{"pageNumber":"158","pageRowStart":"3925","pageSize":"25","recordCount":4111,"records":[{"id":13513,"text":"ofr6897 - 1968 - The geologic classification of the meteorites","interactions":[],"lastModifiedDate":"2012-02-02T00:06:38","indexId":"ofr6897","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-97","title":"The geologic classification of the meteorites","docAbstract":"The meteorite classes of Prior and Mason are assigned to three proposed genetic groups on the basis of a combination of compositional, mineralogical, and elemental characteristics: l) the calcium-poor, volatile-rich carbonaceous chondrites and achondrites; 2) the calcium-poor, volatile-poor chondrites (enstatite, bronzite, hypersthene, and pigeonite), achondrites (enstatite, hypersthene, and pigeonite), stonyirons (pallasites, siderophyre), and irons; and, 3) the calcium-rich (basaltic) achondrites. Chondrites are correlated with calcium-poor achondrites and the silicate phase of the pallasitic meteorites on Fe contents of olivine and pyroxene; and with metal of the stony-irons and irons on the basis of trace elements (Ga and Ge). Transitions in structure and texture between the chondrites and achondrites are recognized. The Van Schmus-Wood chemical-petrologic classification of the chondrites has been modified and expanded to a mineralogic-petrologic classification of the chondrites and calcium-poor achondrites. \r\n\r\nChondrites apparently are the first rocks of the solar system. Paragenetic and textural relations in the Murray carbonaceous chondrite shed new light on the manner of accretion, and on the character of dispersed solid materials ('dust', and chondrules and metal) that existed in the solar system before accretion. \r\n\r\nTwo pre-accretionary mineral assemblages (components) are recognized in the carbonaceous chondrites and in the unequilibrated volatile-poor chondrites. They are: 1) a 'low temperature' water-, rare gas-, and carbon-bearing component; and, 2) a high temperature anhydrous silicate and metal component. Paragenetic relations indicate that component 2 materials predate chondrite formation. An accretionary assemblage (component 3) also is recognized in the carbonaceous chondrites and in the unequilibrated volatile-poor chondrites. Component 3 consists of very fine grains of olivine and pyroxene, which occur as pervasive disseminations, as small irregular aggregates of grains, and as large subround to round, finely granular accretional chondrules. \r\n\r\nEvidence in Murray indicates that component 3 silicates precipitated abruptly and at low pressures, possibly from a high temperature gas, in an environment that contained dispersed component 1 and 2 materials. All component 3 aggregates in Murray contain component 1 material, most commonly as flakes, and locally as tiny granules and larger spherules, some of which are hollow and some of which were broken prior to their mechanical incorporation in accretionary chondrules. Accretion may have occurred as ices associated with dispersed water-bearing component 1 materials temporarily melted during the precipitation of component 3 silicates, and then abruptly refroze to form an icy cementing material. Group 1 materials may be cometary, and group 2 materials may be asteroidal. Schematic models are proposed. \r\n\r\nEvidence is reviewed for the lunar origin of the pyroxeneplagioclase achondrites. On the basis of natural remanent magnetism, it is suggested that the very scarce diopside-olivine achondrites may be samples from Mars. A classification of the meteorite breccias, including the calcium-poor and calcium-rich mesosiderites, and irons that contain silicate fragments, is proposed. A fragmentation history of the meteorites is outlined on the basis of evidence in the polymict breccias, and from gas retention ages in stones and exposure ages in irons. Cometal impacts appear to have caused the initial fragmentation, stud possibly the perturbation of orbits, of two inferred asteroidal bodies (enstatite and bronzite), one and possibly both events occurring before 2000 m.y. ago. Several impacts apparently occurred on the inferred hypersthene body in the interval 1000 to 2000 m.y. ago. \r\n\r\nMajor breakups of the three bodies apparently occurred as the result of interasteroidal collisions at about 900 m.y. ago, and 600 to 700 m.y. ago. The breakups were followed by a number of fr","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6897","usgsCitation":"Elston, D.P., 1968, The geologic classification of the meteorites: U.S. Geological Survey Open-File Report 68-97, 271 p. ill. (some folded, some col.) ;30 cm., https://doi.org/10.3133/ofr6897.","productDescription":"271 p. ill. (some folded, some col.) ;30 cm.","costCenters":[],"links":[{"id":144632,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0097/report-thumb.jpg"},{"id":41989,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41990,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41991,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41992,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41993,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41994,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41995,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0097/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41996,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0097/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d9f5","contributors":{"authors":[{"text":"Elston, Donald Parker","contributorId":38150,"corporation":false,"usgs":true,"family":"Elston","given":"Donald","email":"","middleInitial":"Parker","affiliations":[],"preferred":false,"id":167926,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":19921,"text":"ofr68170 - 1968 - Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah","interactions":[{"subject":{"id":19921,"text":"ofr68170 - 1968 - Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah","indexId":"ofr68170","publicationYear":"1968","noYear":false,"title":"Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah"},"predicate":"SUPERSEDED_BY","object":{"id":6172,"text":"pp688 - 1971 - Sedimentary features of the Blackhawk Formation (Cretaceous) in the Sunnyside District, Carbon County, Utah","indexId":"pp688","publicationYear":"1971","noYear":false,"title":"Sedimentary features of the Blackhawk Formation (Cretaceous) in the Sunnyside District, Carbon County, Utah"},"id":1}],"supersededBy":{"id":6172,"text":"pp688 - 1971 - Sedimentary features of the Blackhawk Formation (Cretaceous) in the Sunnyside District, Carbon County, Utah","indexId":"pp688","publicationYear":"1971","noYear":false,"title":"Sedimentary features of the Blackhawk Formation (Cretaceous) in the Sunnyside District, Carbon County, Utah"},"lastModifiedDate":"2012-02-02T00:07:42","indexId":"ofr68170","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-170","title":"Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah","docAbstract":"The Blackhawk Formation at Sunnyside, Utah, was deposited along the western margin of the Western Interior Cretaceous sea during southeastward withdrawal of the sea. Sand was the dominant type of land-derived sediment deposited in the Sunnyside district during the regressive phases. Sand bodies prograded seaward in response to changing sediment supply from a source west of Sunnyside. Where conditions were favorable for the accumulation of vegetable material, peat deposits formed and were later changed to bituminous Coal by diagenesis. Studies of the coal bed show that the coals were formed from accumulation of small, low-growing plants and plant debris that was transported into the area of accumulation. Remains of large plants in the coals are rare. \r\n\r\nTrace fossils, which are tracks, trails and burrows formed by organisms and preserved in the rock, are extremely abundant in the Blackhawk rocks. These biogenic sedimentary structures are common in Cretaceous deposits throughout the western United States. Trace fossil distribution in the rocks is controlled by the depositional environment preferred by their creators. A study of the trace fossils of a. locality allows a more precise determination of the conditions during deposition of the sediments. Water depth, bottom conditions, salinity, current velocity and amount of suspended nutrients in the water are some of the environmental factors that may be reconstructed by studying trace fossils. \r\n\r\nThe Blackhawk Formation at Sunnyside comprises the members, the Kenilworth Member and the Sunnyside Member. Field studies show that the formation may be further subdivided in the Sunnyside district., according to the precepts of units of mappable thickness and similar lithologic characteristics. The Blackhawk pinches out eastward and north. ward into the Mancos Shale, and names for submembers become meaningless. Names are of value in the region of interest, however, because of the prominence of the named units. \r\n\r\nCoal mining is the main industry of the Book Cliffs region. Mines of the Sunnyside district are plagued by coal mine bumps, which are sudden, catastrophic releases of stress in the coal. Bumps cause loss of life, property age, and loss of profit to mining companies. Bumps occur when shear stress built up in the coal exceeds the shear Strength of the coal. Differential overburden pressure, faulting and tectonic activity, and lithology and structure of roof rocks are factors which influence bumps. Petroleum and natural gas (methane), which occur locally in pockets in the roof rocks above coal beds, may be diagenetic products of organic-rich sediments.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/ofr68170","usgsCitation":"Maberry, J.O., 1968, Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah: U.S. Geological Survey Open-File Report 68-170, 180 p. ill., maps ;28 cm., https://doi.org/10.3133/ofr68170.","productDescription":"180 p. ill., maps ;28 cm.","costCenters":[],"links":[{"id":153250,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0170/report-thumb.jpg"},{"id":49428,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0170/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49429,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0170/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49430,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0170/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49431,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0170/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fbda6","contributors":{"authors":[{"text":"Maberry, John O.","contributorId":87134,"corporation":false,"usgs":true,"family":"Maberry","given":"John","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":181740,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":13510,"text":"ofr6896 - 1968 - Character and geologic habitat of potential deposits of water, carbon and rare gases on the moon","interactions":[],"lastModifiedDate":"2012-02-02T00:06:37","indexId":"ofr6896","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-96","title":"Character and geologic habitat of potential deposits of water, carbon and rare gases on the moon","language":"ENGLISH","doi":"10.3133/ofr6896","usgsCitation":"Elston, D.P., 1968, Character and geologic habitat of potential deposits of water, carbon and rare gases on the moon: U.S. Geological Survey Open-File Report 68-96, 25 p. ill., maps (some folded) ;27 cm., https://doi.org/10.3133/ofr6896.","productDescription":"25 p. ill., maps (some folded) ;27 cm.","costCenters":[],"links":[{"id":144629,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e3e4b07f02db5e5919","contributors":{"authors":[{"text":"Elston, Donald Parker","contributorId":38150,"corporation":false,"usgs":true,"family":"Elston","given":"Donald","email":"","middleInitial":"Parker","affiliations":[],"preferred":false,"id":167919,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70011498,"text":"70011498 - 1968 - Mineralogy as a function of depth in the prehistoric Makaopuhi tholeiitic lava lake, Hawaii","interactions":[],"lastModifiedDate":"2020-11-29T16:49:47.663291","indexId":"70011498","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1336,"text":"Contributions to Mineralogy and Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Mineralogy as a function of depth in the prehistoric Makaopuhi tholeiitic lava lake, Hawaii","docAbstract":"

