The Piedmont Upland in Maryland, Pennsylvania, and Delaware is about 160 miles long and at the most 50 miles wide. Rocks that underlie the province are the Baltimore gneiss of Precambrian age and quartzite, gneiss, schist, marble, phyllite, and greenstone, which make up the Glenarm series of early Paleozoic (?) age. These are intruded by granitic, gabbroic, and ultramaflc igneous rocks. Most of the ultramaflc rocks, originally peridotite, pyroxenite, and dunite, have been partly or completely altered to serpentine and talc; they are all designated by the general term serpentine. The bodies of serpentine are commonly elongate and conformable with the enclosing rocks. Many have been extensively quarried for building, decorative, and crushed stone. In addition, chromite, titaniferous magnetite, rutile, talc and soapstone, amphibole asbestos, magnesite, sodium- rich feldspar (commercially known as soda spar), and corundum have been mined or prospected for in the serpentine.
Both high-grade massive chromite and lower grade disseminated chromite occur in very irregular and unpredictable form in the serpentine, and placer deposits of chromite are in and near streams that drain areas underlain by serpentine. A group of unusual minerals, among them kammererite, are typical associates of high-grade massive chromite but are rare in lower grade deposits.
Chromite was first discovered in the United States at Bare Hills, Md., around 1810. Between 1820 and 1850, additional deposits were discovered and mined in Maryland and Pennsylvania, including the largest deposit of massive chromite ever found in the United States the Wood deposit, in the State Line district. A second period of extensive chromite mining came during the late 1860's and early 1870's.
Production figures are incomplete and conflicting. Estimates from the available data indicate that the aggregate production from 27 of 40 known mines before 1900 totaled between 250,000 and 280,000 tons of lode-chromite ore; information is lacking for the other 13. Placer deposits produced considerably more than 15,000 tons of chromite concentrates. Exploratory work in several of the mines and placer deposits during World War I produced about 1,500 long tons of chromite ore, 920 tons of which was sold.
Most of the chromite from Maryland and Pennsylvania was used to manufacture chemical compounds, pigments, and dyes before metallurgical and refractory uses for chromite were developed. Available analyses of the ores indicate that they would satisfy modern requirements for chemical-grade chromite. With the exception of such deposits as the Line Pit and Red Pit mines, the chromite contains too much iron for the best metallurgical grade, but many would be satisfactory low-grade metallurgical chromite. Perhaps 30,000 to 50,000 tons of chromite concentrates that would range from 30 to 54 percent Cr2O3 could be obtained from placer deposits in the State Line and Soldiers Delight districts. A small tonnage of chromite remains in dumps at six of the old mines. Lode and placer deposits in the Philadelphia district, placers in Montgomery County, Md., and possible downward extensions of known ore bodies below the floors of high-grade mines now flooded have not been completely explored. Although other chromite deposits probably lie concealed at relatively shallow depths, no practical method of finding them has been developed.
Small deposits of titaniferous iron ore in serpentine were mined for iron before 1900, but the titanium content troubled furnace operators. Ore bodies are similar in occurrence to chromite deposits; they are massive or disseminated and are found near the edges of serpentine intrusive rocks. The small size of the deposits and comparatively low titanium content limit their importance as a potential source of titanium.
A single rutile deposit in Harford County, Md., has been prospected but not mined. Pockets in schistose chlorite rock, probably altered from pyroxenite, contain as much as 16 percent rutile and average 8 percent. Rutile-bearing rock has been proved to a depth of about 58 feet.
Talc and soapstone deposits that have been worked in the State Line and Jarrettsville-Dublin districts are the result of steatitization of serpentine at its contact with intrusive sodium-rich pegmatites. Deposits in the Marriottsville and Philadelphia districts seem to be related to shear or crush zones in the serpentine, which served as channelways for steatitizing solutions. Massive soapstone was extensively used in the 19th century for furnace, fireplace, and stove linings and for washtubs and bathtubs. Every year from 1906 until 1960 talc and soapstone have been produced from one or more of the deposits in Maryland and Pennsylvania. Deposits near Dublin and Marriottsville, Md., have produced steadily for years and production continues. Lava-grade steatite from Dublin, Md., is manufactured into ceramic products for electrical and refractory purposes.
Slip-fiber amphibole asbestos deposits were known in the area as early as 1837, but early production was limited. The product was used mostly for linings of safes, boiler covers, and paints. During World War I the demand for domestic asbestos for chemical filters led to further development of deposits in Maryland. Between 1916 and 1940 many small veins of good-quality tremolite and anthophyllite were mined, and the fiber was prepared for market at Woodlawn, Md. Only the upper parts of veins, softened by weathering, were usable. Because prospecting was reportedly fairly thorough and known deposits are said to be mined out, and because demand for amphibole asbestos is limited, the possibility of future asbestos production from the area seems small, except as a byproduct of talc quarrying.
Magnesite from several mines in Pennsylvania and Maryland was much in demand between 1828 and 1871 for the manufacture of epsom salt. Exploratory work at the old Goat Hill mines in 1921 indicated that the product could not be profitably prepared for market at that time. Although reportedly high grade, the magnesite veins are thin and small in comparison with other domestic deposits.
Sodium-rich feldspar and corundum deposits occur in pegmatites that are unusual because they characteristically contain little or no quartz and mica and because, insofar as known, they are confined to serpentine rocks. Many of the known deposits of sodium-rich feldspar commercial soda-spar are reportedly mined out. It is possible, however, that other commercial deposits will be found in the area.
At various times from 1825 until about 1892 in Pennsylvania, corundum mined or found at the surface was used to meet a demand of the abrasives industry. The increased use of artificial abrasives has diminished the demand for natural corundum, and interest in the small, irregular Pennsylvania deposits is at present largely historical or mineralogical.
","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/b1082K","usgsCitation":"Pearre, N., and Heyl, A.V., 1960, Chromite and other mineral deposits in serpentine rocks of the Piedmont Upland, Maryland, Pennsylvania, and Delaware: U.S. Geological Survey Bulletin 1082, Report: vii, 126 p.; 8 Plates: 29.51 x 17.78 inches or smaller, https://doi.org/10.3133/b1082K.","productDescription":"Report: vii, 126 p.; 8 Plates: 29.51 x 17.78 inches or smaller","startPage":"707","endPage":"833","costCenters":[],"links":[{"id":172972,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082k/report-thumb.jpg"},{"id":109308,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20752.htm","linkFileType":{"id":5,"text":"html"},"description":"20752"},{"id":100033,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082k/report.pdf","text":"Report","size":"9.80 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":100034,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-40.pdf","text":"Plate 40","size":"1.66 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 40"},{"id":100035,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-41.pdf","text":"Plate 41","size":"2.03 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 41"},{"id":100036,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-42.pdf","text":"Plate 42","size":"1.29 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 42"},{"id":100037,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-43.pdf","text":"Plate 43","size":"472 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 43"},{"id":100038,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-44.pdf","text":"Plate 44","size":"325 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 44"},{"id":100039,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-45.pdf","text":"Plate 45","size":"536 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 45"},{"id":100040,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-46.pdf","text":"Plate 46","size":"389 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 46"},{"id":100041,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-47.pdf","text":"Plate 47","size":"640 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 47"}],"country":"United States","state":"Delaware, Maryland, Pennsylvania","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.45361328125,\n 39.07464374293251\n ],\n [\n -75.0640869140625,\n 39.07464374293251\n ],\n [\n -75.0640869140625,\n 40.51797520038851\n ],\n [\n -77.45361328125,\n 40.51797520038851\n ],\n [\n -77.45361328125,\n 39.07464374293251\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dde4b07f02db5e2512","contributors":{"authors":[{"text":"Pearre, Nancy C.","contributorId":88208,"corporation":false,"usgs":true,"family":"Pearre","given":"Nancy C.","affiliations":[],"preferred":false,"id":235199,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Heyl, Allen V. Jr.","contributorId":81168,"corporation":false,"usgs":true,"family":"Heyl","given":"Allen","suffix":"Jr.","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":235198,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":3609,"text":"cir415 - 1960 - Water management, agriculture, and ground-water supplies","interactions":[],"lastModifiedDate":"2012-02-02T00:05:34","indexId":"cir415","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"415","title":"Water management, agriculture, and ground-water supplies","docAbstract":"Encyclopedic data on world geography strikingly illustrate the drastic inequity in the distribution of the world's water supply. About 97 percent of the total volume of water is in the world's oceans. The area of continents and islands not under icecaps, glaciers, lakes, and inland seas is about 57.5 million square miles, of which 18 million (36 percent) is arid to semiarid. The total world supply of water is about 326.5 million cubic miles, of which about 317 million is in the oceans and about 9.4 million is in the land areas. Atmospheric moisture is equivalent to only about 3,100 cubic miles of water. \r\n\r\nThe available and accessible supply of ground water in the United States is somewhat more than 53,000 cubic miles (about 180 billion acre ft). The amount of fresh water on the land areas of the world at any one time is roughly 30,300 cubic miles and more than a fourth of this is in large fresh-water lakes on the North American Continent. \r\n\r\nAnnual recharge of ground water in the United States may average somewhat more than 1 billion acre-feet yearly, but the total volume of ground water in storage is equivalent