The St. Regis-Superior area occupies about 300 square miles in northwestern Montana and includes parts of the Squaw Peak Range and Coeur d'Alerie Mountains of the northern Rocky Mountains physiographic province. Nearly 50,000 feet of metasedimentary rocks of the Precambrian Belt series, chiefly varieties of quartzite and argillite, underlies most of the area. The Belt series is informally subdivided with reference to the top of the Wallace formation into lower and upper parts. In this area, the lower part of the Belt series is divided into the Prichard, Burke and Revett, St. Regis, and Wallace formations, in order of decreasing age, and the upper part of the Belt series or the Missoula group is divided »into the Spruce, Lupine, Sloway, and Bouchard formations, and an unnamed feldspathic quartzite at Rock Rabbit Ridge, also from oldest to youngest. Formations in the lower part of the Belt series are correlated with formations of the same names in the Coeur d'Alene district, and formations in the upper part of the Belt series are tentatively correlated in part with formations of the Missoula group in the vicinity of Missoula, Mont. Paleozoic quartzite, shale, limestone, and dolomite crop out in several localities in the southeastern part of the area. The limestone unit contains fragments of a single species of Glossopleura of early Middle Cambrian age which, together with lithologic similarities, has been used to correlate at least the quartzite, shale, and limestone part of this Paleozoic sequence with the Flathead sandstone, Gordon shale, and Damnation limestone sequence known elsewhere in northwestern Montana. Several small diabasic dikes and sills are present in the area, generally associated with northwestward-trending faults.
The major faults generally trend northwestward and are considered to be part of the Lewis and Clark structural line. The Osburn fault, the major element of the Lewis and Clark line through the Coeur d'Alene district and western Mineral County, has been traced to the east edge of the St. Regis- Superior area, thus extending the mapped length of the fault to about 100 miles. Evidence indicates that this major fault has diminished in intensity in this area and that most of the stress has been relieved along the Boyd Mountain fault that apparently splits from the Osburn fault a few miles west of St. Regis. Stratigraphic and structural evidence indicates a strike-slip right-lateral movement of about 3 miles along the Osburn fault. Horizontal stratigraphic separation along the Boyd Mountain fault indicates a right-lateral movement of about 13 miles.
Low-grade regional metamorphism of the sedimentary rocks in the area has caused the recrystallization of quartz grains and the formation of sericite. Argillite and quartzite have been converted to phyllite and foliated quartzite by dynamic metamorphism in a large area north of the central part of the Osburn fault. Some of the shear zones contain a large amount of introduced carbonate minerals.
From 1901 through 1953 this area has produced 8,086,827 pounds of zinc, 7,932,958 pounds of lead, 2,053,715 pounds of copper, 584,168 fine ounces of silver, and 588 fine ounces of gold. The lead, sine, and silver have come chiefly from veins in highly foliated rocks near the Osburn fault zone. The attitudes of these veins are controlled in large part by the cleavage. The principal ore minerals are galena, sphalerite, tetrahedrite, and boulangerite, and the gangue minerals are quartz, carbonate minerals, and barite. Most of the copper has come from the Amador vein where chalcopyrite and bornite are the principal ore minerals, and the gangue minerals are pyrite, quartz, and carbonate minerals. The Amador vein occurs in a belt of copper deposits that extends westward into the Coeur d'Alene district. These copper deposits may be genetically associated with diorite dikes and sills lying within the same belt.
Fluorspar has been found in three closely spaced prospects along a northward- trending zone of brecciation and small-scale folding in Dry Creek valley. Incomplete production records show that 781 tons of fluorspar has been shipped from 2 of these prospects.
The fluorspar deposits in the Northgate district, Jackson County, Colo., are among the largest in Western United States. The mines were operated intermittently during the 1920's and again during World War II, but production during these early periods of operation was not large. Mining was begun on a larger scale in 1951, and the district has assumed a prominent position among the fluorspar producers in the United States.
Within the Northgate district, Precambrian metamorphic and igneous rocks crop out largely in the Medicine Bow Mountains, and later sedimentary rocks underlie North Park and fill old stream valleys in the mountains.
The metamorphic rocks constitute a gneiss complex that formed under progressively changing conditions of regional metamorphism. They consist principally of hornblende-plagioclase gneiss (hornblende gneiss), quartz monzonite gneiss, pegmatite, biotite-garnet-quartz-plagioclase gneiss (biotite-garnet gneiss), hornblende-biotite-quartz-plagioclase gneiss (hornblende-biotite gneiss) and mylonite gneiss.
The igneous rocks comprise some local fine-grained dacite porphyry dikes near the west margin of the district, and a quartz monzonitic stock and associated dikes in the central and eastern parts of the district.
The sedimentary rocks in the district range in age from Permian to Recent. Folded Permian and Mesozoic rocks underlie the basin of North Park, and consist in sequence from oldest to youngest, of Satanka(?) shale (0-50 feet of brick-red shale) and Forelle(?) limestone (8-15 feet of pink to light-gray laminated limestone) of Permian age, Chugwater formation of Permian and Triassic age (690 feet of red silty shale and sandstone), Sundance formation of Late Jurassic age (145 feet of sandstone containing some shale and limestone), Morrison formation of Late Jurassic age (445 feet of variegated shale and minor sandstone and limestone), Dakota group as used by Lee (1927), now considered to be of Early Cretaceous age in this area (200-320 feet of pebbly sandstone, sandstone, and shale), Ben ton shale of Early and Late Cretaceous age (665 feet of dark-gray thin-bedded shale), Niobrara formation of Late Cretaceous age (865 feet of yellow to gray limy siltstone and shale), and Pierre shale of Late Cretaceous age (more than 60 feet of dark-gray fissile shale). Unconformities separate the Chugwater and Sundance formations, and the Morrison formation and the Dakota group.