The electron probe X-ray microanalyzer has been used to determine the compositional variability of the groundmass minerals and glass in 10 specimens from a complete 225-foot section of the prehistoric tholeiitic lava lake of Makaopuhi Crater, Hawaii. The order of beginning of crystallization was: (1) chromite, (2) olivine, (3) augite, (4) plagioclase, (5) pigeonite, (6) iron-titanium oxides and orthopyroxene, (7) alkali feldspar and apatite, and (8) glass.

Although the lake is chemically tholeiitic throughout, the occurrence of ferromagnesian minerals is as though there were a gradation from alkali olivine basalt in the upper chill downwards to olivine tholeiite. Groundmass olivine decreases downwards and disappears at about 20 feet. Pigeonite is absent in the uppermost 5±2 feet, then increases in amount down to 20 feet, below which augite and pigeonite coexist in constant 2∶1 proportions. Strong zoning and metastable compositions characterize the pyroxenes of the chilled zones, but these features gradually disappear towards the interior of the lake to give way to equilibrium pyroxenes. Relatively homogeneous poikilitic orthopyroxene (≈ Ca4Mg70Fe26) occurs in the olivine cumulate zone, having formed partly at the expense of pre-existing olivine, augite, and pigeonite (≈ Ca8Mg66Fe26). The growth of orthopyroxene is believed to have been facilitated by the slower cooling rate and higher volatile pressure at depth, and by the rise in Mg/Fe ratio of the liquid due to the partial dissolution of settled olivine.

Unlike olivine and pyroxene, feldspar is least zoned in the upper and lower chilled regions. The greatest range of compositional zoning in feldspar occurs at 160 to 190 feet, where it extends continuously from Or1.0Ab22An77 to Or64Ab33An3. The feldspar fractionation trend in the An-Ab-Or triangle gradually shifts with depth toward more “equilibrium” trends, even though the zoning becomes more extreme. The variation with depth in the initial (core) composition of the plagioclase suggests the influence of either slow nucleation and growth (undercooling) or slow diffusion in the liquid, relative to the rate of cooling.

Idiomorphic opaque inclusions in olivine phenocrysts are chrome-spinels showing continuous variation from 60 percent chromite to 85 percent ulvospinel and to magnetite-rich spinel. A pre-eruption trend of increasing Al with decreasing Cr can be recognized in chromites from the upper chill. Most of the inclusions show a trend of falling Cr and Al, toward an ulvospinelmagnetite solid solution which is progressively poorer in Usp with depth. This trend was produced by solid state alteration of the chromite inclusions during cooling in the lava lake. Ilmenite (average Ilm91Hm9) coexists with variably oxidized titaniferous magnetite in the basalt groundmass. Estimated oxygen fugacities agree well with other independent determinations in tholeiitic basalt. No sulfide phase has been detected.

Fractional crystallization produced a groundmass glass of granitic composition. Average, in percent, is: SiO2, 75.5; Al2O3, 12.5; K2O, 5.7; Na2O, 3.1; CaO, 0.3; MgO, 0.05; total FeO, 1.2; and TiO2, 0.8. Normative Or> Ab. Minor changes in glass composition with depth are consistent with a greater approach towards the granite minimum. Incipient devitrification precluded reliable analysis of glass from the lower half of the section. The SiO2-phase associated with devitrification contains alkalis and Al and is believed to be cristobalite. Needle-like apatite crystals in the groundmass glass are Siand Fe-bearing fluorapatites containing appreciable rare earths (predominantly Ce) and variable Cl.

The grain-size and maximum An content of the cores of plagioclase grains were controlled by cooling rate and are at a maximum at the center of the section. The most homogeneous pyroxene (and olivine, MOORE and EVANS, 1967), most equilibrium pyroxene trends, most abundant alkali feldspar, and most equilibrium feldspar trends are found at 160 to 190 feet, which is appreciably below that part of the lake which was slowest to crystallize. Volatile pressure, increasing with depth, possibly controlled the degree of attainment of equilibrium more than cooling rate.

Since they are dependent on cooling history, some of the modal criteria commonly used for recognizing basalt types, such as the absence of Ca-poor pyroxene, presence of groundmass olivine, and the presence of alkali feldspar, should be applied with caution. Petrographic comparison of basalts from one flow, volcano, or province, with another, should recognize the possible variations due to cooling history alone.

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\"}}]}","volume":"17","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a5acce4b0c8380cd6f134","contributors":{"authors":[{"text":"Evans, B.W.","contributorId":86896,"corporation":false,"usgs":true,"family":"Evans","given":"B.W.","email":"","affiliations":[],"preferred":false,"id":361266,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Moore, J.G.","contributorId":67496,"corporation":false,"usgs":true,"family":"Moore","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":361265,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70210850,"text":"70210850 - 1967 - Silver-bearing black calcite in western mining districts","interactions":[],"lastModifiedDate":"2020-06-29T16:48:36.515266","indexId":"70210850","displayToPublicDate":"2020-01-01T11:45:40","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Silver-bearing black calcite in western mining districts","docAbstract":"

The name black calcite has been applied from time to time to a dark gray to black variety of calcite or aragonite in metalliferous ore deposits in the Western States. Most of the material shows curved, roughly rhombic cleavage. The color is due to dispersed minute grains of one or more oxides of manganese, so dispersed that they rarely show any relation to cleavage surfaces or outward crystal forms.Recent study shows that the black calcite from numerous metalliferous deposits in the Western States contains small amounts of several metals, especially zinc, lead, and silver; in places, the crude black calcite contains as much as one percent silver and the black residue remaining after solution of the calcite as much as 1,500 ounces of silver to the ton. Black calcite is recognized in some deposits of Late Cretaceous to early Tertiary age where the host is Paleozoic carbonate rocks; thus far, this variety contains the larger amounts of silver. It is also present in some vein deposits where the host is generally volcanic rocks of middle Tertiary age; these are known in many districts in the southwest and even though the lead and zinc content is noteworthy, the silver content rarely exceeds one ounce to the ton (8).By studying polished sections of black calcite from the Aurora mine, White Pine County, Nevada, three silver-bearing manganate minerals have been recognized; (1) an argentian chalcophanite containing 7.5 percent silver (Ag 2 O), to which, in a following paper, the name aurorite is given; (2) argentian todorokite containing 3.9 percent silver (Ag 2 O), and (3) hydrous silver-bearing lead manganese oxide, containing 1.18 percent silver (Ag 2 O).