to all the recharge in about the last 160 years. This accumulation of ground water is the nation's only reserve water resource, but already it is being withdrawn or mined on a large scale in a few areas. \r\n\r\nThe principal withdrawals of water in the United States are for agriculture and industry. Only 7.4 percent of agricultural land is irrigated, however; so natural soil moisture is the principal source of agricultural water, and on that basis agriculture is incomparably the largest water user. In view of current forecasts of population and industrial expansion, new commitments of water for agriculture should be scrutinized very closely, and thorough justification should be required. The 17 Western States no longer contain all the large irrigation developments. Nearly 10 percent of the irrigated area is in States east of the western bloc, chiefly in several Southeastern States. \r\n\r\nGround water is not completely 'self-renewing' because, where it is being mined, the reserve is being diminished and the reserve would be renewed only if pumping were stopped. \r\n\r\nWater is being mined at the rate of 5 million acre-feet per year in Arizona and 6 million in the High Plains of Texas. In contrast, water has been going into storage in the Snake River Plain of Idaho, where deep percolation from surface-water irrigation has added about 10 million acre-feet of storage since irrigation began. \r\n\r\nSituations in California illustrate problems of land subsidence resulting from pumping and use of water, and deterioration of ground-water reservoirs due to sea-water invasion. Much water development in the United States has been haphazard and rarely has there been integrated development of ground water and surface water. Competition is sharpening and new codes of water law are in the making. New laws, however, will not prevent the consequences of bad management. An important task for water management is to recognize the contingencies that may arise in the future and to prepare for them. \r\n\r\nThe three most important tasks at hand are to make more efficient use of water, to develop improved quantitative evaluations of water supplies arid their quality, and to develop management practices which are based on scientific hydrology.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/cir415","usgsCitation":"Nace, R.L., 1960, Water management, agriculture, and ground-water supplies: U.S. Geological Survey Circular 415, 12 p. :ill. ;27 cm., https://doi.org/10.3133/cir415.","productDescription":"12 p. :ill. ;27 cm.","costCenters":[],"links":[{"id":124431,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1960/0415/report-thumb.jpg"},{"id":30645,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1960/0415/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e478fe4b07f02db48a012","contributors":{"authors":[{"text":"Nace, Raymond L.","contributorId":93460,"corporation":false,"usgs":true,"family":"Nace","given":"Raymond","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":147251,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":13682,"text":"ofr5941 - 1959 - Geology of the State of Morelos and contiguous areas in south-central Mexico","interactions":[],"lastModifiedDate":"2012-02-02T00:07:01","indexId":"ofr5941","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"59-41","title":"Geology of the State of Morelos and contiguous areas in south-central Mexico","docAbstract":"The area described lies in south-central Mexico and embraces all but the southeastern corner and easternmost border of the State of Moreles, the second smallest State in the Mexican Republic. It includes small contiguous parts of the State of Mexico, in the northeastern corner, and of the State of Guerrero in the southwestern corner. Limiting geographic coordinates are 98 45\u0019 to 99 39\u001D west longitude and 18 18\u0019 to 19 08\u0019 north latitude, the northern boundary being only 35 km south of Mexico City, capital of the Republic. The geological map does not cover the entire rectangle outlined, but is irregular in form and measures roughly 4150 sq. km, three-quarters of it representing two0thirds of the State of Moreles and the rest lying outside the State.\r\n\r\nThe region ranges in altitude from 730 m above sea level at Iguala near the south edge of the map, to a general level of about 3000 m at the north edge, although individual peaks rise to 3900 m and Popocatepetl Volcano, a few kilometers east of the northeastern border of the map, rises to 5452 m above sea level. Annual rainfall ranges from a minimum of about 640 mm in the low country, to 1200 mm and more at altitudes above 2000 m. Most of it falls in summer between June and September. Winter frosts are rare below 1800 m. The climate is of savanna to steppe type; soils are thin and may be classified as belonging to the tachernoses group, with strong development of calcareous evaporates (caliche) at altitudes below 1800 m.\r\n\r\nThe northern border of the area forms the southern half of the late Pliocene to Recent Neo-volcanic Belt of basic volcanism that crosses Mexico in the direction N. 80 W., and thus has constructional topography. The rest of the area belongs to the Balsas Basin physiographic province, which is characterized by maturely dissected terrain tributary to the large Balsas River. All but the southwestern corner of the area drains southward via the Amacuzac River into the Mexcala-Balsas River, and thence westward into the Pacific Ocean. The southwestern corner drains directly into the Balsas River via the Iguala River. Local relief is of the order of 300 to 600 m. The mature topography was partly buried by late Pliocene alluvium in the central part of the area, owing largely to local volcanism. Dissolution of limestone, dolomite, and anhydrite of the Cretaceous formations has produced sinks and poljes, some of which contain small lakes. Other karst features are also common, such as caves, caverns, underground rivers, and surficial lapies or karren. Drainage blocking by lava and polje development in late Pleistocene and Recent time produced new alluvial flats in this otherwise dissected region.\r\n\r\nThe oldest rock unit in the region is the Texco schist series of late Paleozoic (?) age. It was folded, metamorphosed, foliated, intruded by dikes, and strongly eroded before the next unit, the Texco Viejo green volcanic series of Late Triassic (?) age, was deposited. Another period of metamorphism and erosion followed before the calcareous clastic sediments of the Upper Jurassic (?) Acahuizotla formation were laid down. The next unit consists of the partly phyllitic calcareous shale of the Acuitlapan formation, which is of Neocenian (?) age and rests with at least disconformity on the Acahuizotla formation. The overlying Aptian-Barresian Kochicalco formation of thin-bedded limestone appears to grade upward from the Acuitlapan formation, locally, but it seems to be unconformable elsewhere. All these units have small outcrops in the area mapped and were not studied in detail.\r\n\r\nWarping and erosion occurred before the overlying Morelos formation began to accumulate in early Albian time. The basal member is anhydrite in the eastern part of the area mapped, but limestone and dolomite were deposited elsewhere. The formation consists largely of shallow-water calcareous bank deposits, with a maximum thickness of about 900 m. Deposition ceased in early Cenomanian time and further warpi","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr5941","usgsCitation":"Fries, C.F., 1959, Geology of the State of Morelos and contiguous areas in south-central Mexico: U.S. Geological Survey Open-File Report 59-41, xi, 210 p., 22 plates :ill., maps ;27 cm., https://doi.org/10.3133/ofr5941.","productDescription":"xi, 210 p., 22 plates :ill., maps ;27 cm.","costCenters":[],"links":[{"id":147587,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1959/0041/report-thumb.jpg"},{"id":42230,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1959/0041/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42231,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1959/0041/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42232,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1959/0041/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42233,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1959/0041/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42234,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1959/0041/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e421","contributors":{"authors":[{"text":"Fries, Carl F.","contributorId":107299,"corporation":false,"usgs":true,"family":"Fries","given":"Carl","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":168226,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47376,"text":"b1082B - 1959 - Radioactive rare-earth deposit at Scrub Oaks mine, Morris County, New Jersey","interactions":[{"subject":{"id":47376,"text":"b1082B - 1959 - Radioactive rare-earth deposit at Scrub Oaks mine, Morris County, New Jersey","indexId":"b1082B","publicationYear":"1959","noYear":false,"chapter":"B","title":"Radioactive rare-earth deposit at Scrub Oaks mine, Morris County, New Jersey"},"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":1}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2017-10-18T13:41:38","indexId":"b1082B","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":"B","title":"Radioactive rare-earth deposit at Scrub Oaks mine, Morris County, New Jersey","docAbstract":"A deposit of rare-earth minerals in the Scrub Oaks iron mine, Morris County, N. J., was mapped and sampled in 1955. The rare-earth minerals are mainly in coarse-grained magnetite ore and in pegmatite adjacent to it. Discrete bodies of rare-earth-bearing magnetite ore apparently follow the plunge of the main magnetite ore body at the north end of the mine. Radioactivity of the ore containing rare earths is about 0.2 to 0.6 mllliroentgens per hour.
The principal minerals of the deposit are quartz, magnetite, hematite, albiteoligoclase, perthite and antiperthite. Xenotime and doverite aggregates and bastnaesite with intermixed leucoxene are the most abundant rare-earth minerals, and zircon, sphene, chevkinite, apatite, and monazite are of minor abundance in the ore. The rare-earth elements are partly differentiated into cerium-rich bastnaesite, chevkinite, and monazite, and yttrium-rich xenotime and doverite. Apatite, zircon, and sphene contain both cerium and yttrium group earths.
Eleven samples of radioactive ore and rock average 0.009 percent uranium, 0.062 percent thorium, 1.51 percent combined rare-earth oxides including yttrium oxide and 24.8 percent iron. Scatter diagrams of sample data show a direct correlation between equivalent uranium, uranium, thorium, and combined rare^ earth oxides. Both cerium- and yttrium-group earths are abundant in the rare-earth minerals.
Radioactive magnetite ore containing rare-earth minerals probably formed as a variant of the magnetite mineralization that produced the main iron ore of the Scrub Oaks deposit. The rare-earth minerals and the iron ore were deposited contemporaneously. Zircon crystals, probably deposited at the same time, have been determined by the Larsen method to be about 550 to 600 million years old (late Precambrian age).
Uranium, thorium, and rare-earth elements are potential byproducts of iron in the coarse-grained magnetite ore.