Nonmarine strata of the White River formation of Oligocene age and the North Park formation of Miocene and Pliocene (?) age fill Tertiary valleys cut in the Precambrian rocks of the mountain areas, and Quaternary terrace gravel, alluvium, and dune sand mantle much of the floor of North Park.
The main outlines of the modern Rocky Mountains formed during the Laramide orogeny in late Mesozoic and early Tertiary time. Most of the Laramide structures that can be recognized in the Northgate district involve the sedimentary rocks underlying North Park which are folded into northwest-trending anticlines and synclines. The folds are open and in most the beds dip 60° or less. Yet many anticlines are cut by reverse faults of widely different trends and directions of offset. Transverse faults offset some of the folds, and the character of folding commonly is markedly different on opposing sides of these faults. The North Park basin is cut off on the north by the east-trending Independence Mountain fault, a north-dipping reverse fault along which hard Precambrian rocks have been thrust up across the trend of the earlier Laramide structures. The North Park basin is still a major structure where it is interrupted by the Independence Mountain fault, and the original basin must have extended much farther north.
Disrupted gradients at the base of pre-White River valleys suggest that the Northgate district and adjacent areas may have been deformed in middle Tertiary time, but the evidence is not conclusive. A more definite period of deformation took place in Pliocene time following deposition of the North Park formation. North Park strata in south-central North Park were folded into a northwest-trending syncline, and the central part of the Northgate district probably was warped up along a north- or northwestward-trending axis.
Four north- to northwestward-trending faults cut the Precambrian rocks and White River formation on Pinkham Mountain and the area to the southeast. Similar faults 2½ and 15 miles west of the Northgate district cut rocks of the North Park formation, and all probably formed during the Pliocene period of deformation. The known commercial fluorspar deposits are localized along the two larger faults of the Northgate district, and they have been studied in detail.
The White River formation in early Oligocene time covered a hilly terrain drained by southward-flowing streams. By late Miocene, the northward-flowing streams had cut to about the same levels reached by the pre-White River streams and had partly exhumed and modified the older terrain. During late Miocene and early Pliocene (?) time, the Northgate area was buried beneath the clays, sands, and gravels of the North Park formation. Subsequent erosion removed the higher part of the North Park formation, cut a surface of low relief across the exhumed Precambrian rocks, and removed all topographic evidence of the Pliocene period of deformation. The present courses of the major streams were superimposed across the buried terrains during this period of erosion. Rejuvenation during middle Pleistocene caused all major streams to become incised in sharp canyons.
Copper minerals occur in small concentrations in some of the pegmatite masses in the gneiss complex. The copper-rich masses rarely exceed a few feet in diameter and constitute only a small part of the associated pegmatite body.
Vermiculite is exposed in prospect pits and mine workings along the west margin of the Northgate district. All the venniculite that was seen is associated with small masses of horablendite, massive chlorite, or serpentinite where these masses are near or are cut by pegmatite bodies. Some of the deposits may be potential producers of commercial-grade vermiculite, but most are small and erratic in shape or grade.
Fluorspar is the main mineral commodity that has been produced from the Northgate district. It was deposited during two distinct periods of mineralization, but only the younger deposits have been productive.
Small bodies of silicified breccia containing minor coarsely crystalline fluorite occur along the Independence Mountain fault, and in a few places along other Laramide faults. The fluorspar is an integral part of the fault breccia and apparently was deposited while the enclosing fault was still active.
The largest deposits of fluorspar in the Northgate district occur along the late Tertiary (?) faults on Pinkham Mountain. The fluorspar consists typically of botryoidal layers that formed as successive encrustations along open fractures, or as finely granular aggregates replacing and cementing fault gouge and White River formation. Many incompletely filled cavities, called water courses, still exist. Fluorite is the principal vein material; fragments of country rock constitute the chief impurity although finely granular quartz or chalcedony is common locally. Soft powdery manganese oxide coats many fractures and in places is associated with a fine white clay.
Fluorspar was deposited in or adjacent to open spaces along the late Tertiary (?) faults. Fractures in hard granitic rocks tended to remain open after faulting and were the favored sites for fluorspar deposition; fractures in the less competent hornblende and hornblende-biotite gneiss and schist generally were tight and little fluorspar was deposited. The White River rocks, although soft, were permeable and were widely impregnated or replaced by fluorspar.
Both of the main vein zones are along faults that have predominant rightlateral strike-slip displacement. As they theoretically should be, the vein zones are narrower and contain less fluorspar where the containing fault is deflected to the left than where the fault is deflected to the right and the fractures remained open.
The crustified, vuggy structure of the fluorspar and the common association with chalcedony or finely granular quartz suggest deposition in a very shallow environment, but no direct evidence bearing on the depth at which the fluorspar formed was seen. Fluorspar was deposited throughout a vertical range of 600 feet or more on each of the main vein zones, and for a vertical range of 1,050 feet for the district as a whole. None of the deposits had been bottomed at the time this report was prepared.
