BD-11D7-8645000102C1865D","usgsCitation":"Irwin, W., 1957, Franciscan group in Coast Ranges and its equivalents in Sacramento Valley, California: American Association of Petroleum Geologists Bulletin, v. 41, no. 10, p. 2284-2297, https://doi.org/10.1306/0BDA598D-16BD-11D7-8645000102C1865D.","productDescription":"14 p.","startPage":"2284","endPage":"2297","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":355155,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Coast Ranges, Sacramento Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -120.37565386102392,\n 35.43697381907357\n ],\n [\n -119.56766784450022,\n 35.756423682247146\n ],\n [\n -121.26063833013268,\n 38.958627533836875\n ],\n [\n -122.39424444228172,\n 40.46413166128349\n ],\n [\n -123.63732039385647,\n 40.748395672260216\n ],\n [\n -123.58010245482978,\n 41.9121390843971\n ],\n [\n -124.29984848942979,\n 41.90701007677032\n ],\n [\n -124.08823796557783,\n 40.959378695262984\n ],\n [\n -124.37981704914156,\n 40.314101124394995\n ],\n [\n -123.85452818235751,\n 39.535918156217065\n ],\n [\n -123.70880379131722,\n 38.89660014813049\n ],\n [\n -122.97653408073239,\n 37.93776287592166\n ],\n [\n -122.39459687777702,\n 37.13215129931295\n ],\n [\n -121.73102873565779,\n 36.533638813884764\n ],\n [\n -120.35395583583437,\n 35.41809758668549\n ],\n [\n -120.37565386102392,\n 35.43697381907357\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"41","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Irwin, William P.","contributorId":12889,"corporation":false,"usgs":true,"family":"Irwin","given":"William P.","affiliations":[],"preferred":false,"id":738312,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70216354,"text":"70216354 - 1957 - Eastern and central Montana as a possible source area of uranium","interactions":[],"lastModifiedDate":"2020-11-12T21:03:58.228527","indexId":"70216354","displayToPublicDate":"1957-11-12T14:53:42","publicationYear":"1957","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":"Eastern and central Montana as a possible source area of uranium","docAbstract":"

Geologic settings in central and eastern Montana and in a few places in southwestern Montana are similar to the settings in areas favorable for the occurrence of uranium deposits. Several areas in Montana seem especially favorable for the occurrence of uranium.The alkalic igneous rock province of central Montana is similar to the one of the Colorado Plateau. On the basis of this analogy, certain areas in Montana, where the lithology and (or) structure are considered favorable for the occurrence of uranium, are suggested for prospecting. Seleniferous plants, similar to those that are uranium indicators on the Colorado Plateau, might be used as an aid in prospecting for uranium provided that the seleniferous shale areas are taken into account.Uranium deposits, similar to those in North and South Dakota, may be found in Cretaceous and Tertiary sandstones, lignites, and low-grade coals of eastern Montana; also, the magnetite-bearing beds of certain Cretaceoussandstones may contain fossil placer deposits of radioactive black minerals. Theoccurrence of uranium in basal conglomerates, quartzites, and sandstones in Africa and Ontario suggests that similar basal sedimentary rocks in central Montana may contain uranium.Many of the radioactivity anomalies in Montana found from the air are closely associated with the Eagle sandstone; others are associated with Precambrian basement rocks, Upper Cretaceous and Lower Tertiary igneous rocks, or sedimentary rocks of Jurassic and Cretaceous age. Glacial cover and lack of outcrops locally may hinder prospecting for uranium.