","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.62.1.1","usgsCitation":"Hewett, D.F., and Radtke, A.S., 1967, Silver-bearing black calcite in western mining districts: Economic Geology, v. 62, no. 1, p. 1-21, https://doi.org/10.2113/gsecongeo.62.1.1.","productDescription":"21 p.","startPage":"1","endPage":"21","costCenters":[],"links":[{"id":375985,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","county":"White Pine County","otherGeospatial":"Aurora mine","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-114.0484,40.1186],[-114.0476,39.982],[-114.0474,39.9053],[-114.0469,39.7765],[-114.0468,39.747],[-114.0463,39.6464],[-114.0468,39.543],[-114.0472,39.4696],[-114.0472,39.4551],[-114.0476,39.4068],[-114.0478,39.3816],[-114.048,39.3666],[-114.0481,39.341],[-114.0483,39.2936],[-114.0484,39.2805],[-114.0488,39.2179],[-114.0488,39.2168],[-114.0502,39.1195],[-114.0506,39.0873],[-114.0515,39.0209],[-114.0517,39.0059],[-114.052,38.9994],[-114.052,38.9982],[-114.0512,38.9554],[-114.0507,38.9259],[-114.0497,38.8693],[-114.0495,38.8557],[-114.0491,38.8371],[-114.0491,38.8358],[-114.0492,38.7927],[-114.0492,38.765],[-114.0492,38.7587],[-114.0491,38.7138],[-114.0491,38.6775],[-114.5986,38.6776],[-114.6186,38.678],[-114.6375,38.6785],[-114.6776,38.6781],[-114.7554,38.6784],[-114.8168,38.678],[-114.8916,38.6782],[-114.9241,38.678],[-114.999,38.6777],[-115.0291,38.6937],[-115.0604,38.7107],[-115.0777,38.721],[-115.0969,38.7309],[-115.242,38.8093],[-115.363,38.874],[-115.3694,38.8769],[-115.4433,38.9162],[-115.4725,38.9325],[-115.5191,38.9578],[-115.9082,39.1615],[-115.9059,39.2947],[-115.9059,39.3219],[-115.9061,39.3369],[-115.9063,39.4638],[-115.8939,39.4605],[-115.8741,39.4652],[-115.8693,39.4679],[-115.8649,39.4755],[-115.8684,39.4806],[-115.8695,39.4851],[-115.8658,39.4901],[-115.8598,39.4922],[-115.8525,39.499],[-115.8518,39.5017],[-115.8524,39.5035],[-115.8523,39.5053],[-115.8444,39.5143],[-115.8414,39.5151],[-115.836,39.5182],[-115.8334,39.525],[-115.8279,39.5322],[-115.8271,39.5381],[-115.8306,39.5417],[-115.8341,39.5481],[-115.8363,39.5536],[-115.8374,39.5577],[-115.8361,39.564],[-115.8318,39.5685],[-115.83,39.5707],[-115.8263,39.5748],[-115.814,39.5891],[-115.8127,39.5945],[-115.8138,39.6],[-115.8195,39.6082],[-115.8164,39.6127],[-115.8181,39.6195],[-115.8227,39.6264],[-115.826,39.6378],[-115.8259,39.6446],[-115.8282,39.6478],[-115.8245,39.6523],[-115.8226,39.6563],[-115.823,39.6663],[-115.8234,39.6727],[-115.8233,39.6786],[-115.8237,39.6858],[-115.8248,39.6913],[-115.8312,39.6963],[-115.8314,39.7168],[-115.8305,39.7276],[-115.8315,39.7367],[-115.8266,39.7398],[-115.8236,39.7425],[-115.8223,39.7461],[-115.8193,39.747],[-115.815,39.7492],[-115.8119,39.7541],[-115.8106,39.7595],[-115.8129,39.7641],[-115.8128,39.7677],[-115.8127,39.7727],[-115.8126,39.7782],[-115.8118,39.7845],[-115.8093,39.7904],[-115.8085,39.7976],[-115.8102,39.8008],[-115.8137,39.8072],[-115.8152,39.8176],[-115.8121,39.8226],[-115.8085,39.8257],[-115.8054,39.8288],[-115.8023,39.8329],[-115.7986,39.8369],[-115.7967,39.8432],[-115.7984,39.846],[-115.7971,39.8496],[-115.7958,39.8527],[-115.7951,39.8595],[-115.8039,39.8678],[-115.8013,39.8746],[-115.8012,39.8787],[-115.8052,39.8896],[-115.8068,39.896],[-115.8061,39.9014],[-115.8036,39.905],[-115.8023,39.91],[-115.8081,39.9196],[-115.8139,39.9255],[-115.8162,39.9306],[-115.8173,39.9356],[-115.816,39.9387],[-115.8146,39.9464],[-115.8145,39.9528],[-115.8156,39.9573],[-115.8173,39.96],[-115.8241,39.9769],[-115.8276,39.981],[-115.8323,39.987],[-115.8334,39.9897],[-115.8344,39.9979],[-115.8344,40.0006],[-115.8337,40.0043],[-115.8341,40.0115],[-115.8302,40.0251],[-115.8283,40.0282],[-115.8288,40.0323],[-115.8317,40.0355],[-115.8346,40.0437],[-115.8315,40.0478],[-115.8278,40.0522],[-115.8276,40.0581],[-115.8317,40.0636],[-115.837,40.0682],[-115.8375,40.071],[-115.8344,40.0755],[-115.8349,40.0805],[-115.8384,40.085],[-115.8376,40.0946],[-115.8346,40.0959],[-115.8321,40.0995],[-115.8289,40.1076],[-115.8294,40.1121],[-115.8305,40.1167],[-115.8374,40.1286],[-115.6972,40.1289],[-115.6046,40.1284],[-115.5295,40.1264],[-115.4561,40.1266],[-115.4441,40.1264],[-115.3917,40.1264],[-115.2426,40.1257],[-115.0393,40.1241],[-114.8108,40.1222],[-114.6929,40.1214],[-114.6526,40.121],[-114.634,40.121],[-114.5312,40.1195],[-114.2256,40.1178],[-114.0484,40.1186]]]},\"properties\":{\"name\":\"White Pine\",\"state\":\"NV\"}}]}","volume":"62","issue":"1","noUsgsAuthors":false,"publicationDate":"1967-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Hewett, D. F.","contributorId":19927,"corporation":false,"usgs":true,"family":"Hewett","given":"D.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":791705,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Radtke, A. S.","contributorId":16408,"corporation":false,"usgs":true,"family":"Radtke","given":"A.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":791706,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70038229,"text":"70038229 - 1967 - Water resources inventory of Connecticut Part 2: Shetucket River Basin","interactions":[],"lastModifiedDate":"2014-04-09T12:35:29","indexId":"70038229","displayToPublicDate":"2012-04-22T09:08:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":108,"text":"Connecticut Water Resources Bulletin","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"11","title":"Water resources inventory of Connecticut Part 2: Shetucket River Basin","docAbstract":"The Shetucket River basin has a relatively abundant supply of water of generally good quality which is derived from precipitation that has fallen on the basin. Annual precipitation has ranged from about 30 inches to 75 inches and has averaged about 45 inches over a 35-year period. Approximately 20 inches of water are returned to the atmosphere each year by evaporation and transpiration; the remainder of the annual precipitation either flows overland to streams or percolates downward to the water table and ultimately flows out of the basin in the Shetucket River or as underflow through the deposits beneath. During the autumn and winter months precipitation normally is sufficient to cause a substantial increase in the amount of water stored underground and in surface reservoirs within the basins whereas in the summer most of the precipitation is lost through evaporation and transpiration, resulting in sharply reduced streamflow and lowered groundwater levels. The mean monthly storage of water in the basin on an average is 3.5 inches higher in November than it is in June.\nThe amount of water that flows out of the\nbasin in the Shetucket River represents the total\namount of water potentlally available for use by man.\nAnnual runoff from the entire basin above the\nQuinebaug River has ranged from about 13 to 42\ninches since 1929, and has averaged about 23\ninches (300 billion gallons). Although runoff\nindicates the total amount of water potentially\navailable, it is usually not economically or\nlegally feasible for man to use all of it. On\nthe other hand, with increased development, It\nis possible that some water will be reused several\ntimes.\nThe water available may be tapped as it flows\nthrough the area or is temporarily stored in\nstreams, lakes, and aquifers. The amounts that\ncan be developed vary from place to place and\ntime to time, depending on the amount of precipitation,\non the size of drainage area, on the\nthickness, permeability and areal extent of aquifers,\nand on the variations in chemical and\nphysical quality of the water.\nDifferences in streamflow from point to\npoint are due primarily to differences in the\nproportion of stratified drift in the drainage\nbasin above each point, which affect the timing\nof streamflow, and to differences in precipitation,\nwhich affect the amount of streamflow.\nInformation on streamflow from gaging stations\nmay be extended to ungaged sites by accounting\nfor both of these factors ,in calculations.\nFuture floods on the upper Willimantic\nRiver or the Shetucket River are unlikely to\ncause major damage so long as buildings are not\nconstructed below the highest flood elevations to\nbe expected with the present system of reservoirs\nfor flood control.\nGround water can be obtained from wells\nalmost anywhere in the Shetucket River basin, but\nthe amount obtainable from individual wells at\nany particular point depends upon the type and\nwater-bearing properties of the aquifers present.\nFor practical purposes, the earth materials in\nthe basin comprise three aquifers--stratified\ndrift, till, and bedrock,\nStratified drift is the only aquifer generally capable of yielding more than 100 gpm to\nindividual wells. This aquifer covers about 18\npercent of the basin and occurs chiefly In lowlands\nwhere it overlies till or bedrock. Coefficient\nof permeability of the coarse-grained unit\nof stratified drift averages about 1,900 gpd per\nsq ft. Drilled, screened wells tapping this unit,\nare known to yield from 200 to 675 gpm. Dug wells\nin coarse-grained stratified drift should supply\nat least 2 gpm per foot of drawdown over an 8-hour\nperiod. Fine-grained stratified drift has an\naverage coefficient of permeability of about 400\ngpd per sq ft and can usually yield to dug wells\nsupplies sufficient for household use.\nTill and bedrock are widespread in extent but\ncan provide only small to moderate water supplies.\nTill is tapped chiefly by dug wells; permanent\nsupplies of more than 200 gpd can be obtained from\ndug wells at a majority of sites in areas of till,\nbut there are many sites where the till is too\nimpermeable or too thin to provide this much water\nthroughout the year. The coefficient of permeability of till ranges from about 0.2 gpd per sq ft to\n55 gpd per sq it. Bedrock Is tapped chiefly by\ndrilled wells, about 90 percent of which will\nsupply at least 3 gpm. Very few, however, will\nsupply more than 50 gpm.\nThe amount of ground water potentially available\nIn an area depends upon the amount of groundwater\noutflow, the amount of ground water in storage,\nand the quantity of water available by Induced\ninfiltration from streams and lakes. From\ndata on permeability, saturated thickness, recharge,\nyield from aquifer storage, well performance, and\nstreamflow, preliminary estimates of ground-water\navailability can be made for any point in the\nbasin. Long-term yields estimated for 15 areas\nespecially favorable for development of large\nground-water supplies ranged from 1.3 to 61.8 mgd.\nDetailed site studies to determine optimum yields,\ndrawdowns, and spacing of individual wells are\nneeded before major ground-water development is\nundertaken In these or other areas.\nThe chemical quality of water in the Shetucket\nbasin Is generally good to excellent. Samples of\nnaturally occurring surface water collected from\n32 sites contained less than 61 ppm of dissolved\nsolids and less than 32 ppm of hardness. Water\nfrom wells is more highly mineralized than naturally\noccurring water from streams. Even so only\n7 percent of wells sampled yielded water with more\nthan 200 ppm of dissolved sol-ids and only 9 percent\nyielded water with more than 120 ppm of hardness.\nEven in the major rivers, which are used to\ntransport industrial waste, the dissolved mineral\ncontent is less than 100 ppm and hardness rarely\nexceeds 40 ppm. One notable exception occurs in\nthe lower reaches of Little River where an\nexceptional amount of industrial waste is discharged\ninto the river near Versailles. This\nwaste is particularly noticeable during low\nstreamflow.