Exploration at depth beneath known ore bodies is favorable for developing large tonnages of fluorspar. The best possibilities for finding new ore bodies near the surface are along the northwestern and southeastern parts of the Fluorine-Camp Creek vein zone where large bodies of granitic rocks are intersected by the fault. These areas are generally mantled by a thick overburden, and have been inadequately tested so far.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to economic geology, 1958","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b1082F","collaboration":"Prepared in cooperation with the Colorado State Geological Survey Board and the Colorado Metal Mining Fund Board","usgsCitation":"Steven, T., 1960, Geology and fluorspar deposits, Northgate district, Colorado: U.S. Geological Survey Bulletin 1082, Report: v, 99 p.; 4 Plates: 33.80 x 32.33 inches or smaller, https://doi.org/10.3133/b1082F.","productDescription":"Report: v, 99 p.; 4 Plates: 33.80 x 32.33 inches or smaller","startPage":"323","endPage":"422","costCenters":[],"links":[{"id":100010,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082f/plate-15.pdf","text":"Plate 15","size":"1.58 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 15"},{"id":100007,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082f/plate-12.pdf","text":"Plate 12","size":"8.26 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 12"},{"id":100008,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082f/plate-13.pdf","text":"Plate 13","size":"1.27 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 13"},{"id":100009,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082f/plate-14.pdf","text":"Plate 14","size":"722 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 14"},{"id":172968,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082f/report-thumb.jpg"},{"id":109304,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20747.htm","linkFileType":{"id":5,"text":"html"},"description":"20747"},{"id":100006,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082f/report.pdf","text":"Report","size":"8.19 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Colorado","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -106.33563995361328,\n 40.86965121139933\n ],\n [\n -106.19556427001953,\n 40.86965121139933\n ],\n [\n -106.19556427001953,\n 40.99855696412671\n ],\n [\n -106.33563995361328,\n 40.99855696412671\n ],\n [\n -106.33563995361328,\n 40.86965121139933\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db6861aa","contributors":{"authors":[{"text":"Steven, Thomas A.","contributorId":57529,"corporation":false,"usgs":true,"family":"Steven","given":"Thomas A.","affiliations":[],"preferred":false,"id":235187,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220488,"text":"70220488 - 1960 - Scheelite in the precambrian gneisses of Colorado","interactions":[],"lastModifiedDate":"2021-05-17T11:59:53.430829","indexId":"70220488","displayToPublicDate":"1960-11-01T06:56:15","publicationYear":"1960","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":"Scheelite in the precambrian gneisses of Colorado","docAbstract":"Scheelite of Precambrian age has been found at several localities in Colorado and Wyoming in recent years. Most of it is disseminated in regionally metamorphosed rocks, principally in calc-silicate gneiss, but also in amphibolite. Small amounts are found in pegmatites and in gold-or copper-quartz veins of Precambrian age. The scheelite in most of the deposits contains molybdenum, and much of it is accompanied by discrete powellite (CaMoCX). The scheelite deposits vary in age with the rocks that contain them and show no consistent genetic associations. Many of the deposits are products of some phase of the major plutonic stage that included regional metamorphism, migmatization, and emplacement of syntectonic granites, A few deposits may be related to younger Precambrian granites, and some are related to late diorite and pegmatite. Tungsten originally present in minor concentration in the sedimentary rocks that gave rise to the gneisses was evidently redistributed and r eery stall ized through successive Precambrian plutonic episodes. Reworked Precambrian deposits may have been a source of the tungsten in the economically important Tertiary deposits, and possibly also of molybdenum. The Precambrian scheelite deposits found thus far have proved to be of minor economic importance, but others are still being found, and many more can be presumed to exist; among these may be some of importance.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.55.7.1406","usgsCitation":"Tweto, O., 1960, Scheelite in the precambrian gneisses of Colorado: Economic Geology, v. 55, no. 7, p. 1406-1428, https://doi.org/10.2113/gsecongeo.55.7.1406.","productDescription":"13 p.","startPage":"1406","endPage":"1428","costCenters":[],"links":[{"id":385668,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -109.072265625,\n 37.020098201368114\n ],\n [\n -102.0849609375,\n 37.020098201368114\n ],\n [\n -102.0849609375,\n 40.94671366508002\n ],\n [\n -109.072265625,\n 40.94671366508002\n ],\n [\n -109.072265625,\n 37.020098201368114\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"55","issue":"7","noUsgsAuthors":false,"publicationDate":"1960-11-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Tweto, O.L.","contributorId":102873,"corporation":false,"usgs":true,"family":"Tweto","given":"O.L.","affiliations":[],"preferred":false,"id":815736,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47377,"text":"b1082C - 1959 - Iron-ore resources of the United States including Alaska and Puerto Rico, 1955","interactions":[{"subject":{"id":13430,"text":"ofr5473 - 1954 - Iron deposits of North America, Cuba, and Puerto Rico","indexId":"ofr5473","publicationYear":"1954","noYear":false,"title":"Iron deposits of North America, Cuba, and Puerto Rico"},"predicate":"SUPERSEDED_BY","object":{"id":47377,"text":"b1082C - 1959 - Iron-ore resources of the United States including Alaska and Puerto Rico, 1955","indexId":"b1082C","publicationYear":"1959","noYear":false,"chapter":"C","title":"Iron-ore resources of the United States including Alaska and Puerto Rico, 1955"},"id":1},{"subject":{"id":47377,"text":"b1082C - 1959 - Iron-ore resources of the United States including Alaska and Puerto Rico, 1955","indexId":"b1082C","publicationYear":"1959","noYear":false,"chapter":"C","title":"Iron-ore resources of the United States including Alaska and Puerto Rico, 1955"},"predicate":"IS_PART_OF","object":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"id":2}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2024-09-24T18:21:40.983129","indexId":"b1082C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1082","chapter":"C","title":"Iron-ore resources of the United States including Alaska and Puerto Rico, 1955","docAbstract":"The importance of iron ore, the basic raw material of steel, as a fundamental mineral, resource is shown by the fact that about 100 million long tons of steel is used annually in the economy of the United States, as compared with a combined total of about 5 million long tons of copper, lead, zinc, and aluminum. Satisfying this annual demand for steel requires about 110 million tons of iron ore and 70 million tons of scrap iron and steel.