","language":"English","publisher":"Society of Economic Geologist","doi":"10.2113/gsecongeo.52.3.211","usgsCitation":"Armstrong, F.C., 1957, Eastern and central Montana as a possible source area of uranium: Economic Geology, v. 52, no. 3, p. 211-224, https://doi.org/10.2113/gsecongeo.52.3.211.","productDescription":"14 p.","startPage":"211","endPage":"224","costCenters":[],"links":[{"id":480408,"rank":0,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://digital.library.unt.edu/ark:/67531/metadc502288/","text":"External Repository"},{"id":380485,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","otherGeospatial":"Central and eastern Montana","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -110.0390625,\n 44.96479793033101\n ],\n [\n -110.0390625,\n 48.980216985374994\n ],\n [\n -116.3671875,\n 49.095452162534826\n ],\n [\n -116.21337890625,\n 48.07807894349862\n ],\n [\n -115.7080078125,\n 47.204642388766935\n ],\n [\n -114.47753906249999,\n 46.5739667965278\n ],\n [\n -114.60937499999999,\n 45.66012730272194\n ],\n [\n -113.90625,\n 45.398449976304086\n ],\n [\n -113.26904296874999,\n 44.26093725039923\n ],\n [\n -111.09374999999999,\n 44.402391829093915\n ],\n [\n -111.09374999999999,\n 44.96479793033101\n ],\n [\n -110.0390625,\n 44.96479793033101\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"52","issue":"3","noUsgsAuthors":false,"publicationDate":"1957-05-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Armstrong, Frank Clarkson","contributorId":19559,"corporation":false,"usgs":true,"family":"Armstrong","given":"Frank","email":"","middleInitial":"Clarkson","affiliations":[],"preferred":false,"id":804789,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":62863,"text":"gq98 - 1957 - Carlsbad Caverns East quadrangle, New Mexico","interactions":[],"lastModifiedDate":"2023-12-12T20:56:13.202383","indexId":"gq98","displayToPublicDate":"1957-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":316,"text":"Geologic Quadrangle","code":"GQ","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"98","title":"Carlsbad Caverns East quadrangle, New Mexico","docAbstract":"

No abstract available.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/gq98","usgsCitation":"Hayes, P.T., 1957, Carlsbad Caverns East quadrangle, New Mexico: U.S. Geological Survey Geologic Quadrangle 98, Report: 2 p.; 1 Plate, https://doi.org/10.3133/gq98.","productDescription":"Report: 2 p.; 1 Plate","costCenters":[],"links":[{"id":102578,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_1027.htm","linkFileType":{"id":5,"text":"html"},"description":"1027"},{"id":251683,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gq/0098/report-thumb.jpg"},{"id":249010,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gq/0098/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New Mexico","otherGeospatial":"Carlsbad Caverns East quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -104.5,32 ], [ -104.5,32.25 ], [ -104.25,32.25 ], [ -104.25,32 ], [ -104.5,32 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f4e4b07f02db5efe86","contributors":{"authors":[{"text":"Hayes, P. T.","contributorId":17655,"corporation":false,"usgs":true,"family":"Hayes","given":"P.","email":"","middleInitial":"T.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":267972,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2054,"text":"wsp1425 - 1957 - Ground water in the Crow Creek-Sand Lake area, Brown and Marshall Counties, South Dakota","interactions":[{"subject":{"id":55773,"text":"ofr5758 - 1957 - Geology and ground-water hydrology of the Oahe unit, James River division, South Dakota: Appendixes A, B, C, and E","indexId":"ofr5758","publicationYear":"1957","noYear":false,"title":"Geology and ground-water hydrology of the Oahe unit, James River division, South Dakota: Appendixes A, B, C, and E"},"predicate":"SUPERSEDED_BY","object":{"id":2054,"text":"wsp1425 - 1957 - Ground water in the Crow Creek-Sand Lake area, Brown and Marshall Counties, South Dakota","indexId":"wsp1425","publicationYear":"1957","noYear":false,"title":"Ground water in the Crow Creek-Sand Lake area, Brown and Marshall Counties, South Dakota"},"id":1}],"lastModifiedDate":"2023-03-10T22:11:02.910751","indexId":"wsp1425","displayToPublicDate":"1957-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1425","title":"Ground water in the Crow Creek-Sand Lake area, Brown and Marshall Counties, South Dakota","docAbstract":"

The Crow Creek Sand Lake area is in the northeastern part of South Dakota and consists of flat to gently rolling land. It is roughly 25 miles square and is bounded on the west by the James River, on the north by the North Dakota State line, and on the south and east by arbitrary land lines. Natural drainage, which is very poor, is augmented by a now very dilapidated system of man made drains; undrained or poorly drained potholes and sloughs are common. Most of the report area is in the drainage basin of Crow Creek, a tributary of the James River. About 60 square miles along the west border of the area is drained directly by the James River; and about 36 square miles in the northeastern corner of the area is drained by the Wild Rice River, a tributary of the Red River of the North.