\nIron and manganese In both ground water and\nsurface water are the only constituents whose concentrations\ncommonly exceed recommended limits for\ndomestic and industrial use. Most wells in the\n basin yield clear water with little or no iron or\nmanganese, but distributed among them are wells\nwith ground water that contains enough of these dissolved\nconstituents to be troublesome for most uses.\niron concentrations in naturally occurring\nstream water exceeded 0.3 ppm under tow-flow conditions\nat 20 percent of the sites sampled. Large\nconcentrations of iron in stream water result\nfrom discharge of iron-bearing ground water or\nfrom the discharge of water from swamps. In\nswamps the iron is released largely from decaying\nvegetation.\nGround water more than 30 feet below the\nland surface has a relatively constant temperature,\nusually between 48°F and 50°F. Water\ntemperature in very shallow wells may fluctuate\nfrom about 38°F in February or March to about\n55°F in late summer. Water temperature in the\nlarger streams fluctuates much more widely,\nranging from 32°F at least for brief periods\nin winter, to about 85°F occasionally during\nThe quantity of suspended sediment transported\nby streams in the basin is negligible,\nthough amounts large enough to be troublesome\nmay occur locally at times.\nThe total amount of water used In the\nShetucket Rlver basin for all purposes during\n1961 was about 5,810 million gallons~ which is\nequivalent to 208 gpd per person, Public water\nsystems supplied the domestic needs of nearly\nhalf the population of the basin; 10 systems\nwere sampled, all of which provided water of\nbetter quality than the U.S. Public Health Service\nsuggests for drinking water standards.","language":"English","publisher":"Connecticut Water Resources Commission","collaboration":"Prepared by the U.S. Geological Survey in cooperation with the Connecticut Water Resource Commission","usgsCitation":"Thomas, M.P., Bednar, G.A., Thomas, C.E., and Wilson, W.E., 1967, Water resources inventory of Connecticut Part 2: Shetucket River Basin: Connecticut Water Resources Bulletin 11, Report: viii, 96 p.; 4 Plates: 36.00 x 58.00 inches and smaller.","productDescription":"Report: viii, 96 p.; 4 Plates: 36.00 x 58.00 inches and smaller","numberOfPages":"112","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":258791,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/ctwrb/0011/report.pdf","size":"22651","linkFileType":{"id":1,"text":"pdf"}},{"id":258792,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ctwrb/0011/report-thumb.jpg"},{"id":285972,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038229/plate-c.pdf"},{"id":285973,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038229/plate-d.pdf"},{"id":285970,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038229/plate-a.pdf"},{"id":285971,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038229/plate-b.pdf"}],"scale":"48000","country":"United States","state":"Connecticut","otherGeospatial":"Shetucket River Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -72.466667,41.533333 ], [ -72.466667,42.066667 ], [ -72.0,42.066667 ], [ -72.0,41.533333 ], [ -72.466667,41.533333 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bcb78e4b08c986b32d681","contributors":{"authors":[{"text":"Thomas, Mendall P.","contributorId":104314,"corporation":false,"usgs":true,"family":"Thomas","given":"Mendall","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":463693,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bednar, Gene A.","contributorId":81881,"corporation":false,"usgs":true,"family":"Bednar","given":"Gene","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":463692,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Thomas, Chester E. Jr.","contributorId":37182,"corporation":false,"usgs":true,"family":"Thomas","given":"Chester","suffix":"Jr.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":463690,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wilson, William E.","contributorId":46478,"corporation":false,"usgs":true,"family":"Wilson","given":"William","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":463691,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":5224450,"text":"5224450 - 1967 - Magruder Park Swamp","interactions":[],"lastModifiedDate":"2012-02-02T00:15:33","indexId":"5224450","displayToPublicDate":"2010-06-16T12:17:38","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3119,"text":"Prince Georges Post","active":true,"publicationSubtype":{"id":10}},"title":"Magruder Park Swamp","docAbstract":"The last Tuesday in August, between five-thirty and seven in the evening, we zigzaged through this glorious jungle, attended by a family of Wood Pewees for whom we seemed to be stirring up a feast of flying insects. There was gentle background music by Mole Crickets. A few steps in from the playing field and we were out of sight in ten-foot-high Cattails. All through, we met -- as high as we, or higher--clumped Cinnamon Ferns, deep-rose Joe Pye Weed, and orange, pendent flowers of Jewelweed (first cousins to Balsam and Sultana). Here and there were soft, white spikes of Canadian Burnet, a rare plant hereabouts, and deep purple Ironweed. Dense-foliaged Hempweed climbed over bushes and up small trees, filling the air with its delicate fragrance. Arrowleaf Tear-thumb snatched at us with tiny prongs on its angled stems. Once in a while we tripped over huge sedge tussocks, half-hidden in the tangle. A few times we steered around a small bush of Poison Sumac. The next day We remembered seeing ninety kinds of plants on this hasty trip. Skunk Cabbage leaves recalled April, when a person, from the edge of the lawn, could see huge clumps of them all the way across the swamp. The sky had been washed by last week's downpours; scattered Gums were reddening; and Maples were getting ready for crimson beauty a month from now. There wasn't a mosquito! (Ed. Note.-The Hyattsville City Council is taking pains to preserve this interesting swamp.)","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Prince Georges Post","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","usgsCitation":"Hotchkiss, N., and Uhler, F., 1967, Magruder Park Swamp: Prince Georges Post, v. 36, no. 33.","productDescription":"2","startPage":"2","numberOfPages":"2","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":201803,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"36","issue":"33","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db64965f","contributors":{"authors":[{"text":"Hotchkiss, N.","contributorId":48655,"corporation":false,"usgs":true,"family":"Hotchkiss","given":"N.","affiliations":[],"preferred":false,"id":341713,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Uhler, F.M.","contributorId":81965,"corporation":false,"usgs":true,"family":"Uhler","given":"F.M.","email":"","affiliations":[],"preferred":false,"id":341714,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":4072,"text":"cir545 - 1967 - Marine sediment sample preparation for analysis for low concentrations of fine detrital gold","interactions":[],"lastModifiedDate":"2017-08-27T17:54:55","indexId":"cir545","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"545","title":"Marine sediment sample preparation for analysis for low concentrations of fine detrital gold","docAbstract":"Analyses by atomic absorption for detrital gold in more than 2,000 beach, offshore, marine-terrace, and alluvial sands from southern Oregon have shown that the values determined from raw or unconcentrated sediment containing small amounts of gold are neither reproducible nor representative of the initial sample. This difficulty results from a 'particle sparsity effect', whereby the analysis for gold in a given sample depends more upon the occurrence of random flakes of gold in the analyzed portion than upon the actual gold content of the sample. \r\n\r\nThe particle sparsity effect can largely be eliminated by preparing a gold concentrate prior to analysis. A combination of sieve, gravimetric, and magnetic separation produces a satisfactory concentrate that yields accurate and reproducible analyses. In concentrates of nearly every marine and beach sand studied, the gold occurs in the nonmagnetic fraction smaller than 0.124 mm and with a specific gravity greater than 3.3. The grain size of gold in stream sediments is somewhat more variable. \r\n\r\nAnalysis of concentrates provides a means of greatly increasing the sensitivity of the analytical technique in relation to the initial sample. Gold rarely exceeds 1 part per million in even the richest black sand analyzed; to establish the distribution of gold (and \r\nplatinum) in marine sediments and its relationship to source and environmental factors, one commonly needs to know their content to the part per billion range. Analysis of a concentrate and recalculation to the value in the initial sample permits this degree of sensitivity.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir545","usgsCitation":"Clifton, H.E., Hubert, A., and Phillips, R.L., 1967, Marine sediment sample preparation for analysis for low concentrations of fine detrital gold: U.S. Geological Survey Circular 545, 11 p. :map ;26 cm., https://doi.org/10.3133/cir545.","productDescription":"11 p. :map ;26 cm.","costCenters":[],"links":[{"id":124628,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1967/0545/report-thumb.jpg"},{"id":31166,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1967/0545/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a17e4b07f02db604414","contributors":{"authors":[{"text":"Clifton, H. Edward","contributorId":46503,"corporation":false,"usgs":true,"family":"Clifton","given":"H.","email":"","middleInitial":"Edward","affiliations":[],"preferred":false,"id":148120,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hubert, Arthur","contributorId":17977,"corporation":false,"usgs":true,"family":"Hubert","given":"Arthur","affiliations":[],"preferred":false,"id":148119,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Phillips, R. Lawrence","contributorId":81478,"corporation":false,"usgs":true,"family":"Phillips","given":"R.","email":"","middleInitial":"Lawrence","affiliations":[],"preferred":false,"id":148121,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":36178,"text":"b1185D - 1967 - The Morro do Ferro thorium and rare-earth ore deposit, Pocos de Caldas district, Brazil","interactions":[],"lastModifiedDate":"2012-02-02T00:09:45","indexId":"b1185D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1185","chapter":"D","title":"The Morro do Ferro thorium and rare-earth ore deposit, Pocos de Caldas district, Brazil","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/b1185D","usgsCitation":"Wedow, H., 1967, The Morro do Ferro thorium and rare-earth ore deposit, Pocos de Caldas district, Brazil: U.S. Geological Survey Bulletin 1185, 34 p. :ill., maps ;24 cm., https://doi.org/10.3133/b1185D.","productDescription":"34 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":165705,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1185d/report-thumb.jpg"},{"id":64153,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1185d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac7e4b07f02db67b450","contributors":{"authors":[{"text":"Wedow, Helmuth Jr.","contributorId":14374,"corporation":false,"usgs":true,"family":"Wedow","given":"Helmuth","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":215898,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":34336,"text":"b1241F - 1967 - Geology and petrology of the Greenville quadrangle, Piscataquis and Somerset Counties, Maine","interactions":[],"lastModifiedDate":"2017-09-20T13:08:31","indexId":"b1241F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1241","chapter":"F","title":"Geology and petrology of the Greenville quadrangle, Piscataquis and Somerset Counties, Maine","docAbstract":"