","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/b1082B","collaboration":"This report concerns work done on behalf of the U.S. Atomic Energy Commission and is published with the permission of the Commission","usgsCitation":"Klemic, H., Heyl, A., Taylor, A.R., and Stone, J., 1959, Radioactive rare-earth deposit at Scrub Oaks mine, Morris County, New Jersey: U.S. Geological Survey Bulletin 1082, Report: iv, 31 p.; Plate: 23.16 x 17.41 inches, https://doi.org/10.3133/b1082B.","productDescription":"Report: iv, 31 p.; Plate: 23.16 x 17.41 inches","startPage":"29","endPage":"59","costCenters":[],"links":[{"id":170648,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082b/report-thumb.jpg"},{"id":99994,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082b/report.pdf","text":"Report","size":"2.12 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":99995,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082b/plate-1.pdf","text":"Plate 1","size":"330.07 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"}],"country":"United States","state":"New Jersey","county":"Morris County","otherGeospatial":"Scrub Oaks mine","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -74.65776443481444,\n 40.84861859343548\n ],\n [\n -74.57433700561523,\n 40.84861859343548\n ],\n [\n -74.57433700561523,\n 40.911436954156436\n ],\n [\n -74.65776443481444,\n 40.911436954156436\n ],\n [\n -74.65776443481444,\n 40.84861859343548\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a81e4b07f02db649d57","contributors":{"authors":[{"text":"Klemic, Harry","contributorId":49767,"corporation":false,"usgs":true,"family":"Klemic","given":"Harry","email":"","affiliations":[],"preferred":false,"id":235179,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Heyl, A.V. Jr.","contributorId":97550,"corporation":false,"usgs":true,"family":"Heyl","given":"A.V.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":235180,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Taylor, Audrey R.","contributorId":10396,"corporation":false,"usgs":false,"family":"Taylor","given":"Audrey","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":235177,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Stone, Jerome","contributorId":19621,"corporation":false,"usgs":true,"family":"Stone","given":"Jerome","email":"","affiliations":[],"preferred":false,"id":235178,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70206770,"text":"70206770 - 1959 - Paleozoic and mesozoic fossils in a thick stratigraphic section in the eastern Sierra Nevada, California","interactions":[],"lastModifiedDate":"2019-11-21T13:15:24","indexId":"70206770","displayToPublicDate":"1959-11-21T13:15:01","publicationYear":"1959","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Paleozoic and mesozoic fossils in a thick stratigraphic section in the eastern Sierra Nevada, California","docAbstract":"A thick section of metamorphosed Paleozoic and Mesozoic rocks is exposed in two roof pend- ants, one each in the Mount Morrison and Devils Postpile quadrangles in the eastern Sierra Nevada near Mammoth Lakes, Cali- fornia (Fig. 1). In the course of geologic mapping in these quadrangles by the U. S. Geo- logical Survey in co-operation with the California Division of Mines, fossils of Ordovician, Pennsylvanian, Permian(P), and Early Jurassic ages were collected from weakly metamorphosed parts of the pendants. Detailed map- ping in the Mount Morrison quadrangle has been completed by Rinehart and Ross, and a report on this area is in preparation. Similar mapping in the Devils Postpile quadrangle by Rinehart and Huber is in progress. In the part of the Devils Postpile quadrangle not yet covered in the present study, the contacts shown on the map (Fig. 1) are after Erwin (1934). Because diagnostic fossils are extremely rare in the metamorphic rocks of the Sierra Nevada, these fossils are considered important enough to merit this short note prior to completion of the detailed mapping in the Devils Postpile quadrangle and the publication of more comprehensive reports on the two quadrangles
","language":"English","publisher":"GSA","doi":"10.1130/0016-7606(1959)70[941:PAMFIA]2.0.CO;2","usgsCitation":"Huber, N., 1959, Paleozoic and mesozoic fossils in a thick stratigraphic section in the eastern Sierra Nevada, California: GSA Bulletin, v. 70, no. 7, p. 141-146, https://doi.org/10.1130/0016-7606(1959)70[941:PAMFIA]2.0.CO;2.","productDescription":"6 p.","startPage":"141","endPage":"146","onlineOnly":"Y","costCenters":[],"links":[{"id":369391,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Mammoth Lakes Region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -119.15,\n 37.45\n ],\n [\n -118.45,\n 37.45\n ],\n [\n -118.45,\n 37.30\n ],\n [\n -119.15,\n 37.30\n ],\n [\n -119.15,\n 37.45\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"70","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Huber, N.K.","contributorId":73610,"corporation":false,"usgs":true,"family":"Huber","given":"N.K.","affiliations":[],"preferred":false,"id":775719,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010776,"text":"70010776 - 1959 - Composition of monazites from pegmatites in eastern Minas Gerais, Brazil","interactions":[],"lastModifiedDate":"2020-11-13T21:20:43.492334","indexId":"70010776","displayToPublicDate":"1959-01-01T00:00:00","publicationYear":"1959","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":"Composition of monazites from pegmatites in eastern Minas Gerais, Brazil","docAbstract":"Two zoned pegmatites in south-eastern Minas Gerais were sampled in detail for their content of monazite and xenotime and the monazite was analysed for certain of the rare-earth elements and thorium.
The ratio of xenotime to monazite increases in both pegmatites from the wall toward the quartz core. The content of the less basic rare-earth elements and of thorium in monazite rises in the same direction. These variation trends suggest that during the crystallization of these pegmatites there was a fractionation of the elements leading to a more or less steady enrichment of the less basic rare-earth elements and of thorium in the residual fluids. One mode of explaining these observed effects postulates that the rare-earth elements and thorium were present in pegmatitic fluids as co-ordination complexes rather than as simple cations.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(59)90043-2","usgsCitation":"Murata, K.J., Dutra, C.V., Costa, D., and Branco, J., 1959, Composition of monazites from pegmatites in eastern Minas Gerais, Brazil: Geochimica et Cosmochimica Acta, v. 16, no. 1-3, p. 1-14, https://doi.org/10.1016/0016-7037(59)90043-2.","productDescription":"14 p.","startPage":"1","endPage":"14","numberOfPages":"14","costCenters":[],"links":[{"id":218729,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Brazil","state":"Minas Gerais","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -46.142578125,\n -22.75592068148639\n ],\n [\n -43.06640625,\n -21.53484700204879\n ],\n [\n -40.166015625,\n -17.72775860985227\n ],\n [\n -40.078125,\n -15.792253570362446\n ],\n [\n -43.9453125,\n -14.264383087562637\n ],\n [\n -45.439453125,\n -14.859850400601037\n ],\n [\n -46.142578125,\n -22.75592068148639\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"16","issue":"1-3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f92ae4b0c8380cd4d48d","contributors":{"authors":[{"text":"Murata, K. J.","contributorId":18759,"corporation":false,"usgs":true,"family":"Murata","given":"K.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":359620,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dutra, C. V.","contributorId":37884,"corporation":false,"usgs":false,"family":"Dutra","given":"C.","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":359621,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Costa, da","contributorId":48306,"corporation":false,"usgs":true,"family":"Costa","given":"da","email":"","affiliations":[],"preferred":false,"id":359622,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Branco, J.J.R.","contributorId":84894,"corporation":false,"usgs":true,"family":"Branco","given":"J.J.R.","email":"","affiliations":[],"preferred":false,"id":359623,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70010963,"text":"70010963 - 1959 - α-Radioactivity of cerium-142","interactions":[],"lastModifiedDate":"2015-06-22T10:30:06","indexId":"70010963","displayToPublicDate":"1959-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2840,"text":"Nature","active":true,"publicationSubtype":{"id":10}},"title":"α-Radioactivity of cerium-142","docAbstract":"JOHNSON AND NIER1 have measured the atomic masses of some of the rare-earth isotopes and have shown that the mass difference cerium-142—(barium-138 + helium-4) is equivalent to 1.68 ± 0.10 MeV. Similar results for the naturally occurring samarium and neodymium isotopes show that the α-active isotope of each element is the one having the largest possible decay energy. Rasmussen and others2 suggest that the two or three neutrons just beyond the closed shell of 82 neutrons have decreased binding energies and hence the α-energy has a maximum about 84 neutrons. Johnson and Nier suggest that the α-decay of cerium-142 may take place with enough energy to be experimentally observable. Porschen and Riezler3 examined a sample of un-enriched cerium ammonium citrate using nuclear track plates sensitive to α-particles. No α-activity was observed after a 30-day exposure of 1.2 mgm. of the cerium salt. In 1957 Riezler and Kauw4 reported an alpha activity for an enriched sample of cerium-142. From their results they calculated a half-life of 5.1 × 1015 years with an uncertainty factor of 2.
","language":"English","publisher":"Nature Publishing Group","doi":"10.1038/184630a0","issn":"00280836","usgsCitation":"Senftle, F.E., Stern, T.W., and Alekna, V.P., 1959, α-Radioactivity of cerium-142: Nature, v. 184, no. 4686, https://doi.org/10.1038/184630a0.","startPage":"630","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":480398,"rank":10000,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1038/184630a0","text":"Publisher Index Page"},{"id":221080,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":205082,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1038/184630a0"}],"volume":"184","issue":"4686","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"558931dce4b0b6d21dd61c26","contributors":{"authors":[{"text":"Senftle, F. E.","contributorId":47788,"corporation":false,"usgs":true,"family":"Senftle","given":"F.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":359981,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stern, T. W.","contributorId":36122,"corporation":false,"usgs":true,"family":"Stern","given":"T.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":359980,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Alekna, V. P.","contributorId":35459,"corporation":false,"usgs":true,"family":"Alekna","given":"V.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":359979,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":33748,"text":"b1045D - 1959 - Core logs from Bristol, Cadiz, and Danby Dry Lakes, San Bernardino County, California","interactions":[],"lastModifiedDate":"2022-11-07T15:09:28.184162","indexId":"b1045D","displayToPublicDate":"1959-01-01T00:00:00","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":"1045","chapter":"D","title":"Core logs from Bristol, Cadiz, and Danby Dry Lakes, San Bernardino County, California","docAbstract":"Detailed core logs of four holes drilled in Bristol, Cadiz, and Danby Dry Lakes in southeastern San Bernardirio County, Calif., are given in the present report. These 3 dry lakes lie in a chain of basins having a drainage area of 4,000 square miles which is made up of alluvial slopes and of mountains composed of granitic, metamorphic, and volcanic rocks. Rainfall in the basins averages less than 3 inches annually.
In Bristol Dry Lake, 1 hole was drilled to a depth of 1,007 feet, and penetrated layers of dense clay alternating with salt. About 40 percent of the recovered core is halite, ranging from scattered crystals in clay to massive beds more than 8 feet thick. In Cadiz Dry Lake, 1 hole was drilled to a depth of 500 feet. The core is composed of clay, silt, and sand, with scattered gypsum crystals in small quantities, and a single salt layer, 1 foot thick, lying about 9 feet below the surface. Bedding in this core is horizontal down to a fracture at a depth of about 256 feet; from there to the bottom, the dip increases gradually to a maximum of 35°. In Danby Dry Lake, 2 holes were drilled: the first and more northerly one to a depth of 880 feet and the southerly one to a depth of 460 feet. 'Both cores are composed of clastic sediments ranging from clay to coarse sand with fine sand the most abundant. Crystalline gypsum in silt occurs between 310 and 520 feet in the northern hole and between 278 arid 334 feet in the southern hole. The northern hole was drilled in gravel for the last 20 feet. No salt beds were cut in either of the Danby holes despite the occurrence of commercial salt deposits elsewhere on the surface of the playa. Correlation of sediments between any of these cores, even between those from the same basin, is difficult and seldom convincing.
Fossils were found in the Cadiz core and in both Danby cores. The most abundant fossils are Chara, the calcified seeds of the Charophyta algae. Foraminifers, ostracodes, gastropods, pelecypods, and barnacles, in order of decreasing abundance, occur at rare intervals in these three cores.