\n

Granite and other related rocks of Precambrian age underlie the entire area below a depth of about 1,100 to 1,200 feet. Under part of the area these rocks are overlain by the Sioux quartzite, also of Precambrian age. Next above is the Dakota sandstone of Cretaceous age, which is about 250 feet thick and is the aquifer tapped by more than 600 deep wells in the area. The Dakota sandstone in turn is overlain by younger formations of Cretaceous age, which include the Graneros shale, Greenhorn limestone, Carlile shale, Niobrara formation, and Pierre shale. These younger formations have an aggregate thickness of about 700 to 950 feet and generally do not yield water. Mantling, the consolidated stratified rocks are unconsolidated deposits of Quaternary age that are absent locally but in places are as much as 200 feet thick. These deposits consist principally of glacial outwash, glacial till, and lake sediments and are the source of water for all shallow wells in the area.

\n

Precipitation is the principal source of recharge to the ground-water reservoir tapped by the shallow wells. The water table ranges in depth from less than 1 foot to a little more than 30 feet below the land surface; in July 1951 the depth to water was less than 5 feet in 15 percent of the area and 5 to 10 feet in an additional 25 percent of the area. Because the hydraulic gradient in most of the area is less than 10 feet per mile and because much of the water-bearing material is only slightly permeable, lateral movement of the ground water in the unconsolidated deposits is exceedingly slow.

\n

Transpiration by vegetation and evaporation account for most of the ground water discharged in the area; relatively little ground water is discharged by streams, wells, and springs, or as underflow out of the area. Much of the low-lying land is waterlogged. However, by improving and cleaning both the natural and artifical drains and by lowering the water table by pumping, waterlogging can be materially decreased and its recurrence prevented.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, DC","doi":"10.3133/wsp1425","usgsCitation":"Koopman, F.C., 1957, Ground water in the Crow Creek-Sand Lake area, Brown and Marshall Counties, South Dakota: U.S. Geological Survey Water Supply Paper 1425, Report: iv, 125 p.; 7 Plates: 20.00 x 19.00 inches or smaller, https://doi.org/10.3133/wsp1425.","productDescription":"Report: iv, 125 p.; 7 Plates: 20.00 x 19.00 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":413982,"rank":10,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24379.htm","linkFileType":{"id":5,"text":"html"}},{"id":27590,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1425/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27589,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1425/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27588,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1425/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27587,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1425/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27586,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1425/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27585,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1425/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27584,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1425/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27583,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1425/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138460,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1425/report-thumb.jpg"}],"country":"United States","state":"North Dakota","county":"Brown County, Marshall County","otherGeospatial":"Crow Creek-Sand Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -98.208,\n 45.933\n ],\n [\n -98.208,\n 45.5\n ],\n [\n -97.6,\n 45.5\n ],\n [\n -97.6,\n 45.933\n ],\n [\n -98.208,\n 45.933\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66d9c7","contributors":{"authors":[{"text":"Koopman, F. C.","contributorId":40586,"corporation":false,"usgs":true,"family":"Koopman","given":"F.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":144603,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70195913,"text":"70195913 - 1957 - On the postglacial history of the Devils Lake Region, North Dakota","interactions":[],"lastModifiedDate":"2018-03-07T16:12:57","indexId":"70195913","displayToPublicDate":"1957-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3566,"text":"The Journal of Geology","active":true,"publicationSubtype":{"id":10}},"title":"On the postglacial history of the Devils Lake Region, North Dakota","docAbstract":"