The average annual consumption of iron ore in the United States from 1951 to 1955, inclusive, was about 110 million long tons, which is about twice the annual average from 1900 to 1930. Production of iron ore in the United States in this 5-year period averaged approximately 100 million long tons annually, divided by regions as follows (in percent): Lake Superior, 84.1; southeastern, 6.7; western, 6.7; northeastern, 1.4; and central and gulf, 1.1.
Mining of iron ore began in the American Colonies about 1619, and for 225 years it was limited to eastern United States where fuel and markets were readily available. Production of iron ore from the Lake Superior region began in 1846; the region became the leading domestic source by 1890, and the Mesabi range in Minnesota has been the world's most productive area since 1896. Proximity of raw materials, water transportation, and markets has resulted in centralization of the country's iron and steel industry in the lower Great Lakes area. Increased imports of iron ore being delivered to eastern United States as well as demands for steel in nearby markets have given impetus to expansion in the steel-making capacity in this area.
The four chief iron-ore minerals - hematite, liminite, magnetite, and siderite - are widely distributed but only locally form deposits of sufficient tonnage and grade to be commercially valuable at the present time. The iron content of these minerals, of which hematite is the most important, ranges from 48 percent in siderite to 72 percent in magnetite, but as these minerals are associated with other rock-forming minerals, the iron content of marketable ore has a lower range from 30 to 67 percent.
Chemical constituents other than iron also are important in determining the marketability of iron ore. Although some iron ores can be used in the blast furnace as mined, others must first be improved either chemically by reduction of undesirable constituents, or physically by aggregation. Phosphorus and sulfur particularly are common deleterious elements; excessive silica is also undesirable but within certain limits can be controlled by additional flux. Lime and magnesia are beneficial in specified amounts because of their fluxing qualities, and a small amount of alumina improves the fluidity of slag. Manganese is especially desirable as a deoxidizing and desulfurizing agent. Titanium, chromium, and nickel must also be considered in the use of ore containing these elements.
The principal iron-ore deposits in the United States have been formed by three processes. Hematite-bearing bedded deposits such as those at Birmingham, Ala., are marine sedimentary rocks which, except for weathering along the outcrop, have remained practically unaltered since deposition. Deposits of the Lake Superior region, also in sedimentary strata, originally had a slightly lower iron content than those at-Birmingham, but ore bodies of hematite and limonite were formed by removal of other constituents in solution after deposition of the beds, with a relative increase of iron content in the material remaining. Limestone adjacent to igneous intrusions has been replaced by magnetite deposits at Cornwall, Pa., and by hematite-magnetite deposits near Cedar City, Utah. Magnetite deposits in New Jersey and in the Adirondack Mountains of New York are generally believed to have been formed by replacement of grains of other minerals in metamorphic rocks.
Iron-ore resources are made up of reserves of iron ore, material usable under existing economic and technologic conditions; and potential ore, material likely to become usable under more favorable conditions. The tonnage and grade of material of combined reserves and potential ore in each of the deposits known or believed to contain at least 200,000 long tons of iron-ore resources are tabulated in this report, and numerous sources of additional information are given in a selected bibliography.
The total domestic iron-ore resources are estimated at approximately 75,000 million long tons of crude ore. About 10,000 million tons of the resources is reserves of crude ore that will probably yield 5,500 million tons of concentrates and direct-shipping ore. About 65,000 million tons is potential ore and may yield 25,000 million tons of concentrates and some direct-shipping ore.
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Edward Huntington","contributorId":25916,"corporation":false,"usgs":true,"family":"Cobb","given":"Edward","email":"","middleInitial":"Huntington","affiliations":[],"preferred":false,"id":223004,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":36288,"text":"b1087A - 1959 - Geology of the Garo uranium-vanadium-copper deposit, Park County, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:09:48","indexId":"b1087A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1087","chapter":"A","title":"Geology of the Garo uranium-vanadium-copper deposit, Park County, Colorado","language":"ENGLISH","publisher":"U.S. Govt. Print. Office,","doi":"10.3133/b1087A","usgsCitation":"Wilmarth, V., 1959, Geology of the Garo uranium-vanadium-copper deposit, Park County, Colorado: U.S. Geological Survey Bulletin 1087, p. 1-21, ill., maps ;23 cm., https://doi.org/10.3133/b1087A.","productDescription":"p. 1-21, ill., maps ;23 cm.","costCenters":[],"links":[{"id":109313,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20759.htm","linkFileType":{"id":5,"text":"html"},"description":"20759"},{"id":97338,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1087a/report.pdf","size":"1618","linkFileType":{"id":1,"text":"pdf"}},{"id":97339,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1087a/plate-1.pdf","size":"2657","linkFileType":{"id":1,"text":"pdf"}},{"id":97340,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1087a/plate-2.pdf","size":"177","linkFileType":{"id":1,"text":"pdf"}},{"id":97341,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1087a/plate-3.pdf","size":"1321","linkFileType":{"id":1,"text":"pdf"}},{"id":97342,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1087a/plate-4.pdf","size":"740","linkFileType":{"id":1,"text":"pdf"}},{"id":97343,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1087a/plate-5.pdf","size":"269","linkFileType":{"id":1,"text":"pdf"}},{"id":165157,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1087a/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acfe4b07f02db68035d","contributors":{"authors":[{"text":"Wilmarth, Verl R.","contributorId":89951,"corporation":false,"usgs":true,"family":"Wilmarth","given":"Verl R.","affiliations":[],"preferred":false,"id":216076,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70211608,"text":"70211608 - 1959 - Geology and uranium-vanadium deposits of the slick rock district, San Miguel and Dolores counties, Colorado","interactions":[],"lastModifiedDate":"2020-08-05T14:24:39.206652","indexId":"70211608","displayToPublicDate":"1959-08-04T11:45:16","publicationYear":"1959","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Geology and uranium-vanadium deposits of the slick rock district, San Miguel and Dolores counties, Colorado","docAbstract":"Sedimentary rocks known in the Slick Rock district in southwestern Colorado range in age from Devonian (?) to Cretaceous, and aggregate about 13,000 feet in maximum thickness. Important uranium-vanadium production has come from deposits in the Salt Wash member of the Morrison formation of Late Jurassic age.