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b1045D","usgsCitation":"Bassett, A.M., Kupfer, D., and Barstow, F., 1959, Core logs from Bristol, Cadiz, and Danby Dry Lakes, San Bernardino County, California: U.S. Geological Survey Bulletin 1045, 46 p.; 1 Plate, https://doi.org/10.3133/b1045D.","productDescription":"46 p.; 1 Plate","startPage":"97","endPage":"138","costCenters":[],"links":[{"id":61621,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1045a/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":163950,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1045d/report-thumb.jpg"},{"id":96084,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1045d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad8e4b07f02db684a3a","contributors":{"authors":[{"text":"Bassett, Allan Mordorf","contributorId":92315,"corporation":false,"usgs":true,"family":"Bassett","given":"Allan","email":"","middleInitial":"Mordorf","affiliations":[],"preferred":false,"id":211872,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kupfer, D.H.","contributorId":83935,"corporation":false,"usgs":true,"family":"Kupfer","given":"D.H.","email":"","affiliations":[],"preferred":false,"id":211871,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Barstow, F.C.","contributorId":64305,"corporation":false,"usgs":true,"family":"Barstow","given":"F.C.","email":"","affiliations":[],"preferred":false,"id":211870,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":47375,"text":"b1082A - 1958 - Zirconium and hafnium in the southeastern Atlantic States","interactions":[{"subject":{"id":47375,"text":"b1082A - 1958 - Zirconium and hafnium in the southeastern Atlantic States","indexId":"b1082A","publicationYear":"1958","noYear":false,"chapter":"A","title":"Zirconium and hafnium in the southeastern Atlantic States"},"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":1}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2017-10-18T13:01:54","indexId":"b1082A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1958","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":"A","title":"Zirconium and hafnium in the southeastern Atlantic States","docAbstract":"The principal source of zirconium and hafnium is zircon, though a minor source is baddeleyite, mined only in Brazil. Zircon is an accessory mineral in igneous, metamorphic, and sedimentary rocks, but rarely occurs in hardrock in minable quantities. The principal sources of zircon are therefore alluvial deposits, which are mined in many countries of five continents. The principal commercial deposits in the United States are in Florida, though others exist elsewhere in the southeastern Coastal Plain.
The evidence indicates that conditions for the accumulation of workable deposits of heavy minerals were more favorable during the interglacial stages of the Pleistocene epoch than during Recent time. Therefore detrital ores of large volume and high tenor are more likely to be found in the terrace deposits than along the present beaches. Other concentrations of heavy minerals, however, are possible at favored sites close to the Fall Line where the Tuscaloosa formation rests upon the crystalline rocks of the Piedmont province.
A score of heavy and semiheavy minerals occur in the detrital deposits of Florida, but the principal salable minerals are ilmenite, leucoxene, rutile, and zircon, though monazite and staurolite are saved at some mining plants. Commercial deposits of heavy minerals are generally required to have a tenor of 4 percent, though ores with a lower tenor can be mined at a profit if the content of monazite is notably high. The percentages of zircon in the concentrates ranges from 10 to 16 percent, and in eastern Florida from 13 to 15 percent. Thus the tenor in zircon of the ore-bearing sands ranges from 0.4 to 0.6 percent.
The content of hafnium in zircon is immaterial for many uses, but for some purposes very high or very low tenors in hafnium are required. Alluvial zircon cannot be separated into such varieties, which, if needed, must be obtained from sources in bedrock. It thus becomes necessary to determine the Hf : Zr ratios in zircon from many kinds of bedrock.
Granitic rocks are the principal sources of zircon, though not the best sources of zircon with a high tenor in hafnium. A general study by the Geological Survey of the granitic rocks of the Southeastern Atlantic States has been in progress for 10 years, and hundreds of samples of granitic accessory minerals have been acquired. Thirty samples of zircon from these collections were selected for spectrographic and X-ray determinations of their tenors in hafnium. Nine other samples of alluvial zircon were included, of which three are from Florida and six from foreign countries. No domestic zircon was discovered with very high or very low tenors in hafnium.
The volume of zircon in the southeastern Coastal Plain is enormous, but most of it is not recoverable. The minable reserves of heavy minerals, however, are very large, and from these it is estimated conservatively that 10 million short tons of zircon can be obtained. The corresponding amounts of zirconium and hafnium, using the mean Hf:Zr ratio of the deposits in Florida, are 4,868,000 and 112,000 tons, respectively. These reserves could be delivered, if needed, at the rate of 100,000 tons a year.
","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/b1082A","usgsCitation":"Mertie, J., 1958, Zirconium and hafnium in the southeastern Atlantic States: U.S. Geological Survey Bulletin 1082, 28 p., https://doi.org/10.3133/b1082A.","productDescription":"28 p.","numberOfPages":"28","costCenters":[],"links":[{"id":99993,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082a/report.pdf","text":"Report","size":"2.08 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":170647,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082a/report-thumb.jpg"}],"country":"United States","state":"Florida, Georgia, North Carolina, South Carolina, Tennessee, Virginia","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"MultiPolygon\",\"coordinates\":[[[[-81.582923,24.658732],[-81.451267,24.747464],[-81.298028,24.656774],[-81.765993,24.552103],[-81.582923,24.658732]]],[[[-84.777208,29.707398],[-84.696726,29.76993],[-85.036219,29.588919],[-84.777208,29.707398]]],[[[-82.255777,26.703437],[-82.038403,26.456907],[-82.186441,26.489221],[-82.255777,26.703437]]],[[[-80.250581,25.34193],[-80.611693,24.93842],[-80.192336,25.473331],[-80.250581,25.34193]]],[[[-81.444124,30.709714],[-81.256711,29.784693],[-80.567361,28.562353],[-80.566432,28.09563],[-80.031362,26.796339],[-80.152896,25.702855],[-80.229107,25.732509],[-80.409103,25.25346],[-80.652253,25.146705],[-81.079859,25.118797],[-81.362272,25.824401],[-81.678287,25.845301],[-81.868983,26.378648],[-82.094748,26.48393],[-82.076349,26.958263],[-82.147068,26.789803],[-82.301736,26.841588],[-82.714521,27.500415],[-82.393383,27.837519],[-82.716522,27.958398],[-82.566819,27.858002],[-82.721622,27.663908],[-82.851126,27.8863],[-82.674787,28.441956],[-82.702618,28.932955],[-83.679219,29.918513],[-84.245668,30.093021],[-84.335953,29.912962],[-85.343619,29.672004],[-85.405052,29.938487],[-86.222561,30.343585],[-87.518324,30.280435],[-87.395941,30.643968],[-87.626228,30.857127],[-87.548543,30.997927],[-85.057534,31.000585],[-85.141831,31.839261],[-84.925427,32.221551],[-85.188741,32.889727],[-85.598781,34.944915],[-90.309297,34.995694],[-90.09061,35.118287],[-90.166594,35.274588],[-89.992975,35.560774],[-89.923161,35.514428],[-89.915491,35.754917],[-89.68182,35.88999],[-89.699677,36.230821],[-89.534507,36.261802],[-89.5391,36.498201],[-88.045304,36.504081],[-88.068208,36.659747],[-87.872062,36.665089],[-83.690714,36.582581],[-83.156696,36.742187],[-81.968297,37.537798],[-81.896001,37.331967],[-81.560625,37.206663],[-81.367052,37.334504],[-81.225104,37.234874],[-80.332038,37.493744],[-79.649075,38.591515],[-79.291813,38.419627],[-79.023053,38.798613],[-78.869276,38.762991],[-78.439429,39.132146],[-78.346718,39.427618],[-77.828157,39.132329],[-77.687124,39.319914],[-77.46021,39.228359],[-77.47701,39.100331],[-77.038898,38.800813],[-77.291103,38.515721],[-77.286202,38.347025],[-77.024866,38.386791],[-76.910832,38.197073],[-76.265998,37.91138],[-76.339892,37.655966],[-76.722156,37.83668],[-76.252415,37.447274],[-76.475927,37.250543],[-76.300352,37.00885],[-76.780532,37.209336],[-76.482407,36.917364],[-75.972151,36.842268],[-75.533012,35.787377],[-75.960069,36.495025],[-75.791637,36.082267],[-76.132005,36.287773],[-76.191715,36.107197],[-76.447812,36.192514],[-76.298733,36.1012],[-76.575936,36.006167],[-76.721445,36.147838],[-76.675462,36.266882],[-76.744436,36.212725],[-76.608052,35.936668],[-76.014685,35.960361],[-76.046813,35.717935],[-75.86042,35.978262],[-75.713502,35.693993],[-76.165392,35.328659],[-76.499251,35.381492],[-76.586349,35.508957],[-76.476706,35.511707],[-76.634468,35.510332],[-76.580187,35.387113],[-77.023912,35.514802],[-76.472273,35.294936],[-76.801426,34.964369],[-76.958465,35.047647],[-76.762931,34.920374],[-76.463468,35.076411],[-76.332044,34.970917],[-76.524712,34.681964],[-76.673619,34.71491],[-76.523303,34.652271],[-76.093349,35.048705],[-76.524199,34.615416],[-76.990262,34.669623],[-77.556943,34.417218],[-77.956881,33.87779],[-78.383964,33.901946],[-78.772737,33.768511],[-79.359961,33.006672],[-79.55756,33.021269],[-79.968468,32.639732],[-80.413487,32.470672],[-80.466342,32.31917],[-80.905378,32.051943],[-80.841913,32.002643],[-81.065255,31.877095],[-81.254218,31.55594],[-81.17831,31.52241],[-81.276862,31.254734],[-81.490586,30.984952],[-81.408484,30.977718],[-81.444124,30.709714]]],[[[-75.753765,35.199612],[-75.523952,35.318198],[-75.533512,35.773577],[-75.52592,35.233839],[-75.982812,35.081513],[-75.753765,35.199612]]],[[[-75.242266,38.027209],[-75.962596,37.117535],[-75.981624,37.434116],[-75.712065,37.936082],[-75.242266,38.027209]]]]},\"properties\":{\"name\":\"Florida\",\"nation\":\"USA \"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d5e4b07f02db5ddd44","contributors":{"authors":[{"text":"Mertie, J.B. Jr.","contributorId":29383,"corporation":false,"usgs":false,"family":"Mertie","given":"J.B.","suffix":"Jr.","affiliations":[],"preferred":false,"id":235176,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":71987,"text":"tei230 - 1958 - Radioactive phonolite and associated thorium - rare earth - niobium veins in the Laughlin Peak area, Chico Hills, Colfax County, New Mexico","interactions":[],"lastModifiedDate":"2012-02-02T00:13:55","indexId":"tei230","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1958","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":"230","title":"Radioactive phonolite and associated thorium - rare earth - niobium veins in the Laughlin Peak area, Chico Hills, Colfax County, New Mexico","language":"ENGLISH","doi":"10.3133/tei230","usgsCitation":"Tschanz, C.M., 1958, Radioactive phonolite and associated thorium - rare earth - niobium veins in the Laughlin Peak area, Chico Hills, Colfax County, New Mexico: U.S. Geological Survey Trace Elements Investigations 230, 4 p., https://doi.org/10.3133/tei230.","productDescription":"4 p.","costCenters":[],"links":[{"id":191066,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/tei/230/report-thumb.jpg"},{"id":91079,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tei/230/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a81e4b07f02db649d7a","contributors":{"authors":[{"text":"Tschanz, Charles M.","contributorId":12937,"corporation":false,"usgs":true,"family":"Tschanz","given":"Charles","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":284963,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15556,"text":"ofr5879 - 1958 - The geology and ore deposits of Upper Mayflower Gulch, Summit County, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:07:07","indexId":"ofr5879","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1958","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":"58-79","title":"The geology and ore deposits of Upper Mayflower Gulch, Summit County, Colorado","docAbstract":"Upper Mayflower Gulch is on the highly glaciated western side of the Tenmile Range near Kokomo in central Colorado. Somewhat less than $500,000 in silver and gold has been produced from the area since the first mining in the 1880' s. \r\n\r\nIn the mapped area high grade regional metamorphism has produced two varieties of gneiss and a granulite. Total thickness of the rocks is about 5,000 feet. Relict bedding is preserved in compositional banding which strikes north to N. 20 ? E. and dips 70 ? to 80 ? southeast. No significant folding was observed. Normal faulting has occurred since the Precambrian; two major sets of faults are recognizable: (1) a set striking N. 70 ? to 85 ? E. and dipping 75?