Devils and Stump lakes in eastern North Dakota have been diminishing in area more or less continuously since the land around them was settled in the 1880's. Desiccations similar to the current one have occurred at least once and possibly two or more times in the past and are indicated directly and indirectly by tree stumps recently uncovered as the lake water receded and by lacustrine deposits containing buried soils and vertebrate remains. The lake levels seem to respond in a very sensitive manner to slight climatic changes. Probably the present desiccation and certainly the ones in the past are the result of changes toward a drier and warmer climate. The first may have been synchronous with the Thermal Maximum. A high abandoned strand line and associated lacustrine deposits containing buried soils and vertebrate remains indicate at least one period in the postglacial past, possibly following the Thermal Maximum, that was wetter and cooler than the present. A second desiccation, more definitely established and based on the radiocarbon dating of a tree stump, occurred less than 700 years ago, possibly during the sixteenth century.

","language":"English","publisher":"The University of Chicago Press","doi":"10.1086/626442","usgsCitation":"Aronow, S., 1957, On the postglacial history of the Devils Lake Region, North Dakota: The Journal of Geology, v. 65, no. 4, p. 410-427, https://doi.org/10.1086/626442.","productDescription":"18 p.","startPage":"410","endPage":"427","costCenters":[{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":352308,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"North Dakota","otherGeospatial":"Devils Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -99.3109130859375,\n 47.74486433470359\n ],\n [\n -98.30841064453125,\n 47.74486433470359\n ],\n [\n -98.30841064453125,\n 48.37723330604312\n ],\n [\n -99.3109130859375,\n 48.37723330604312\n ],\n [\n -99.3109130859375,\n 47.74486433470359\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"65","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5aff669ae4b0da30c1bfe15d","contributors":{"authors":[{"text":"Aronow, Saul","contributorId":59509,"corporation":false,"usgs":true,"family":"Aronow","given":"Saul","email":"","affiliations":[],"preferred":false,"id":730481,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":76921,"text":"tem951 - 1956 - Tectonic map of Wyoming, east of the overthrust belt, showing the distribution of uranium deposits","interactions":[],"lastModifiedDate":"2014-07-23T13:51:31","indexId":"tem951","displayToPublicDate":"2013-07-23T13:50:00","publicationYear":"1956","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":338,"text":"Trace Elements Memorandum","code":"TEM","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"951","title":"Tectonic map of Wyoming, east of the overthrust belt, showing the distribution of uranium deposits","docAbstract":"No abstract available.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/tem951","collaboration":"Performed for the Division of Raw Materials, U.S. Atomic Energy Commission.","usgsCitation":"Osterwald, F.W., and Dean, B.G., 1956, Tectonic map of Wyoming, east of the overthrust belt, showing the distribution of uranium deposits: U.S. Geological Survey Trace Elements Memorandum 951, 40 p., https://doi.org/10.3133/tem951.","productDescription":"40 p.","costCenters":[],"links":[{"id":290824,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"Wyoming","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -111.0569,40.9947 ], [ -111.0569,45.0059 ], [ -104.0522,45.0059 ], [ -104.0522,40.9947 ], [ -111.0569,40.9947 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57ffd416e4b0824b2d1770f3","contributors":{"authors":[{"text":"Osterwald, Frank W.","contributorId":98301,"corporation":false,"usgs":true,"family":"Osterwald","given":"Frank","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":288154,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dean, Basil Gray","contributorId":60288,"corporation":false,"usgs":true,"family":"Dean","given":"Basil","email":"","middleInitial":"Gray","affiliations":[],"preferred":false,"id":288153,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70046293,"text":"70046293 - 1956 - Heavy-mineral suites in unconsolidated Paleocene and younger sands, western Tennessee","interactions":[{"subject":{"id":51614,"text":"ofr5423 - 1954 - Heavy minerals suites in the unconsolidated sands of Paleocene age and younger in western Tennessee","indexId":"ofr5423","publicationYear":"1954","noYear":false,"title":"Heavy minerals suites in the unconsolidated sands of Paleocene age and younger in western Tennessee"},"predicate":"SUPERSEDED_BY","object":{"id":70046293,"text":"70046293 - 1956 - Heavy-mineral suites in unconsolidated Paleocene and younger sands, western Tennessee","indexId":"70046293","publicationYear":"1956","noYear":false,"title":"Heavy-mineral suites in unconsolidated Paleocene and younger sands, western Tennessee"},"id":1}],"lastModifiedDate":"2020-10-15T15:25:46.418027","indexId":"70046293","displayToPublicDate":"2013-01-01T00:00:00","publicationYear":"1956","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2450,"text":"Journal of Sedimentary Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Heavy-mineral suites in unconsolidated Paleocene and younger sands, western Tennessee","docAbstract":"