The sedimentary rocks are gently folded in the Dolores and Glade anticlines and the Disappointment syncline, and are cut by the Dolores fault zone in the north part of the district and by the Glade fault zone in the south part of the district. Principal fracture sets are oriented approximately parallel to the major faults.
Detrital hematite, magnetite, and ilmenite in rocks of the Morrison formation not affected by epigenetic alteration contain appreciable amounts of several of the elements found in the ore deposits. Epigenetic alteration processes have bleached large volumes of rock and largely destroyed these minerals. Such alteration is spatially associated with the Dolores fault zone.
Most of the known ore deposits are in the north part of the Slick Rock district in a belt called the Dolores ore zone. The zone lies along the Dolores fault zone but is wider than the fault zone. All known deposits are associated with abundant carbonaceous plant material. Uranium-vanadium deposits in the district are chiefly tabular to lenticular and are roughly parallel to the sedimentary bedding. Some ore bodies, however, are narrow, elongate, and curve sharply across bedding; these bodies have been called \"rolls\" by the miners. Mineral zoning is evident in some roll bodies; carbonates, goethite (altered from pyrite), selenides, and sulfides are commonly found in concentric layers at the concave edge of rolls. This zoning, and the relationship of roll ore bodies to sedimentary structures and lithology, suggest that ore was deposited at an interface between two solutions, possibly cool connate water and a warmer ore solution.
On a district scale, copper and lead are distinctly most abundant in the ore deposits within and immediately adjacent to the Dolores fault zone, and less abundant in deposits toward the edge of the zone. Uranium-vanadium deposits in the district occur only in sandstone that is considered to be epigenetically altered, and the most extensive epigenetic changes have occurred close to ore bodies.
It is concluded that ground water, heated and set into circulation near the end of Cretaceous time by igneous intrusions in the La Sal and other centers on the Colorado Plateau, picked up elements from sedimentary rocks where they had been faulted and fractured, and deposited the elements at solution interfaces where accumulations of carbonaceous material provided favorable chemical conditions for precipitation.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.54.3.395","usgsCitation":"Shawe, D., Archbold, N.L., and Simmons, G.C., 1959, Geology and uranium-vanadium deposits of the slick rock district, San Miguel and Dolores counties, Colorado: Economic Geology, v. 54, no. 3, p. 395-415, https://doi.org/10.2113/gsecongeo.54.3.395.","productDescription":"21 p.","startPage":"395","endPage":"415","costCenters":[],"links":[{"id":377012,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado, Utah","county":"Dolores County, San Miguel County","otherGeospatial":"Slick Rock District","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -109.610595703125,\n 37.25656608611523\n ],\n [\n -108.424072265625,\n 37.25656608611523\n ],\n [\n -108.424072265625,\n 38.14319750166766\n ],\n [\n -109.610595703125,\n 38.14319750166766\n ],\n [\n -109.610595703125,\n 37.25656608611523\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"54","issue":"3","noUsgsAuthors":false,"publicationDate":"1959-05-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Shawe, D. R.","contributorId":48819,"corporation":false,"usgs":true,"family":"Shawe","given":"D. R.","affiliations":[],"preferred":false,"id":794780,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Archbold, Norbert L.","contributorId":64714,"corporation":false,"usgs":true,"family":"Archbold","given":"Norbert","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":794781,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Simmons, G. C.","contributorId":82737,"corporation":false,"usgs":true,"family":"Simmons","given":"G.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":794782,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70211606,"text":"70211606 - 1959 - Plastic standards for geochemical prospecting","interactions":[],"lastModifiedDate":"2020-08-05T14:29:17.758343","indexId":"70211606","displayToPublicDate":"1959-08-04T11:12:02","publicationYear":"1959","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":"Plastic standards for geochemical prospecting","docAbstract":"Plastic standards for use in geochemical prospecting have been prepared by impregnating a clear thermosetting resin with different amounts of a stable dye or colored metal complex. The colored plastic is molded or subsequently milled into convenient shapes to form standards that are less bulky and more stable than the liquid standards conventionally used in rapid field methods. The use of such standards is limited only by the availability of stable coloring materials. The preparation of plastic standards for use with copper, zinc, tin, and mercury field procedures is described.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.54.4.738","usgsCitation":"Hawkins, D.B., Canney, F., and Ward, F.N., 1959, Plastic standards for geochemical prospecting: Economic Geology, v. 54, no. 4, p. 738-744, https://doi.org/10.2113/gsecongeo.54.4.738.","productDescription":"7 p.","startPage":"738","endPage":"744","costCenters":[],"links":[{"id":377010,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"54","issue":"4","noUsgsAuthors":false,"publicationDate":"1959-06-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Hawkins, D. B.","contributorId":43366,"corporation":false,"usgs":true,"family":"Hawkins","given":"D.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":794776,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Canney, F. C.","contributorId":24790,"corporation":false,"usgs":true,"family":"Canney","given":"F. C.","affiliations":[],"preferred":false,"id":794777,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ward, F. N.","contributorId":96254,"corporation":false,"usgs":true,"family":"Ward","given":"F.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":794778,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70211566,"text":"70211566 - 1959 - Amygdule mineral zoning in the Portage Lake lava series, Michigan copper district","interactions":[],"lastModifiedDate":"2020-07-31T13:33:57.228155","indexId":"70211566","displayToPublicDate":"1959-07-30T15:22:51","publicationYear":"1959","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":"Amygdule mineral zoning in the Portage Lake lava series, Michigan copper district","docAbstract":"No abstract available.