-85 ? NW; and (2) a set striking N. 70?-50 ? W. and dipping 50?-60 ? SW. Tabular bodies of pegmatite and retrogressively metamorphosed schist along many faults indicate Precambrian movement. \r\n\r\nThe Mayflower fault, a 90 to 300 foot wide zone of siltification and shattered rock, strikes about N. 40 ? W. It extends the entire length of the gulch and appears to form the northern terminus for the northeast trending Mosquito Fault. The Mayflower fault shows repeated movement since the Precambrian, totaling about 3,000 feet of apparent dip slip and 640 feet of apparent strike slip. Faulting during the Tertiary includes both additional movement along Precambrian faults and development of shears trending N. to N. 20 ? E. The shears served as channels for the intrusion of two varieties of quartz latite porphyry dikes. \r\n\r\nSpecular hematite and base-metal sulfide mineralization followed intrusion of the porphyry dikes; the minerals were deposited in open fault zones by high temperature solutions in a low pressure environment. The principal metallic minerals in order of deposition are: hematite, pyrite, chalcopyrite, sphalerite, galena, and rarer argentite. The major mines are the Gold Crest, Payrock, Nova Scotia Boy, and Bird's Nest.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr5879","usgsCitation":"Randall, J.A., 1958, The geology and ore deposits of Upper Mayflower Gulch, Summit County, Colorado: U.S. Geological Survey Open-File Report 58-79, 38 p. ill., maps (1 col.) ;27 cm., https://doi.org/10.3133/ofr5879.","productDescription":"38 p. ill., maps (1 col.) ;27 cm.","costCenters":[],"links":[{"id":148417,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1958/0079/report-thumb.jpg"},{"id":44522,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0079/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44523,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0079/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44524,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1958/0079/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44525,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1958/0079/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d96b","contributors":{"authors":[{"text":"Randall, John Alexander","contributorId":67898,"corporation":false,"usgs":true,"family":"Randall","given":"John","email":"","middleInitial":"Alexander","affiliations":[],"preferred":false,"id":171327,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":33947,"text":"b1036N - 1958 - Fractional precipitation of rare earths with phosphoric acid","interactions":[],"lastModifiedDate":"2012-02-02T00:09:19","indexId":"b1036N","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1958","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":"1036","chapter":"N","title":"Fractional precipitation of rare earths with phosphoric acid","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/b1036N","usgsCitation":"Carron, M.K., Naeser, C., Rose, H.J., and Hildebrand, F., 1958, Fractional precipitation of rare earths with phosphoric acid: U.S. Geological Survey Bulletin 1036, p. 253-275, ill. ;24 cm., https://doi.org/10.3133/b1036N.","productDescription":"p. 253-275, ill. ;24 cm.","costCenters":[],"links":[{"id":163923,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1036n/report-thumb.jpg"},{"id":61833,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1036n/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a905e","contributors":{"authors":[{"text":"Carron, M. K.","contributorId":59492,"corporation":false,"usgs":true,"family":"Carron","given":"M.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":212213,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Naeser, C.R.","contributorId":47432,"corporation":false,"usgs":true,"family":"Naeser","given":"C.R.","email":"","affiliations":[],"preferred":false,"id":212212,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rose, H. J. Jr.","contributorId":79465,"corporation":false,"usgs":true,"family":"Rose","given":"H.","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":212214,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Hildebrand, F.A.","contributorId":34569,"corporation":false,"usgs":true,"family":"Hildebrand","given":"F.A.","email":"","affiliations":[],"preferred":false,"id":212211,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70211930,"text":"70211930 - 1958 - Contact metamorphism adjacent to a teschenite intrusion","interactions":[],"lastModifiedDate":"2020-08-12T15:10:37.713101","indexId":"70211930","displayToPublicDate":"1958-08-11T15:10:30","publicationYear":"1958","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":6005,"text":"Journal of the Geological Society of Australia","onlineIssn":"0016-7614","active":false,"publicationSubtype":{"id":10}},"title":"Contact metamorphism adjacent to a teschenite intrusion","docAbstract":"Shale adjacent to the upper contact of an annular teschenite intrusion was converted to andalusite hornfels in an aureole 2–4 feet wide. At some points along the contact there is no evidence of anhydrous recrystallization. Rarely, magmatic reaction with small shale xenoliths resulted in formation of cordierite‐sillimanite (?) hornfelses, and locally a very small‐scale movement of magmatic constituents took place across the contact before consolidation of the teschenite. Very severe deuteric alteration of teschenite adjacent to the contact resulted in large losses of Si, Fe, Mg, alkalis, and probably Ca, some of which were recombined in clays and carbonates in the more porous shales and in joints, but analyses of uniformly fine‐grained shales indicate little change in bulk composition. Mineralogical evidence indicates a maximum contact temperature within the range 500°‐600° C, and a maximum intrusion temperature within the range 1000°‐1200° C.
","language":"English","publisher":"Taylor & Francis","doi":"10.1080/00167615808728492","usgsCitation":"Wilshire, H.G., 1958, Contact metamorphism adjacent to a teschenite intrusion: Journal of the Geological Society of Australia, v. 6, no. 1, p. 11-20, https://doi.org/10.1080/00167615808728492.","productDescription":"11 p.","startPage":"11","endPage":"20","costCenters":[],"links":[{"id":377387,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"6","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Wilshire, Howard G.","contributorId":68346,"corporation":false,"usgs":true,"family":"Wilshire","given":"Howard","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":795850,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010562,"text":"70010562 - 1958 - Dithizone method for determination of lead in monazite","interactions":[],"lastModifiedDate":"2020-11-12T22:06:14.46517","indexId":"70010562","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":"Dithizone method for determination of lead in monazite","docAbstract":"In the determination of lead in monazite-to be used as the basis for geologic age measurements-it was necessary to eliminate interferences due to the presence of phosphates of thorium and the rare earth metals. The method involves attacking the monazite samples with hot, concentrated sulfuric acid, then taking them up with dilute nitric acid. Lead is extracted as the dithizonate and determined spectrophotometrically at 520 mµ. Rapid determinations were made with good reproducibility on a series of monazite samples.
","language":"English","publisher":"American Chemical Society","doi":"10.1021/ac60138a043","usgsCitation":"Powell, R.A., and Kinser, C., 1958, Dithizone method for determination of lead in monazite: Analytical Chemistry, v. 30, no. 6, p. 1139-1141, https://doi.org/10.1021/ac60138a043.","productDescription":"3 p.","startPage":"1139","endPage":"1141","numberOfPages":"3","costCenters":[],"links":[{"id":480405,"rank":1,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://digital.library.unt.edu/ark:/67531/metadc1050379/","text":"External Repository"},{"id":219082,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"30","issue":"6","noUsgsAuthors":false,"publicationDate":"2002-05-01","publicationStatus":"PW","scienceBaseUri":"505a0330e4b0c8380cd503a7","contributors":{"authors":[{"text":"Powell, R. A.","contributorId":41789,"corporation":false,"usgs":true,"family":"Powell","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":359174,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kinser, C. A.","contributorId":104984,"corporation":false,"usgs":true,"family":"Kinser","given":"C. A.","affiliations":[],"preferred":false,"id":359175,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010754,"text":"70010754 - 1958 - Biogeochemistry of the rare-earth elements with particular reference to hickory trees","interactions":[],"lastModifiedDate":"2020-11-12T21:11:22.260526","indexId":"70010754","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":"Biogeochemistry of the rare-earth elements with particular reference to hickory trees","docAbstract":"Hickory trees concentrate the rare-earth elements in their leaves to a phenomenal degree and may contain as much as 2300 p.p.m. of total rare earths based on the dry weight of the leaves. The average proportions of the individual elements (atomic percent of the total rare-earth elements) in the leaves are: Y 36, La 16, Ce 14, Pr 2, Nd 20, Sm 1, Eu 0.7, Gd 3, Tb 0.6, Dy 3, Ho 0.7, Er 2, Tm 0.2, Yb 1, and Lu 0.2. The similarity in the proportions of the rare-earth elements in the leaves and in the exchange complex of the soil on which the hickory trees grow indicates that the trees do not fractionate the rare earths appreciably.