Heavy-mineral suites from unconsolidated sands of Wilcox and Claiborne age (Eocene) in the subsurface of western Tennessee were tabulated and compared with heavy-mineral suites obtained from outcropping sands known to be of Midway (Paleocene) and Wilcox age and younger. In the subsurface at Memphis, both pink and colorless garnet are relatively abundant in the Claiborne but rare in the Wilcox. Garnet, however, is very rare in both the Claiborne and the Wilcox in the subsurface 35 miles northeast of Memphis. The mineral is very rare also in the terrace sands of western Tennessee and in samples of the Pliocene(?) and Pleistocene deposits of the Tennessee River in eastern and western Tennessee. It is possible, therefore, that the relative abundance of the mineral garnet is related to the quantity of sediment received from differing source areas in Wilcox and Claiborne times, but that, owing to the shifting of the axis of the embayment, no one source area furnished all the sediment for any formation. Heavy-mineral suites from Pliocene(?) and Pleistocene terrace deposits of the Tennessee River in both eastern and western Tennessee, and heavy-mineral suites from Pliocene(?) deposits of the Mississippi River are much alike, and the only isotropic mineral noted in these sediments was a very rare green mineral. Heavy-mineral suites from Recent deposits of the Mississippi River at Memphis and reported heavy-mineral suites from Cambrian sandstones of Wisconsin and Minnesota differ greatly from heavy-mineral suites of Pliocene(?) terrace deposits of the Tennessee and Mississippi Rivers and include much pink and colorless garnet. The possibility, therefore, is suggested that the Pliocene(?) terrace deposits of the Mississippi River in western Tennessee were derived largely from the basin of the Tennessee River.