","language":"English","publisher":"GeoScienceWorld","doi":"10.2113/gsecongeo.54.8.1444","usgsCitation":"Stoiber, R., and Davidson, E., 1959, Amygdule mineral zoning in the Portage Lake lava series, Michigan copper district: Economic Geology, v. 54, no. 8, p. 1444-1460, https://doi.org/10.2113/gsecongeo.54.8.1444.","productDescription":"17 p.","startPage":"1444","endPage":"1460","costCenters":[],"links":[{"id":376925,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Michigan","otherGeospatial":"Portage Lake lava series","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -89.945068359375,\n 46.164614496897094\n ],\n [\n -84.935302734375,\n 46.164614496897094\n ],\n [\n -84.935302734375,\n 47.56911375866714\n ],\n [\n -89.945068359375,\n 47.56911375866714\n ],\n [\n -89.945068359375,\n 46.164614496897094\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"54","issue":"8","noUsgsAuthors":false,"publicationDate":"1959-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Stoiber, R.E.","contributorId":51020,"corporation":false,"usgs":true,"family":"Stoiber","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":794636,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Davidson, Edward S.","contributorId":75843,"corporation":false,"usgs":true,"family":"Davidson","given":"Edward S.","affiliations":[],"preferred":false,"id":794637,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70221608,"text":"70221608 - 1959 - Some phase relations in the hydrothermally altered rocks of porphyry copper deposits","interactions":[],"lastModifiedDate":"2021-06-25T13:17:42.933624","indexId":"70221608","displayToPublicDate":"1959-06-25T08:16:31","publicationYear":"1959","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Some phase relations in the hydrothermally altered rocks of porphyry copper deposits","docAbstract":"The application of ACF and AKF diagrams to the hydrothermal alteration in porphyry Cu deposits aids in the recognition of the critical components, and the characteristic mineral phases permit the distinction of one alteration facies from another. The somewhat meager chemical and mineralogical data suggest 3 principal alteration facies, herein called the propylitic, argillic, and potassium silicate facies. The ACF diagram applies to the propylitic alteration. The critical components are Al 2 O 3 , CaO, and (FeO + MgO + MnO), and the characteristic minerals are muscovite (sericite), epidote, chlorite, and a member of the carbonate group. The AKF diagram applies to the argillic and potassium silicate facies. The critical components are Al 2 O 3 , K 2 O, and (FeO + MgO + MnO). The characteristic minerals for the argillic facies are kaolinite (or other member of the group) and muscovite (sericite); and for the potassium silicate facies, muscovite (sericite), biotite, and K-Feldspar. For the propylitic facies, insufficient chemical analyses are available to show the chemical changes between the fresh and altered rock. For the argillic and potassium silicate facies, chemical analyses indicate a loss in Al, Fe, Mg, Ca, and Na; and a gain in K, hydroxyl ion (water), and S. The gain in K is about 60% greater for the potassium silicate facies than for the argillic.
No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr581","usgsCitation":"Albers, J.P., 1958, Geology and ore deposits of the east Shasta copper-zinc district, Shasta County, California: U.S. Geological Survey Open-File Report 58-1, Report: xxxvi, 337 p.; 6 Plates: 63.38 x 29.37 inches or smaller, https://doi.org/10.3133/ofr581.","productDescription":"Report: xxxvi, 337 p.; 6 Plates: 63.38 x 29.37 inches or smaller","costCenters":[],"links":[{"id":489313,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0001/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":489312,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0001/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":489311,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0001/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":489310,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0001/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":489309,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0001/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":489308,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0001/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":489307,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1958/0001/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":144029,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1958/0001/report-thumb.jpg"}],"country":"United States","state":"California","county":"Shasta County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -123.41344924573305,\n 41.15461559091611\n ],\n [\n -123.41344924573305,\n 39.94270771512089\n ],\n [\n -120.93861877988127,\n 39.94270771512089\n ],\n [\n -120.93861877988127,\n 41.15461559091611\n ],\n [\n -123.41344924573305,\n 41.15461559091611\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad7e4b07f02db6843ce","contributors":{"authors":[{"text":"Albers, John Patrick","contributorId":26669,"corporation":false,"usgs":true,"family":"Albers","given":"John","email":"","middleInitial":"Patrick","affiliations":[],"preferred":false,"id":166107,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39757,"text":"pp308 - 1958 - Geology and ore deposits of the Jerome area, Yavapai County, Arizona","interactions":[],"lastModifiedDate":"2016-05-19T15:12:02","indexId":"pp308","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1958","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":"308","title":"Geology and ore deposits of the Jerome area, Yavapai County, Arizona","docAbstract":"The Jerome area, in central Arizona, includes the Mingus Mountain quadrangle and parts of the adjacent Clarkdale, Mayer, and Mount Union quadrangles. The largest copper mines in the area at Jerome are the United Verde Extension and the United Verde. The United Verde Extension, closed in 1938 and the United Verde closed in 1953. The Iron King mine at Humboldt, the most active mine in the area after 1953, produces lead and zinc.