In the Greenville quadrangle, west-central Maine, slate, siltstone, and sandstone (calcareous and noncalcareous) of probable Silurian to Early Devonian age are intruded by a large mafic pluton and two granitic stocks of probable Early Devonian age. Ages of the sedimentary rocks are based upon tentative correlations with fossiliferous beds in adjacent quadrangles because the few fossils in the Greenville quadrangle are nondiagnostic; ages of the intrusive rocks are based upon radiometric age determinations. The sedimentary rocks are tightly folded about northeast-trending axes and have strong slaty cleavage. Widespread graded bedding is very useful in determining the tops of beds and thus the location of fold axes. The sedimentary rocks are in the chlorite zone of metamorphism except in the contact aureoles where the metamorphism ranges from the biotite zone, through the andalusiite-amphibole zone, to the sillimanite-cordierite zone adjacent to the intrusions; retrograde metamorphism is a minor local feature.

The mafic rocks are part of the Moxie pluton, which extends southwest and northeast of the Greenville quadrangle for a total distance of about 45 miles. Troctolite and norite are the principal rock types; gabbro is less common. Plagioclase is the dominant mineral; it usually makes up 50-75 percent of the rock. Olivine and orthopyroxene are widespread, clinopyroxene is uncommon and biotite and hornblende are generally present in small amounts. The rocks can be separated into magnesium-rich and iron-rich varieties; magnesium-rich olivine and orthopyroxene are usually accompanied by plagioclase containing from 57 to 77 percent anorthite, and iron-rich olivine and orthopyroxene are associated with plagioclase containing about 50-62 percent anorithite. Compositional layering is rare, but flow structure is very common. Flow structure generally dips northward to eastward, whereas geophysical data indicate that the contacts of the pluton dip southeastward. The granitic stocks are discordant pipelike bodies that range from granodiorite to quartz monzonite in composition. Both the mafic and the felsic intrusions are undeformed and unmetamorphosed.

Slate quarrying was once an important industry in the region, but in 1965 only one quarry was active at Monson just east of the report area. Slate is a potential source of raw material for lightweight concrete aggregate. There are several possible sites for stone quarries in the intrusive masses. Sand and gravel resources seem to be limited. Small amounts of sulfides that have low copper and nickel values are known at a few places in the mafic pluton.