","language":"English","publisher":"American Geological Institute","doi":"10.1306/74D70632-2B21-11D7-8648000102C1865D","usgsCitation":"Blankenship, R.R., 1956, Heavy-mineral suites in unconsolidated Paleocene and younger sands, western Tennessee: Journal of Sedimentary Petrology, v. 26, no. 4, p. 356-362, https://doi.org/10.1306/74D70632-2B21-11D7-8648000102C1865D.","productDescription":"7 p.","startPage":"356","endPage":"362","costCenters":[],"links":[{"id":273298,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Tennessee","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -90.3103,34.9829 ], [ -90.3103,36.678 ], [ -81.6469,36.678 ], [ -81.6469,34.9829 ], [ -90.3103,34.9829 ] ] ] } } ] }","volume":"26","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"51b05de5e4b030b519801214","contributors":{"authors":[{"text":"Blankenship, Reginald R.","contributorId":69875,"corporation":false,"usgs":true,"family":"Blankenship","given":"Reginald","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":479391,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":76935,"text":"tem901 - 1956 - Geology of the Ralston Buttes district, Jefferson County, Colorado: a preliminary report","interactions":[],"lastModifiedDate":"2014-03-10T14:45:42","indexId":"tem901","displayToPublicDate":"2012-09-11T13:29:00","publicationYear":"1956","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":338,"text":"Trace Elements Memorandum","code":"TEM","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"901","title":"Geology of the Ralston Buttes district, Jefferson County, Colorado: a preliminary report","docAbstract":"The Ralston Buttes district in Jefferson County is one of the most significant new uranium districts located east of the Continental Divide in Colorado. The district is east of the Colorado Front Range mineral belt, along the east front of the range. From November 1953 through October 1956, about 10,000 tons of uranium ore, much of which was high-grade pitchblende-bearing vein material, was shipped from the district. The ore occurs in deposits that range in size from bodies containing less than 50 tons to ore shoots containing over 1,000 tons. The only other mining activity in the area has been a sporadic production of beryl, feldspar, and scrap mica from Precambrian pegmatites, and quarrying of dimension stone, limestone, and clay from sedimentary rocks. Most of the Ralston Buttes district consists of complexly folded Precambrian metamorphic and igneous rocks - gneiss, schist, quartzite, amphibolite, and granodiorite. Paleozoic and Mesozoic sedimentary rocks crop out in the northeastern part of the district. These rocks are cut by northwesterly-trending fault systems of Laramide age and by small bodies of intrusive rocks that are Tertiary in age. The typical uranium deposits in the district are hydrothermal veins occupying openings in Laramide fault breccias or related fractures that cut the Precambrian rocks. Pitchblende and lesser amounts of secondary uranium minerals are associated with sparse base-mental sulfides in a gangue of carbonate minerals, potash feldspar, and, more rarely, quartz. Less common types of deposits consist of pitchblende and secondary uranium minerals that occupy fractures cutting pegmatites and quartz veins. The uranium deposits are concentrated in two areas, the Ralston Creek area and the Golden Gate Canyon area. The deposits in the Ralston Creek area are located along the Rogers fault system, and the deposits in the Golden Gate Canyon area are along the Hurricane Hill fault system. Two geologic factors were important to the localization of the uranium deposits: (1) favorable structural environment and (2) favorable host rocks. The deposits in each of the two major areas are located where a northwesterly-trending Laramide fault system splits into a complex network of faults. Also, most of the deposits appear to be localized where the faults cut Precambrian rocks rich in hornblende, biotite, or garnet and biotite. The ore controls recognized in this relatively new uranium district may have wider application in areas of similar geology elsewhere in the Front Range.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/tem901","collaboration":"This report concerns work done on behalf of the Division of Raw Materials of the U.S. Atomic Energy Commission","usgsCitation":"Sheridan, D.M., Maxwell, C.H., Albee, A., and Van Horn, R., 1956, Geology of the Ralston Buttes district, Jefferson County, Colorado: a preliminary report: U.S. Geological Survey Trace Elements Memorandum 901, Report: 25 p.; Plate 1: 23.92 inches x 32.40 inches; Plate 2: 12.85 inches x 24.65 inches; Plate 3: 13.33 inches x 18.47 inches; Plate 4: 13.22 inches x 24.70 inches, https://doi.org/10.3133/tem901.","productDescription":"Report: 25 p.; Plate 1: 23.92 inches x 32.40 inches; Plate 2: 12.85 inches x 24.65 inches; Plate 3: 13.33 inches x 18.47 inches; Plate 4: 13.22 inches x 24.70 inches","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":277477,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":8973,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tem/0901/report.pdf"},{"id":283731,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0901/plate-expl1.pdf"},{"id":283732,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0901/plate-expl2.pdf"},{"id":283733,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0901/plate-expl3.pdf"},{"id":283730,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0901/plate-2.pdf"}],"country":"United States","state":"Colorado","county":"Jefferson County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -105.3991,39.1295 ], [ -105.3991,39.9144 ], [ -105.0487,39.9144 ], [ -105.0487,39.1295 ], [ -105.3991,39.1295 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"523190e3e4b079b6e76e60d9","contributors":{"authors":[{"text":"Sheridan, Douglas M.","contributorId":13966,"corporation":false,"usgs":true,"family":"Sheridan","given":"Douglas","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":288172,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Maxwell, Charles H.","contributorId":100349,"corporation":false,"usgs":true,"family":"Maxwell","given":"Charles","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":288175,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Albee, Arden L.","contributorId":68211,"corporation":false,"usgs":true,"family":"Albee","given":"Arden L.","affiliations":[],"preferred":false,"id":288174,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Van Horn, Richard","contributorId":52169,"corporation":false,"usgs":true,"family":"Van Horn","given":"Richard","email":"","affiliations":[],"preferred":false,"id":288173,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ]}