","language":"English","publisher":"United States Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp308","usgsCitation":"Anderson, C., and Creasey, S., 1958, Geology and ore deposits of the Jerome area, Yavapai County, Arizona: U.S. Geological Survey Professional Paper 308, Report: vi, 185 p.; 9 Plates: 49.18 x 63.34 inches or smaller, https://doi.org/10.3133/pp308.","productDescription":"Report: vi, 185 p.; 9 Plates: 49.18 x 63.34 inches or smaller","numberOfPages":"194","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":321137,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0308/plate-9.pdf","text":"Plate 9","linkFileType":{"id":1,"text":"pdf"}},{"id":321138,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0308/plate-10.pdf","text":"Plate 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Valleriite, gold and sphalerite are minor primary minerals; chalcocite and violarite or bravoite are supergene minerals. Pyrrhotite and pyrite are absent. From the textural relations it is inferred that a complex copper-nickel-iron sulfide was deposited early. On cooling, the sulfide unmixed into two different complex sulfides, one of which in turn unmixed into chalcopyrite and cubanite, the other into chalcopyrite and pentlandite. The latter exsolution relationship has not been previously reported. Valleriite either exsolved from, or replaced, chalcopyrite. Late solutions altered the niccolite to maucherite, and introduced gold and magnetite. The gold is almost always with maucherite.
","language":"English","publisher":"Elsevier","doi":"10.2113/gsecongeo.53.4.426","usgsCitation":"Milton, C., and Milton, D., 1958, Nickel-gold ore of the mackinaw mine, Snohomish County, Washington: Economic Geology, v. 53, no. 4, p. 426-447, https://doi.org/10.2113/gsecongeo.53.4.426.","productDescription":"22 p.","startPage":"426","endPage":"447","costCenters":[],"links":[{"id":368916,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.er.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Washington","county":"Snohomish 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C.","contributorId":37472,"corporation":false,"usgs":true,"family":"Milton","given":"C.","affiliations":[],"preferred":false,"id":774540,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Milton, D.J.","contributorId":44121,"corporation":false,"usgs":true,"family":"Milton","given":"D.J.","email":"","affiliations":[],"preferred":false,"id":774541,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010647,"text":"70010647 - 1958 - Some natural variations in the relative abundance of copper isotopes","interactions":[],"lastModifiedDate":"2020-11-12T21:03:08.201349","indexId":"70010647","displayToPublicDate":"1958-01-01T00:00:00","publicationYear":"1958","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"Some natural variations in the relative abundance of copper isotopes","docAbstract":"The relative isotopic abundance of copper has been measured in a number of minerals and a few plant materials. Suites of samples from Michigan and the Colorado Plateau have been examined in more detail to determine if local variations due to isotopic exchange or diffusion could be found. The relative isotopic abundance of copper in specimens from several other localities was also determined. The variations noted were small but in some cases were felt to be significant because they were larger than the experimental error (0·1 per cent in the ratio). A total spread of −1 to +8 parts per mil compared to the standard was found in the specimens tested.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(58)90056-5","usgsCitation":"Walker, E.C., Cuttitta, F., and Senftle, F.E., 1958, Some natural variations in the relative abundance of copper isotopes: Geochimica et Cosmochimica Acta, v. 15, no. 3, p. 183-194, https://doi.org/10.1016/0016-7037(58)90056-5.","productDescription":"12 p.","startPage":"183","endPage":"194","numberOfPages":"12","costCenters":[],"links":[{"id":480404,"rank":1,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://digital.library.unt.edu/ark:/67531/metadc1050186/","text":"External Repository"},{"id":219260,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"15","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b92c0e4b08c986b31a0c7","contributors":{"authors":[{"text":"Walker, E. C.","contributorId":71690,"corporation":false,"usgs":true,"family":"Walker","given":"E.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":359346,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cuttitta, F.","contributorId":33837,"corporation":false,"usgs":true,"family":"Cuttitta","given":"F.","affiliations":[],"preferred":false,"id":359344,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Senftle, F. E.","contributorId":47788,"corporation":false,"usgs":true,"family":"Senftle","given":"F.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":359345,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70010559,"text":"70010559 - 1958 - Spectrochemical method for the determination of selenium","interactions":[],"lastModifiedDate":"2020-08-27T20:53:12.916835","indexId":"70010559","displayToPublicDate":"1958-01-01T00:00:00","publicationYear":"1958","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":761,"text":"Analytical Chemistry","active":true,"publicationSubtype":{"id":10}},"title":"Spectrochemical method for the determination of selenium","docAbstract":"Selenium can be determined in pyrite, chalcocite, and marcasite by a simple and rapid spectrochemical method that requires no complicated arrangement of spectrographic equipment or chemical pretreatment of samples. Advantage is taken of the new short wave length radiation plates (Eastman) and the addition of copper oxide to enhance the selenium lines 2039.85 and 2062.78 A. The possibility exists of determining many other elements on the same exposure of the sample. The method is applicable in the range of 0.0015 to 2% selenium. Tests indicate an average difference from the chemical results of 0.07% in the few per cent range, 0.03% in the 0.1 to 1.0% range, 0.005% in the 0.01 to 0.1% range, and 0.00075% in the 0.001 to 0.01% range. The relative accuracy over the entire range is to about 7% of the concentration.","language":"English","publisher":"ACS Publications","doi":"10.1021/ac60141a017","usgsCitation":"Waring, C.L., Worthing, H., and Hazel, K., 1958, Spectrochemical method for the determination of selenium: Analytical Chemistry, v. 30, no. 9, p. 1504-1506, https://doi.org/10.1021/ac60141a017.","productDescription":"3 p.","startPage":"1504","endPage":"1506","numberOfPages":"3","costCenters":[],"links":[{"id":219079,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"30","issue":"9","noUsgsAuthors":false,"publicationDate":"2002-05-01","publicationStatus":"PW","scienceBaseUri":"505b954fe4b08c986b31ae7e","contributors":{"authors":[{"text":"Waring, C. L.","contributorId":96355,"corporation":false,"usgs":true,"family":"Waring","given":"C.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":359170,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Worthing, H.W.","contributorId":13104,"corporation":false,"usgs":true,"family":"Worthing","given":"H.W.","affiliations":[],"preferred":false,"id":359168,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hazel, K.V.","contributorId":65334,"corporation":false,"usgs":true,"family":"Hazel","given":"K.V.","email":"","affiliations":[],"preferred":false,"id":359169,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70010451,"text":"70010451 - 1958 - Apparatus and technique for multiple tests by the confined-spot method of colorimetric analysis: Application to field estimation of nickel and copper","interactions":[],"lastModifiedDate":"2020-11-12T21:58:14.469974","indexId":"70010451","displayToPublicDate":"1958-01-01T00:00:00","publicationYear":"1958","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":761,"text":"Analytical Chemistry","active":true,"publicationSubtype":{"id":10}},"title":"Apparatus and technique for multiple tests by the confined-spot method of colorimetric analysis: Application to field estimation of nickel and copper","docAbstract":"The confined-spot method of colorimetric analysis is generally applicable to the semiquantitative estimation of traces of ions in solution that form colored precipitates or otherwise alter material on a confined area of reagent paper. For precise results, the rate of flow of test solutions through the reagent paper must be reproduced on successive runs, so that the same proportion of reaction products is collected each time on the confined spot. A simple apparatus gives a controlled rate of flow and makes possible the analysis of many samples at one time with good reproducibility. This apparatus utilizes the increasing pull, resulting from the gradual lowering of the water level in a tank, to draw a sample solution through a confined area of reagent paper at a reproducible rate. Application to the rapid determination of nickel with dimethylglyoxime and of copper with rubeanic acid provides a method for determination of as little as 0.06 γ of nickel and 0.03 γ of copper. The coefficients of variation are 14 and 22%, respectively. This method has wide applicability in more rapid and convenient determination of trace amounts of many metals.