","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to general geology, 1966","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b1241F","usgsCitation":"Espenshade, G.H., and Boudette, E.L., 1967, Geology and petrology of the Greenville quadrangle, Piscataquis and Somerset Counties, Maine: U.S. Geological Survey Bulletin 1241, Report: v, 60 p.; Plate: 16.83 x 21.42 inches, https://doi.org/10.3133/b1241F.","productDescription":"Report: v, 60 p.; Plate: 16.83 x 21.42 inches","startPage":"F1","endPage":"F60","costCenters":[],"links":[{"id":96360,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1241f/report.pdf","text":"Report","size":"4.43 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":96361,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1241f/plate-1.pdf","text":"Plate 1","size":"2.89 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"},{"id":165889,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1241f/report-thumb.jpg"}],"country":"United States","state":"Maine","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -69.5,\n 45.4\n ],\n [\n -69.75,\n 45.4\n ],\n [\n -69.75,\n 45.50\n ],\n [\n -69.5,\n 45.5\n ],\n [\n -69.5,\n 45.4\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db6842de","contributors":{"authors":[{"text":"Espenshade, Gilbert H.","contributorId":97474,"corporation":false,"usgs":true,"family":"Espenshade","given":"Gilbert","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":212806,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Boudette, Eugene L.","contributorId":65085,"corporation":false,"usgs":true,"family":"Boudette","given":"Eugene","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":212805,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70009780,"text":"70009780 - 1967 - The occurrence and origin of lamellar troilite in iron meteorites","interactions":[],"lastModifiedDate":"2024-03-07T16:19:02.936871","indexId":"70009780","displayToPublicDate":"1967-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"The occurrence and origin of lamellar troilite in iron meteorites","docAbstract":"

A number of iron meteorites contain elongated inclusions consisting predominantly of troilite, which have been termed Reichenbach lamellae. Two types of inclusions exist, the first up to 6 cm long and 0·2 mm wide, the second up to 2 cm long and 3 mm wide. The first type contains troilite with subordinate daubreelite and is commonly rimmed by schreibersite and swathing kamacite; the second consists largely of troilite with daubreelite and rare graphite and silicate grains.

Both types formed from a residual sulfide melt after the solidification of Ni\"singleFe metal. Swatching kamacite surrounding troilite in iron meteorites formed by nucleation at the troilite-metal interface during the formation of the Widmanstätten texture.

Meteorites containing troilite inclusions of the second type appear to have cooled more rapidly than most iron meteorites.

In view of the confusion surrounding the use of the term Reichenbach lamella, it is suggested that the term be dropped from the literature.

","language":"English","publisher":"Elsevier","doi":"10.1016/S0016-7037(67)80027-9","issn":"00167037","usgsCitation":"Brett, R., and Henderson, E., 1967, The occurrence and origin of lamellar troilite in iron meteorites: Geochimica et Cosmochimica Acta, v. 31, no. 5, p. 721-730, https://doi.org/10.1016/S0016-7037(67)80027-9.","productDescription":"10 p.","startPage":"721","endPage":"730","costCenters":[],"links":[{"id":219644,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"31","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bae37e4b08c986b323f5c","contributors":{"authors":[{"text":"Brett, R.","contributorId":106632,"corporation":false,"usgs":true,"family":"Brett","given":"R.","email":"","affiliations":[],"preferred":false,"id":357120,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Henderson, E.P.","contributorId":100040,"corporation":false,"usgs":true,"family":"Henderson","given":"E.P.","email":"","affiliations":[],"preferred":false,"id":357119,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010040,"text":"70010040 - 1967 - Fractionation of rare-earth elements in allanite and monazite as related to geology of the Mt. Wheeler mine area, Nevada","interactions":[],"lastModifiedDate":"2024-03-07T16:17:24.475759","indexId":"70010040","displayToPublicDate":"1967-01-01T00:00:00","publicationYear":"1967","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":"Fractionation of rare-earth elements in allanite and monazite as related to geology of the Mt. Wheeler mine area, Nevada","docAbstract":"

Rare-earth contents of 20 allanites and 13 monazites, accessory minerals from a restricted outcrop area of intrusive granitic rocks, are reported. A quantity called sigma (Σ), which is the sum of the atomic percentages of La, Ce and Pr, is used as an index of composition with respect to the rare-earth elements. Values of sigma vary from 61.3 to 80.9 at.% for these allanites and monazites, representing an appreciable range of composition in terms of the rare-earth elements.

Degree of fractionation of rare earths varies directly with CaO content of the granitic rocks, which in turn depends largely on proximity of limestone. Four xenoliths included in the study suggest that spotty mosaic equilibria are superimposed on the regional gradients and that locally the degree of fractionation of rare earths responds to whole rock composition over distances of a few yards or less.

The chemistry of the granitic rocks under study appears to be similar in some respects to that of alkalio rocks and carbonatites. Allanites from the most calcium-rich rocks show a pronounced concentration of the most basic rare earths, and whole-rock concentrations of such rare constituents as total cerium earths, Zr, F, Ti, Ba and Sr increase sympathetically with whole-rock calcium.

The explanation for the concentration gradients observed in this chemical system must involve assimilation more than magmatic differentiation.

","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(67)90046-4","issn":"00167037","usgsCitation":"Lee, D.E., and Bastron, H., 1967, Fractionation of rare-earth elements in allanite and monazite as related to geology of the Mt. Wheeler mine area, Nevada: Geochimica et Cosmochimica Acta, v. 31, no. 3, p. 339-356, https://doi.org/10.1016/0016-7037(67)90046-4.","productDescription":"18 p.","startPage":"339","endPage":"356","numberOfPages":"18","costCenters":[],"links":[{"id":219737,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"31","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a13abe4b0c8380cd5472a","contributors":{"authors":[{"text":"Lee, D. E.","contributorId":96705,"corporation":false,"usgs":true,"family":"Lee","given":"D.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":357755,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bastron, H.","contributorId":20067,"corporation":false,"usgs":true,"family":"Bastron","given":"H.","affiliations":[],"preferred":false,"id":357754,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70171421,"text":"70171421 - 1967 - Yakima basalt of the Tieton River area, south-central Washington","interactions":[],"lastModifiedDate":"2016-05-31T11:42:27","indexId":"70171421","displayToPublicDate":"1967-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Yakima basalt of the Tieton River area, south-central Washington","docAbstract":"

Up to 1700 feet of the upper Miocene-lower Pliocene Yakima Basalt of the Columbia River Group underlie much of the eastern flank of the Cascade Range in the Tieton River area, Yakima County, Washington. Local prebasalt relief was more than 1700 feet, so thicknesses of each of the 15 exposed flows vary widely. Single flows can be traced for many miles, and terminate only against local topographic highs. The flows show typical colonnade-entablature jointing, and commonly overlie thin pillow-palagonite complexes.

\n

The basalts have Yakima-type chemistry. Plagioclase varies chiefly from An65(microphenocrysts) to An45 (microlites). Clinopyroxenes range from Ca-rich pigeonite to augite, with subcalcic augite most abundant. Complex continuous zoning with respect to optic angles occurs between all the clinopyroxene phases. Olivine is sparse, and phenocrysts of all minerals are rare.

\n

Plots of 40 modal analyses indicate that plagioclase and pyroxene began crystallizing at about the same time, and crystallized at the same rate until the flows were at least 75 per cent crystalline. Individual flows differ in their plagioclase/pyroxene ratios and, to a lesser degree, in other microscopic characteristics. Therefore they can be correlated between the measured sections. The stratigraphy thus defined indicates that the youngest flow in the area is slightly older than the Vantage Sandstone Member (about 13.5 m.y.), a prominent sedimentary interbed farther east on the Columbia River Plateau.

\n

Flow directions show that the basalts advanced into the area from the east and southeast. Sedimentary interbeds between some of the flows contain a heavy mineral suite indicative of a northern or northeastern provenance, and crossbedding measurements suggest westward and southwestward current directions. The regional paleoslope, therefore, sloped westward or southwestward; and the basalts probably extended somewhat beyond the present Cascade Crest before being dammed by the ancient Western Cascades. Floods of pyrogenic hornblende in the interbeds and overlapping K/A ages suggest sporadic explosive activity of Tatoosh-type plutons in the Cascades contemporaneous with Yakima extrusions.