The variation of the rare-earth elements in the leaves and soils can be explained generally in terms of the relative abundance of the cerium group and the yttrium group, except for the element cerium. The large fluctuations in the proportion of cerium [Ce/(La + Nd) atomic ratios of 0.16 to 0.86] correlate with oxidation-reduction conditions in the soil profile. The substitution of dilute H2SO3 for dilute HC1 in the determination of available rare-earth elements brings about a large increase in the proportion of cerium that is extracted from an oxygenated subsoil. These relationships strongly suggest that quadrivalent cerium is present in oxygenated subsoil and is less available to plants than the other rare-earth elements that do not undergo such a change in valence.
A few parts per billion of rare-earth elements have been detected in two samples of ground water.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(58)90093-0","usgsCitation":"Robinson, W.O., Bastron, H., and Murata, K.J., 1958, Biogeochemistry of the rare-earth elements with particular reference to hickory trees: Geochimica et Cosmochimica Acta, v. 14, no. 1-2, p. 55-67, https://doi.org/10.1016/0016-7037(58)90093-0.","productDescription":"13 p.","startPage":"55","endPage":"67","numberOfPages":"13","costCenters":[],"links":[{"id":219705,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"14","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f159e4b0c8380cd4abeb","contributors":{"authors":[{"text":"Robinson, W. O.","contributorId":56924,"corporation":false,"usgs":true,"family":"Robinson","given":"W.","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":359574,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bastron, H.","contributorId":20067,"corporation":false,"usgs":true,"family":"Bastron","given":"H.","affiliations":[],"preferred":false,"id":359573,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Murata, K. J.","contributorId":18759,"corporation":false,"usgs":true,"family":"Murata","given":"K.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":359572,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70160531,"text":"70160531 - 1957 - Teratological hermaphroditism in the chum salmon Oncorhynchus keta (Walbaum)","interactions":[],"lastModifiedDate":"2021-04-06T15:56:20.797572","indexId":"70160531","displayToPublicDate":"2015-12-22T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3196,"text":"Progressive Fish-Culturist","active":true,"publicationSubtype":{"id":10}},"displayTitle":"Teratological hermaphroditism in the chum salmon Oncorhynchus keta (Walbaum)","title":"Teratological hermaphroditism in the chum salmon Oncorhynchus keta (Walbaum)","docAbstract":"The anomalous condition of hermaphroditism appears to be no less rare in fish than in other normally dioecious animals. Previous records of bisexuality' in the Pacific salmons, Oncorhynchus spp., are few in number despite the intensive study accorded this group. Rutter (1902) reported the condition in two king salmon (O. tshawytscha); Crawford (1927) reported the condition in a silver salmon (O. kisutch); and Gibbs (1956) described a bisexual steelhead trout (Salmo gairdneri) and briefly noted another instance of hermaphroditism in the king salmon. We wish to record an example of this anomaly in the chum salmon (O. keta).
","language":"English","publisher":"Taylor & Francis","publisherLocation":"Washington D.C.","doi":"10.1577/1548-8659(1958)20[191:THITCS]2.0.CO;2","usgsCitation":"Uzmann, J., and Hesselholt, M.N., 1957, Teratological hermaphroditism in the chum salmon Oncorhynchus keta (Walbaum): Progressive Fish-Culturist, v. 20, no. 4, p. 191-192, https://doi.org/10.1577/1548-8659(1958)20[191:THITCS]2.0.CO;2.","productDescription":"2 p.","startPage":"191","endPage":"192","numberOfPages":"2","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":654,"text":"Western Fisheries Research Center","active":true,"usgs":true}],"links":[{"id":312718,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"20","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"567a742de4b0a04ef490fcbd","contributors":{"authors":[{"text":"Uzmann, J. R.","contributorId":38647,"corporation":false,"usgs":true,"family":"Uzmann","given":"J. R.","affiliations":[],"preferred":false,"id":583061,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hesselholt, M. N.","contributorId":150793,"corporation":false,"usgs":false,"family":"Hesselholt","given":"M.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":583062,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":14976,"text":"ofr5772 - 1957 - Geology of possible petroleum provinces in Alaska","interactions":[{"subject":{"id":14976,"text":"ofr5772 - 1957 - Geology of possible petroleum provinces in Alaska","indexId":"ofr5772","publicationYear":"1957","noYear":false,"title":"Geology of possible petroleum provinces in Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":35230,"text":"b1094 - 1959 - Geology of possible petroleum provinces in Alaska","indexId":"b1094","publicationYear":"1959","noYear":false,"title":"Geology of possible petroleum provinces in Alaska"},"id":1}],"supersededBy":{"id":35230,"text":"b1094 - 1959 - Geology of possible petroleum provinces in Alaska","indexId":"b1094","publicationYear":"1959","noYear":false,"title":"Geology of possible petroleum provinces in Alaska"},"lastModifiedDate":"2024-05-03T22:50:46.949424","indexId":"ofr5772","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"57-72","title":"Geology of possible petroleum provinces in Alaska","docAbstract":"The history of petroleum exploration in Alaska and the geology of possible petroleum provinces in Alaska are reviewed. Maps showing Alaska's major Mesozoic and Tertiary tectonic elements, possible petroleum provinces, and indications of petrol, are included in this report. Annotated references in Geological Survey publications relating to petroleum and oil shale in Alaska are given at the end of the report.
For the purpose of appraising its petroleum possibilities, Alaska is divided into the southern, central, and northern major geologic-physiographic regions.
Southern Alaska includes the arcuate mountain chain formed by the Alaska and Aleutian Ranges and the Mentasta- Nutzotin Mountains, the coastal range and valley area to the south, and the southeastern Alaska \"panhandle\" -- an area of 185,000 square miles.
Oil seeps on the west shore of Cook Inlet in southern Alaska were known as early as 1853, and claims were staked in this region in 1882. Drilling began near the oil seeps in the Katalla district about 1901, and this started Alaska's first period of oil activity. From 1902 to 1933 the Katalla field produced 154,000 barrels of oil from fractured shale and sandstone of Tertiary age the- first and only commercial production in Alaska.
On the basis of geology, surficial indications of petroleum, and test wells drilled, six possible petroleum provinces are indicated in southern Alaska. They are Heceta Island area, Keku Islands area, Cook Inlet Mesozoic province, Gulf of Alaska Tertiary province, Cook Inlet Tertiary province, and Copper River basin.
The exposed rocks in the Heceta Island area include lower Paleozoic graywacke-type sandstone, sandstone, conglomerate, and massive limestones with reeflike structures; igneous rocks are rare or lacking in much of the area. The Kosciusko-Tuxekan-Heceta synclinorium, the main structural feature, is modified by minor folds and faults. Some of the minor folds are reported to be broad and open, with flanks dipping 20°-145°. As far as known, the Heceta Island area has not heretofore been seriously considered as a possible petroleum province.
Rocks of Silurian to Cretaceous age are exposed in the Keku Island area and include moderately folded and relatively unaltered limestone and other marine sedimentary rocks.
The Cook Inlet Mesozoic province, a land area of approximately 18,500 square miles, includes a great thickness of unmetamorphosed marine sedimentary rocks of Jurassic and Cretaceous age. At least 23 test wells were drilled or started in this province by the end of 1955. Shows of oil and gas were encountered in many of these wells. During 1955 at least ten oil companies were active in this area and by the end of 1955 about 1 1/2 million acres were included in oil and gas leases applied for or granted.
The Gulf of Alaska Tertiary province includes about 5,200 square miles in which rocks of Tertiary age are exposed or are believed to underlie Quaternary deposits. Between 1901 and the end of 1955 about 47 wells were drilled or started in this province.
The Cook Inlet Tertiary province embraces an area of about 9,500 square miles, of which about 4,100 is covered by the shallow waters of Cook Inlet. Petroleum exploration has been in that part of the area which overlaps the Cook Inlet Mesozoic province. Eocene or younger Tertiary nonmarine sedimentary rocks are believed to underlie much of the province, and marine rocks of Tertiary age may also be present.
The Copper River basin is a topographic basin underlain by unconsolidated deposits of Quaternary age. Tertiary rocks favorable for the accumulation of petroleum may underlie part of the basin but this is not believed likely. Except for some leasing activity no petroleum exploration has been recorded in the Copper River Basin to the end of 1955.
Central Alaska is a region of about 275,000 square miles and consists of an irregular assemblage of intricately dissected uplands and alluvium-floored lowland basins. Scattered peaks of resistant intrusive igneous rocks surmount most of the upland areas.
In the vast region of central Alaska only six test wells are known to have been drilled for the purpose of finding oil and gas. The maximum depth reached was 350 feet and the holes were mostly or entirely in Quaternary deposits. In recent years several oil companies have investigated some parts of the region and large areas in the Yukon-Koyukuk province are now under lease. Oil seeps, gas seeps, and other indications of petroleum have been reported from many localities; samples from two localities have been analyzed and reported to be petroleum.
The geology of central Alaska is similar in a general way to that of the area between the Rocky Mountains and Sierra-Cascade belts of the United States. Sedimentary rocks, probably equivalent to the Precambrian Belt series, and rocks of the Cambrian and all younger geologic systems have been recognized in central Alaska. The structure of the region is known to be complex, but except in local mineral districts, it has not been mapped in detail. Based on the limited amount of available information, the region cannot be regarded as distinctly favorable for significant accumulations of petroleum. However, three pre-Cenozoic provinces, the Yukon-Koyukuk, the Kobuk, and the Kandik, and several large Cenozoic basin provinces may be worthy of further investigation.
Northern Alaska includes the Brooks Range and all the treeless tundra north to the Arctic Coast, an area of about 125,000 square miles. The presence of oil seeps along the Arctic Coast has been known at least since 1900 and a description of the Cape Simpson oil seeps vas published in 1909. Since then oil and gas seeps have been described from nine localities, and oil shales and oil-bearing sandstones are known from many localities in the Arctic Foothills province. Oil and gas deposits have been discovered and geologic conditions are favorable for oil and gas accumulations in approximately half of the region.
In 1923 approximately 37,000 square miles in northern Alaska was reserved by Executive order as Naval Petroleum Reserve No. 4. In 1944 the U. S. Navy began a vast petroleum exploration program which was suspended in 1953. In the years 1945 through 1955, 37 test wells and 45 core tests were drilled on 18 structures. Three oil fields, Umiat, Simpson, and Fish Creek, and two gas fields, South Barrow and Gubik, were discovered. Total reserve estimates for all discoveries of oil to 1955 range from 30 to 100 million barrels, and for gas, from 370 billion to 900 billion cubic feet.