","language":"English","publisher":"American Chemical Society","doi":"10.1021/ac60136a026","usgsCitation":"McCarthy, J.H., and Stevens, R., 1958, Apparatus and technique for multiple tests by the confined-spot method of colorimetric analysis: Application to field estimation of nickel and copper: Analytical Chemistry, v. 30, no. 4, p. 535-538, https://doi.org/10.1021/ac60136a026.","productDescription":"4 p.","startPage":"535","endPage":"538","numberOfPages":"4","costCenters":[],"links":[{"id":218801,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"30","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059ec76e4b0c8380cd492ac","contributors":{"authors":[{"text":"McCarthy, J. H. Jr.","contributorId":89947,"corporation":false,"usgs":true,"family":"McCarthy","given":"J.","suffix":"Jr.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":358956,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stevens, R.E.","contributorId":62954,"corporation":false,"usgs":true,"family":"Stevens","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":358955,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":71693,"text":"tei696 - 1957 - Some natural variations in the relative abundance of copper isotopes","interactions":[],"lastModifiedDate":"2012-02-02T00:13:37","indexId":"tei696","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":337,"text":"Trace Elements Investigations","code":"TEI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"696","title":"Some natural variations in the relative abundance of copper isotopes","language":"ENGLISH","doi":"10.3133/tei696","usgsCitation":"Walker, E.C., Cuttitta, F., and Senftle, F.E., 1957, Some natural variations in the relative abundance of copper isotopes: U.S. Geological Survey Trace Elements Investigations 696, 29 p.: ill. ; 27 cm., https://doi.org/10.3133/tei696.","productDescription":"29 p.: ill. ; 27 cm.","costCenters":[],"links":[{"id":188371,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/tei/696/report-thumb.jpg"},{"id":90943,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tei/696/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e8e4b07f02db5e8f3a","contributors":{"authors":[{"text":"Walker, Edward C.","contributorId":48253,"corporation":false,"usgs":true,"family":"Walker","given":"Edward","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":284622,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cuttitta, Frank","contributorId":20731,"corporation":false,"usgs":true,"family":"Cuttitta","given":"Frank","email":"","affiliations":[],"preferred":false,"id":284620,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Senftle, F. E.","contributorId":47788,"corporation":false,"usgs":true,"family":"Senftle","given":"F.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":284621,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"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.
The distribution of minor elements in three basaltic flows of the Keweenawan series, of Michigan, is related to differentiation in the flows. Thus, nickel is most abundant in the early differentiates; nickel, chromium, and barium are generally deficient in the pegmatites, which formed late; whereas copper, vanadium, yttrium, and other minor elements are concentrated in the pegmatites.
The minor-element content of individual minerals in the Greenstone flow varies markedly from one mineral to another and seems to depend primarily on the presence or absence in the minerals of major elements for which the minor elements can substitute. Minor elements have substituted most readily for those major elements with similar ionic radii. Valence and electronegativity also seem to influence the ease of substitution.
The distribution of other minor elements in copper-bearing lodes of the Michigan copper district shows no apparent relation to copper mineralization.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(57)90033-9","usgsCitation":"Cornwall, H.R., and Rose, H.J., 1957, Minor elements in Keweenawan lavas, Michigan: Geochimica et Cosmochimica Acta, v. 12, no. 3, p. 209-224, https://doi.org/10.1016/0016-7037(57)90033-9.","productDescription":"16 p.","startPage":"209","endPage":"224","numberOfPages":"16","costCenters":[],"links":[{"id":218832,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Michigan","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.50537109375,\n 46.46813299215554\n ],\n [\n -84.48486328124999,\n 46.46813299215554\n ],\n [\n -84.48486328124999,\n 47.53203824675999\n ],\n [\n -90.50537109375,\n 47.53203824675999\n ],\n [\n -90.50537109375,\n 46.46813299215554\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"12","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a5b23e4b0c8380cd6f35c","contributors":{"authors":[{"text":"Cornwall, H. R.","contributorId":92333,"corporation":false,"usgs":true,"family":"Cornwall","given":"H.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":357278,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rose, H. J. Jr.","contributorId":79465,"corporation":false,"usgs":true,"family":"Rose","given":"H.","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":357277,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}