\n

The basalts are warped into five nearly west-trending folds and an eastward-sloping homocline. The homocline is related directly to Cascade uplift, which may have begun at about the time that Yakima-type flows ceased flooding the area.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1967)78[1077:YBOTTR]2.0.CO;2","usgsCitation":"Swanson, D., 1967, Yakima basalt of the Tieton River area, south-central Washington: Geological Society of America Bulletin, v. 78, no. 9, p. 1077-1110, https://doi.org/10.1130/0016-7606(1967)78[1077:YBOTTR]2.0.CO;2.","productDescription":"34 p.","startPage":"1077","endPage":"1110","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true}],"links":[{"id":321909,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"78","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"574eb5dee4b0ee97d51a841c","contributors":{"authors":[{"text":"Swanson, Donald A. donswan@usgs.gov","contributorId":149804,"corporation":false,"usgs":true,"family":"Swanson","given":"Donald A.","email":"donswan@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":false,"id":630946,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2969,"text":"wsp1806 - 1966 - Ground-water resources and geology of northern and central Johnson County, Wyoming","interactions":[],"lastModifiedDate":"2012-02-02T00:05:41","indexId":"wsp1806","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1966","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1806","title":"Ground-water resources and geology of northern and central Johnson County, Wyoming","docAbstract":"Northern and central Johnson County, Wyo., is an area of about 2,600 square miles that lies principally in the western part of the Powder River structural basin but also includes the east flank of the Bighorn Mountains. Sedimentary rocks exposed range in age from Cambrian to Recent and have an average total thickness of about 16,000 feet. Igneous and metamorphic rocks of Precambrian age crop out in the Bighorn Mountains. Rocks of pre-Tertiary age, exposed on the flanks and in the foothills of the Bighorns, dip steeply eastward and lie at great depth in the Powder River basin. The rest of the project area is underlain by a thick sequence of interbedded sandstone, siltstone, and shale of Paleocene and Eocene age. Owing to the regional structure, most aquifers in Johnson County contain water under artesian pressure. \r\n\r\nThe Madison Limestone had not been tapped for water in Johnson County at the time of the present investigation (1963), but several wells in eastern Big Horn and Washakie Counties, on the west flank of the Bighorn Mountains, reportedly have flows ranging from 1,100 to 2,800 gallons per minute. Comparable yields can probably be obtained from the Madison in Johnson County in those areas where the limestone is fractured or cavernous. The Tensleep Sandstone reportedly yields 600 gallons per minute to a pumped irrigation well near its outcrop in the southwestern part of the project area. Several flowing wells tap the formation on the west flank of the Bighorn Mountains. The Madison Limestone and the Tensleep Sandstone have limited potential as sources of water because they can be developed economically only in a narrow band paralleling the Bighorn Mountain front in the southwestern part of the project area. \r\n\r\nOverlying the Tensleep Sandstone is about 6,000 feet of shale, siltstone, and fine-grained sandstone that, with a few exceptions, normally yields only small quantities of water to wells. The Cloverly Formation and the Newcastle Sandstone may yield moderate quantities of water to wells; but, in some areas, properly constructed wells tapping both formations might yield large quantities of water. The Shannon Sandstone Member of the Cody Shale will probably yield only small quantities of water to Wells, but it is the best potential source of ground water in the stratigraphic interval between the Newcastle and Parkman Sandstones. \r\n\r\nThe Parkman Sandstone and the Lance Formation yield water to relatively shallow wells principally in the southwestern part of the project area. The Fort Union Formation yields adequate supplies of water for stock and domestic use from relatively shallow wells near its outcrop almost everywhere in the county. A few deep wells tap the Fort Union along the Powder River valley in the northeastern part of Johnson County. Some of these wells flow, but their flows rarely exceed 10 gallons per minute; larger yields could be undoubtedly be obtained by pumping. \r\n\r\nThe Wasatch Formation is the principal source of ground water in Johnson County. It yields adequate supplies to many relatively shallow stock and domestic wells, some of which flow, but much larger yields probably would require pumping lifts that are prohibitive for most purposes. The Kingsbury Conglomerate and Moncrief Members of the Wasatch Formation, though, may yield moderate quantities of water in some places. \r\n\r\nAlluvial deposits underlying the valleys of the Powder River and Crazy Woman, Clear, and Piney Creeks are potential sources of moderate to large supplies of water in the Powder River drainage basin. The permeability of these deposits decreases with distance from the Bighorn Mountain front, so that largest yields can probably be obtained along the upper reaches of these streams. \r\n\r\nMost ground water utilized in the project area is for domestic and stock supplies and is obtained from drilled wells and from springs. Water for irrigation is obtained almost entirely by diverting flows of perennial streams. The discharge of wel","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1806","usgsCitation":"Whitcomb, H.A., Cummings, T.R., and McCullough, R.A., 1966, Ground-water resources and geology of northern and central Johnson County, Wyoming: U.S. Geological Survey Water Supply Paper 1806, v, 90 p. :illus., maps. ;24 cm., https://doi.org/10.3133/wsp1806.","productDescription":"v, 90 p. :illus., maps. ;24 cm.","costCenters":[],"links":[{"id":139273,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1806/report-thumb.jpg"},{"id":29704,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1806/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa7e4b07f02db666f87","contributors":{"authors":[{"text":"Whitcomb, Harold A.","contributorId":102868,"corporation":false,"usgs":true,"family":"Whitcomb","given":"Harold","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":146066,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cummings, T. Ray","contributorId":20722,"corporation":false,"usgs":true,"family":"Cummings","given":"T.","email":"","middleInitial":"Ray","affiliations":[],"preferred":false,"id":146064,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McCullough, Richard A.","contributorId":78712,"corporation":false,"usgs":true,"family":"McCullough","given":"Richard","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":146065,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70206437,"text":"70206437 - 1966 - Dawsonite in the green river formation of Colorado","interactions":[],"lastModifiedDate":"2019-11-04T07:53:24","indexId":"70206437","displayToPublicDate":"1966-09-01T07:37:07","publicationYear":"1966","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"displayTitle":"Dawsonite in the green river formation of Colorado","title":"Dawsonite in the green river formation of Colorado","docAbstract":"

Dawsonite NaAl(OH)2C03 is a rare mineral that occurs in relative abundance over hundreds of square miles in the Piceance Creek Basin of northwestern Colorado, as a rock-forming constituent of the oil shales in the green River Formation. In some specimens it makes up 25 percent by weight of the shale. Containing 35 percent of acid-soluble A1203, it has been viewed as a potential ore of aluminum. The dawsonite extends through 700 feet of continuous section of high-grade oil shale (averaging 25 gallons per ton), which may be as much as 1,500 feet in thickness. Its distribution, areally and stratigraphically, is reviewed; methods for its identification, and for its quantitative determination in the oil shale, with special reference to X-ray diffraction procedures are described; and the geochemistry of dawsonite, as it relates to the origin of the mineral, is considered. The scattered literature on dawsonite is briefly summarized. © 1966 Society of Economic Geologists, Inc..