All northern Alaska, with the exception of the Brooks Range, can be considered a possible petroleum province, but the region can be subdivided into provinces of somewhat different potentialities. These subdivisions roughly correspond with the geomorphic provinces and sections, which in turn reflect differences in geology. The known oil-bearing beds are of Mesozoic age, primarily Cretaceous, and thus the possible petroleum provinces could be designated as Mesozoic. However, Paleozoic and Cenozoic rocks with favorable reservoir characteristics are exposed in the region and possibly underlie, in favorable structural situations, some of the areas as yet not tested.
The Arctic Coastal Plain province includes gently folded and flat-lying Mesozoic beds that overlie a basement complex of Paleozoic and early Mesozoic age. Near the southern edge of this province the basement rocks are at depths of at least 20,000 feet, and to the north these rocks rise to within 2,500 feet of the surface.
The Teshukpuk Lake section of the Arctic Coastal plain includes many of the known oil seeps; it is the most accessible to sea transportation, and lies almost completely within NPR 4. Thirteen test wells and 35 core tests have been drilled here; one gas field and two (at present, noncommercial) oil fields have been discovered. The possibility of further discoveries may depend largely on locating porous sandstones in stratigraphic rather than anticlinal traps.
The White Hills section is distinguished topographically from the Teshukpruk section by its white-gravel-covered hills and fever lakes, and geologically by the presence of Tertiary rocks, including 2,000 feet of nonmarine beds in the west and at least 7,000 feet of marine beds to the east, in the vicinity of Carter Creek. This section appears to be more complex structurally. No test wells have been drilled in the White Hills section.
The Northern Foothills section includes many closed anticlines. Twenty-four test wells and ten core tests have been drilled on 11 structures and two discoveries have been made -the Umiat oil field and the Gubik gas field. All these tests have been drilled in Cretaceous rocks.
The Southern Foothills section is structurally similar to the Alberta Foothills and to the northern part of the Brooks Range. Great thicknesses of marine shale of Lover Cretaceous, Jurassic, and Triassic age are exposed. The outcropping Mesozoic sandstones are generally poorly sorted, nonporous, and impermeable. To the south the section is bordered by mountainous exposures of Mississippian limestone, which probably underlie at least part of this section.
The rocks that underlie the deeply eroded complex structures of the Brooks Range include schist, slate, argillite, and limestone. Some exposed limestones have a strong petroleum-like odor and contain traces of petroleum residues.
Analysed samples of uraninite were x-rayed, annealed by heating to 550° and 900° for various times in a nitrogen atmosphere, and x-rayed again. A decrease in unit cell size was generally observed. Calculations on the basis of Vegard's Law showed that the ordering of the interstitial oxygen ions could account for the decrease in cell size on annealing. The interstitial oxygens are not necessarily completely disordered before annealing. The degree of original disorder is dependent on the Rare Earth/ThO2 ratio; for high ThO2 and low rare earths, the interstitial oxygens are completely random. The degree of disorder apparently depends solely on the composition, and not on the past history of the sample; this implies that the oxygens are being continuously disordered, perhaps by alpha particles, to the equilibrium point determined by the R.E./ThO2 ratio. The degree of ordering of the interstitial oxygens also accounts for the difference in cell size between vein pitchblendes and those from the sediments of the Colorado Plateau.
\nA study was also made of the degree of oxidation of uraninites. Although the uranium in many pegmatitic uraninites is more oxidized than can be obtained with the cubic UO2 phase in the laboratory, if the atoms proxying for uranium are calculated into the structural formula, and the lead is assumed to be radiogenic and calculated as original uranium, almost all pegmatitic uraninites fall into the range of interstitial oxygen content obtainable in the laboratory. This fact supports the auto-oxidation hypothesis.
\nMany of the vein and sedimentary pitchblendes have compositions close to U3O8, although they are cubic. They may gave crystallized as U3O8, the decomposed to the cubic phase and a amorphous phase. This suggests that the stability range of U3O8 includes only very exceptional natural conditions.
\nVegard's Law calculations, studies of zoning in crystals, differential leaching, polished section textures, and other lines of evidence indicate that lead, including radiogenic lead, is exsolved from uraninite. A study of x-ray line intensities indicates that it exsolves as oriented monomolecular layers of orthohombic PbO (massicot) along cube planes in the uraninite, separating the uraninite crystallites so that the x-ray reflections interfere destructively to different degrees for different reflections.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5711","collaboration":"This report concerns work done on behalf of the Division of Raw Materials of the U.S. Atomic Energy Commission","usgsCitation":"Berman, R.M., 1957, The role of lead and excess oxygen in uranite: U.S. Geological Survey Open-File Report 57-11, 100 p., https://doi.org/10.3133/ofr5711.","productDescription":"100 p.","numberOfPages":"146","costCenters":[],"links":[{"id":287354,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287353,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1957/0011/report.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6fe4b07f02db640e42","contributors":{"authors":[{"text":"Berman, Robert Morris","contributorId":36145,"corporation":false,"usgs":true,"family":"Berman","given":"Robert","email":"","middleInitial":"Morris","affiliations":[],"preferred":false,"id":166531,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":33870,"text":"b1019F - 1957 - Selected annotated bibliography of thorium and rare-earth deposits in the United States including Alaska","interactions":[],"lastModifiedDate":"2012-02-02T00:09:37","indexId":"b1019F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1957","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":"1019","chapter":"F","title":"Selected annotated bibliography of thorium and rare-earth deposits in the United States including Alaska","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/b1019F","usgsCitation":"Buck, K.L., 1957, Selected annotated bibliography of thorium and rare-earth deposits in the United States including Alaska: U.S. Geological Survey Bulletin 1019, p. 517-541 ;23 cm., https://doi.org/10.3133/b1019F.","productDescription":"p. 517-541 ;23 cm.","costCenters":[],"links":[{"id":109145,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20554.htm","linkFileType":{"id":5,"text":"html"},"description":"20554"},{"id":247444,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1019f/report.pdf","size":"1322","linkFileType":{"id":1,"text":"pdf"}},{"id":247445,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1019f/plate-3.pdf","size":"896","linkFileType":{"id":1,"text":"pdf"}},{"id":251850,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1019f/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a09e4b07f02db5fa714","contributors":{"authors":[{"text":"Buck, Katharine L.","contributorId":55059,"corporation":false,"usgs":true,"family":"Buck","given":"Katharine","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":212083,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":56097,"text":"ofr57109 - 1957 - Continued utilization of ground-water storage basins","interactions":[],"lastModifiedDate":"2014-05-21T09:42:46","indexId":"ofr57109","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":"57-109","title":"Continued utilization of ground-water storage basins","docAbstract":"Doubtless most of you are more familiar with surface reservoirs, their capabilities and limitations, than you are with ground-water reservoirs. I believe that this is true of people in general, even the experts. And because of our inadequate knowledge of ground-water reservoirs, our use of them creates problems that are rarely if ever encountered in the operation of surface reservoirs. Nevertheless there are many similarities between these two basic forms of water storage, and I should like to point out some of these similarities, was well as some important contrasts.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr57109","usgsCitation":"Thomas, H.E., 1957, Continued utilization of ground-water storage basins: U.S. Geological Survey Open-File Report 57-109, 16 p., https://doi.org/10.3133/ofr57109.","productDescription":"16 p.","numberOfPages":"16","costCenters":[],"links":[{"id":287413,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287412,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1957/0109/report.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afde4b07f02db696c0e","contributors":{"authors":[{"text":"Thomas, H. E.","contributorId":12829,"corporation":false,"usgs":true,"family":"Thomas","given":"H.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":254759,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":71657,"text":"tei639 - 1957 - Radioactive rare-earth deposit at the Scrub Oaks Mine, Morris County, New Jersey","interactions":[],"lastModifiedDate":"2012-02-02T00:13:48","indexId":"tei639","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":"639","title":"Radioactive rare-earth deposit at the Scrub Oaks Mine, Morris County, New Jersey","language":"ENGLISH","doi":"10.3133/tei639","usgsCitation":"Klemic, H., Heyl, A.V., Taylor, A.R., and Stone, J., 1957, Radioactive rare-earth deposit at the Scrub Oaks Mine, Morris County, New Jersey: U.S. Geological Survey Trace Elements Investigations 639, 57 p., 6 fig., https://doi.org/10.3133/tei639.","productDescription":"57 p., 6 fig.","costCenters":[],"links":[{"id":185852,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/tei/639/report-thumb.jpg"},{"id":90904,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tei/639/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":90905,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tei/639/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649d4f","contributors":{"authors":[{"text":"Klemic, Harry","contributorId":49767,"corporation":false,"usgs":true,"family":"Klemic","given":"Harry","email":"","affiliations":[],"preferred":false,"id":284555,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Heyl, A. V.","contributorId":70032,"corporation":false,"usgs":true,"family":"Heyl","given":"A.","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":284556,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Taylor, Audrey R.","contributorId":10396,"corporation":false,"usgs":false,"family":"Taylor","given":"Audrey","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":284553,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Stone, Jerome","contributorId":19621,"corporation":false,"usgs":true,"family":"Stone","given":"Jerome","email":"","affiliations":[],"preferred":false,"id":284554,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70219992,"text":"70219992 - 1957 - Physical and ecologic features of the Sagadahoc Bay Tidal Flat, Georgetown, Maine","interactions":[],"lastModifiedDate":"2021-04-16T17:03:54.075817","indexId":"70219992","displayToPublicDate":"1957-03-01T11:53:52","publicationYear":"1957","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1726,"text":"GSA Memoirs","active":true,"publicationSubtype":{"id":10}},"title":"Physical and ecologic features of the Sagadahoc Bay Tidal Flat, Georgetown, Maine","docAbstract":"Sagadahoc Bay is open to the ocean at the south and has no significant fresh-water stream entering it. The intertidal zone is roughly a mile long by half a mile wide; most of it is made up of medium to fine sand, but organic-rich mud characterizes the head of the flat and the protected coves. Refraction-seismograph surveys showed that the bedrock surface lies 30 to 200 feet below the surface of the tidal flat and that it is irregular and fluted longitudinally. Repeated surveys indicate that the intertidal flat builds up and cuts down but is apparently in equilibrium with the present sea level. The sediment that fills the bay came from the sea. Waves and tidal currents tend to move it landward; storms accelerate this, or reverse the direction of movement, depending on the characteristics of the storm.
Tidal- and wave-generated currents 0.1 foot above the bottom range in velocity from 0.35 to 0.82 foot per second on incoming tides and from 0.20 to 0.58 foot per second on ebbing tides. Incoming tides float large quantities of sand landward; ebbing tides never carry floating sand.
Two distinctive and extensive Mya shell-pavement layers were found at depths of roughly 2 and 3 feet below the present surface of the tidal flat. The lower layer is approximately 1,000 years old according to a radiocarbon age determination of its Mya shells. It is suggested that these shell layers formed by sluicing away of a layer of sand about 2 feet thick, which had been thrown into loose packing by an earthquake at high tide. The earth shock induced a submarine slide of the sand in the outer part of the bay, which oversteepened the profile of the sand headward nearly to the head of the bay. Mya and other shells settled through the layer of quicksand while the sand was running out seaward.
Living in the intertidal zone is the usual assemblage of clams, gastropods, crustaceans, worms, and seaweeds found on most northern New England tidal flats. The Mya arenaria population is decreasing, but in general myas are more numerous in the muddy areas than in the sandy areas. They grow more rapidly in the sand, though in the past decade there has been no significant renewal of the Mya population in the sandy part of the flat. Macoma balthica inhabits the muddy areas, whereas Ensis, Spisula, and Arctica are restricted to the low-tide zone and the shallow water below. Gemma gemma grows in great abundance in the sandy part of the flat but is rare in the muddy parts. Small shrimp and green crabs are common.
The calcareous shells of these animals are all potential fossils, but the shrimp and crab exoskeletons are not, for their tests are rapidly decomposed in this environment. Other potential fossils are wood and bark, acorn caps, conifer cones, leaves of deciduous trees, seeds, and occasionally even grass stems and pieces of eel grass. All these are reasonably well preserved in the constant reducing environment that prevails an inch or two below the surface.
An inverse relationship exists between the abundances of Mya arenaria and Gemma gemma. Cores and test pits show that gemmas are more numerous on the Sagadahoc flat now than they have been in the recent past (estimated 10–100 years). Gemmas are the dominant mollusk in the sandy part of the flat now that the myas are so extremely rare. The speculation is that gemmas became dominant largely because the Mya population was greatly reduced by intensive digging during and just after the last war and through depredations by green crabs. Possibly the warming climate has favored the gemmas selectively.
The writer infers that the gemmas are a serious competitor of the myas and that the gemmas now starve out Mya spat, which is known to be carried into the bay each spring and fall. Two recommendations are made: (1) determining under controlled laboratory conditions the food requirements of Gemma and the density of Gemma population that will permit survival of Mya larvae from set through a stage that will assure maturation; and (2) killing off a large percentage of the Gemma population and observing whether or not a natural set of Mya occurs. Gemmas can be killed quickly under a flame shield such as is used to soften asphalt-sand mixtures in street paving. Inasmuch as gemmas are ovoviviparous they should not repopulate the flat rapidly.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/MEM67V2-p641","usgsCitation":"Bradley, W., 1957, Physical and ecologic features of the Sagadahoc Bay Tidal Flat, Georgetown, Maine: GSA Memoirs, v. 67, no. 2, https://doi.org/10.1130/MEM67V2-p641.","costCenters":[],"links":[{"id":385165,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Maine","otherGeospatial":"Sagadahoc Bay Tidal Flat","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -69.80712890625,\n 43.72744458647464\n ],\n [\n -69.36767578124999,\n 43.72744458647464\n ],\n [\n -69.36767578124999,\n 43.929549935614595\n ],\n [\n -69.80712890625,\n 43.929549935614595\n ],\n [\n -69.80712890625,\n 43.72744458647464\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"67","issue":"2","noUsgsAuthors":false,"publicationDate":"1957-03-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Bradley, W.H.","contributorId":220222,"corporation":false,"usgs":false,"family":"Bradley","given":"W.H.","email":"","affiliations":[],"preferred":false,"id":814415,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010798,"text":"70010798 - 1957 - Systematic variation of rare-earth elements in cerium-earth minerals","interactions":[],"lastModifiedDate":"2024-03-06T17:58:43.969092","indexId":"70010798","displayToPublicDate":"1957-01-01T00:00:00","publicationYear":"1957","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":"Systematic variation of rare-earth elements in cerium-earth minerals","docAbstract":"In a continuation of a study reported previously, rare-earth elements and thorium have been determined in monazite, allanite, cerite, bastnaesite, and a number of miscellaneous cerium-earth minerals. A quantity called sigma (∑), which is the sum of the atomic percentages of La, Ce, and Pr, is proposed as an index of composition of all cerium-earth minerals with respect to the rare-earth elements. The value of ∑ for all of the minerals analysed falls between 58 and 92 atomic per cent. Monazites, allanites, and cerites cover the entire observed range, whereas bastnaesites are sharply restricted to the range between 80 and 92 atomic per cent.
The minimum value of ∑ for a cerium-earth mineral corresponds to the smallest possible unit-cell size of the mineral. In monazite, this structurally controlled minimum value of ∑ is estimated to be around 30 atomic per cent. Neodymium, because of its abundance, and yttrium, because of its small size, have dominant roles in contraction of the structure. In the other direction, the limit of variation in composition will be reached when lanthanum becomes the sole rare-earth element in a cerium-earth mineral.
Cerium-earth minerals from alkalic rocks are all characterized by values of ∑ greater than 80 atomic per cent, indicating that the processes that formed these rocks were unusually efficient in fractionating the rare-earth elements—efficient in the sense that a highly selected assemblage is produced without eliminating the bulk of these elements.
Analyses of inner and outer parts of two large crystals of monazite from different deposits show no difference in ∑ in one crystal and a slightly smaller value of ∑ in the outer part of the other crystal compared to the inner part. The ∑ of monazites from pegmatites that intrude genetically related granitic rocks in North Carolina is found to be either higher or lower than the ∑ of monazites in the intruded host rock. These results indicate that the fractionation of the rare-earth elements is not a simple unidirectional process.
When a cerium-earth mineral undergoes replacement, its rare-earth elements may be fractionated into two parts, one forming a new mineral with ∑ that is smaller, and the other a second new mineral with ∑ that is larger than that of the original mineral.
The complete analysis of a cerium-earth mineral to determine its ∑ is time consuming. The discovery of a direct relationship between ∑ and the Ce/(Nd + Y) atomic ratio in cerium earth minerals allows a rapid determination of ∑ from spectrograms obtained in a previously described method for determining thorium in these minerals.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(57)90077-7","issn":"00167037","usgsCitation":"Murata, K.J., Rose, H.J., Carron, M.K., and Glass, J., 1957, Systematic variation of rare-earth elements in cerium-earth minerals: Geochimica et Cosmochimica Acta, v. 11, no. 3, p. 141-161, https://doi.org/10.1016/0016-7037(57)90077-7.","productDescription":"21 p.","startPage":"141","endPage":"161","numberOfPages":"21","costCenters":[],"links":[{"id":218802,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"11","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505ba371e4b08c986b31fcdc","contributors":{"authors":[{"text":"Murata, K. J.","contributorId":18759,"corporation":false,"usgs":true,"family":"Murata","given":"K.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":359670,"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":359673,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Carron, M. K.","contributorId":59492,"corporation":false,"usgs":true,"family":"Carron","given":"M.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":359671,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Glass, J.J.","contributorId":75621,"corporation":false,"usgs":true,"family":"Glass","given":"J.J.","email":"","affiliations":[],"preferred":false,"id":359672,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70209047,"text":"70209047 - 1956 - Ringworm in a population of snowshoe hares","interactions":[],"lastModifiedDate":"2020-03-12T10:29:41","indexId":"70209047","displayToPublicDate":"2020-03-12T10:08:09","publicationYear":"1956","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2373,"text":"Journal of Mammalogy","onlineIssn":"1545-1542","printIssn":"0022-2372","active":true,"publicationSubtype":{"id":10}},"title":"Ringworm in a population of snowshoe hares","docAbstract":"The occurrence of ringworm, or dermatomycosis, in wild animals has been rarely reported. DeLamater (1939) described infections of Trichophyton mentagrophytes in common gray squirrels on and near the Johns Hopkins University campus at Baltimore. Errington (1942) and Charles (1946) reported on the occurrence of T. mentagrophytes in 35 of 364 litters (9.6%) of muskrats (Ondatra zibethicus zibethicus) in northwestern Iowa. Ninety-eight of 134 members (73%) of infected litters were recorded as contracting the fungus disease; of the 98, 90 died. Paul (1917), Lawrence (1918), and Connor (1932) mentioned ringworm epidemics of T. mentagrophytes among mice in wheat stacks of New South Wales and Victoria.
","language":"English","publisher":"Oxford Academic","doi":"10.2307/1375533","usgsCitation":"Adams, L.W., Salvin, S.B., and Hadlow, W.J., 1956, Ringworm in a population of snowshoe hares: Journal of Mammalogy, v. 37, no. 1, p. 94-99, https://doi.org/10.2307/1375533.","productDescription":"6 p.","startPage":"94","endPage":"99","costCenters":[],"links":[{"id":373177,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","otherGeospatial":"Bull Island, Flathead Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -114.12305831909178,\n 47.76402232094469\n ],\n [\n -114.10932540893555,\n 47.76402232094469\n ],\n [\n -114.10932540893555,\n 47.77463696233246\n ],\n [\n -114.12305831909178,\n 47.77463696233246\n ],\n [\n -114.12305831909178,\n 47.76402232094469\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"37","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Adams, Lowell W.","contributorId":37655,"corporation":false,"usgs":true,"family":"Adams","given":"Lowell","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":784621,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Salvin, S. B.","contributorId":223228,"corporation":false,"usgs":false,"family":"Salvin","given":"S.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":784622,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hadlow, W. J.","contributorId":223229,"corporation":false,"usgs":false,"family":"Hadlow","given":"W.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":784623,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"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}]}} ]}