","language":"English ","publisher":"Elsevier","doi":"10.2113/gsecongeo.61.6.1029","issn":" 03610128","usgsCitation":"Smith, J., and Milton, C., 1966, Dawsonite in the green river formation of Colorado: Economic Geology, v. 61, no. 6, p. 1029-1042, https://doi.org/10.2113/gsecongeo.61.6.1029.","productDescription":"14 p. ","startPage":"1029","endPage":"1042","costCenters":[],"links":[{"id":368915,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States ","state":"Colorado ","otherGeospatial":"Piceance Creek Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.96240234375,\n 39.33429742980725\n ],\n [\n -106.3037109375,\n 39.33429742980725\n ],\n [\n -106.3037109375,\n 40.94671366508002\n ],\n [\n -108.96240234375,\n 40.94671366508002\n ],\n [\n -108.96240234375,\n 39.33429742980725\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"61","issue":"6","noUsgsAuthors":false,"publicationDate":"1966-09-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Smith, J.W.","contributorId":205527,"corporation":false,"usgs":false,"family":"Smith","given":"J.W.","email":"","affiliations":[{"id":6682,"text":"Utah State University","active":true,"usgs":false}],"preferred":false,"id":774538,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Milton, C.","contributorId":37472,"corporation":false,"usgs":true,"family":"Milton","given":"C.","affiliations":[],"preferred":false,"id":774539,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70207930,"text":"70207930 - 1966 - Gravity slide origin of rift zones of some Hawaiian volcanoes","interactions":[],"lastModifiedDate":"2020-01-20T13:36:19","indexId":"70207930","displayToPublicDate":"1966-01-20T13:32:59","publicationYear":"1966","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1093,"text":"Bulletin Volcanologique","active":true,"publicationSubtype":{"id":10}},"title":"Gravity slide origin of rift zones of some Hawaiian volcanoes","docAbstract":"

The east-trending east rift zone of Kilauea volcano on the island of Hawaii is 50 km long and up to 3 km wide. It consists of three elements arranged roughly in three belts from north to south: 1) eruptive fissures, cracks, faults, and narrow grabens, 2) cinder cones (produced by eruptions more localised than the fissure eruptions), and 3) pit craters. Eruptive vents, either fissure or cone, do not occur south of pit craters; vents occur on the floor of some pit craters but are conlined to the north half. Most earthquakes near the rift zone are shallow; they are abundant south of the rift zone but rare north of it.

Precise levelling over a 6-year period shows elevation changes of up to 1 metre. Profiles of elevation change across the rift zone are asymmetrically steep on the north side. Precise triangulation shows that points south of the rift have been moving southward at right angles to the rift zone at rates of as much as 10 cm per year. During the major earthquake of 1868, the south coast of the island subsided as much as 2 metres, and abundant evidence indicates other recent subsidence of the south coast.

The above facts suggest that the rift zone dips south and that it bounds a large segment of the volcano which is sliding down the steep southern flank. Tensional cracks at the head of this slide tap the shallow central reservoir of the volcano at a depth of a few kilometres. The resulting dikes may feed eruptive fissures in the tensional zone at the head (northernmost part) of the slide, or they may pierce the hanging wall of the south-dipping rift zone through more confined conduits and feed the cinder cones. Likewise, shallow collapse into the rift zone on the north produces narrow grabens, whereas deeper collapse farther south (perhaps aided by magma stoping upward) produces circular pit craters.

Submarine topography south of Kilauea caldera indicates a submarine landslide on the south slope of the volcano. The landslide tongue is more than 25 kilometres long and is bounded upslope by a concave escarpment. On land, the northern rim of this escarpment is formed by a series of faults down-dropped on the south, called the Hilina fault system. Dredge hauls from a 300-metre hill on the crest of the landslide tongue at a water depth of 800 metres consists of angular fragments of fresh, glassy, tholeiitic basalt. The high vesicularity of this basalt suggests that it was erupted at a water depth several hundred metres less than that at which it was collected. Presumably, landsliding has carried the lava downward into deeper water.

","language":"English","publisher":"Springer Nature","doi":"10.1007/BF02597189","usgsCitation":"Moore, J.G., 1966, Gravity slide origin of rift zones of some Hawaiian volcanoes: Bulletin Volcanologique, v. 29, p. 719-720, https://doi.org/10.1007/BF02597189.","productDescription":"2 p.","startPage":"719","endPage":"720","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":371382,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"29","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Moore, James G. 0000-0002-7543-2401 jmoore@usgs.gov","orcid":"https://orcid.org/0000-0002-7543-2401","contributorId":2892,"corporation":false,"usgs":true,"family":"Moore","given":"James","email":"jmoore@usgs.gov","middleInitial":"G.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true},{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"preferred":true,"id":779797,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70274624,"text":"70274624 - 1966 - Hawaiian Volcano Observatory record book 1960, 1965, and 1966","interactions":[],"lastModifiedDate":"2026-04-17T14:49:53.55122","indexId":"70274624","displayToPublicDate":"1966-01-01T10:46:48","publicationYear":"1966","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":3,"text":"Organization Series"},"title":"Hawaiian Volcano Observatory record book 1960, 1965, and 1966","docAbstract":"

The Hawaiian Volcano Observatory (HVO) record books are annual journals in which field observations of eruptive activity at Kīlauea and Mauna Loa volcanoes, on the Island of Hawaiʻi, were compiled by HVO staff for most years from 1912 through early 1966. In addition to descriptive observations, the record books also contain hundreds of annotated photographs and sketches, as well as temperature and transit measurements. When photographs are included, the camera settings and film types used are noted. The field notes, sketches, and photographs used to compile the record books provide an unparalleled record of eruptive activity and were the basis for published newspaper reports and periodic bulletins, such as the Hawaiian Volcano Observatory bulletins and The volcano letter.  

HVO staff also painstakingly prepared a second copy of each early record book, virtually identical to the original, complete with photographs and sketches. The original version of the record book was kept at HVO, while the duplicate went to the Hawaiian Volcano Research Association, which was created by a group of Honolulu, Hawaiʻi, businessmen to promote HVO’s work. The Hawaiian Volcano Research Association, which dissolved decades ago, held the duplicate books in Honolulu, where they were more readily accessible to the public. After 1923, HVO stopped duplicating the books—at least, no duplicate records for subsequent years have been found. During the decade of the 1940s, preparation of the record books stopped altogether. In 1952, compilation of the record books resumed and continued, with long gaps, until early 1966. Entries in these later volumes are sparse, and these books are little more than photo albums of the episodic eruptions of Kīlauea. 

The original record books were held at HVO and, later, at Hawai‘i Volcanoes National Park. In 1972, the original record books for the years 1912 through 1939 were transferred to the Bishop Museum, in Honolulu, for safekeeping. These record books are now stored in archival boxes at that institution (accession number 172.265). The duplicate set of record books held by the Hawaiian Volcano Research Association were bound into volumes at an unknown date and turned over to the U.S. Geological Survey. This set of record books, spanning 1912 through 1923, is now housed in the rare book room of the U.S. Geological Survey Library in Reston, Virginia (catalog number 220(950) H3d). The record books for 1952 through early 1966 remain in storage at HVO. After 1955, typed annotations were no longer placed in the record books, and only photographs, most with captions, were included. Although the volumes titled “Record Book” end with the 1955 volume, the photograph albums that followed are similar, and the record book designation is retained for simplicity. Note that the photographs in these albums were not all originally arranged in chronological order. 

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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW"} ,{"id":70010041,"text":"70010041 - 1966 - Chemical composition of phosphorites of the Phosphoria Formation","interactions":[],"lastModifiedDate":"2020-11-24T01:26:01.930585","indexId":"70010041","displayToPublicDate":"1966-01-01T00:00:00","publicationYear":"1966","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":"Chemical composition of phosphorites of the Phosphoria Formation","docAbstract":"

The chemical composition, both major and minor constituents, of 60 samples of phosphorite from the Phosphoria Formation was determined. Major constituents of the average phosphorite are, by weight per cent: SiO2, 11·9; Al2O3, 1·7; Fe2O3,1·1; MgO, 0·3; CaO, 44·0; Na2O, 0·6; K2O, 0·5; total H2O, 2·2; H2O−, 0·6; TiO2, 0·1; P2O5, 30·5; CO2, 2·2; SO3, 1·8; F, 3·1; organic matter, 2·1; and oil, 0·2. Uranium averages 0·009 per cent.

The phosphate mineral is basically apatite, Ca5(PO4)3F, with small but significant and variable substitutions—Na, Sr, U and Th for Ca, and CO3 and SO4 for PO4.

Rare metals not associated with apatite are associated principally with the organic-matter component of the rocks. This group includes As, Ag, Cd, Cr, Cu, Mo, Ni, Sb, Se, V and Zn. Chromium is the most abundant, having a modal abundance of 0·1 per cent and a maximum concentration of 0·3 per cent.

The average phosphorite is composed of approximately 80 per cent apatite, 10 per cent quartz, 5 per cent muscovite-illite, 2 per cent organic matter, 1 per cent dolomite—calcite, 1 per cent iron oxide, and 1 per cent other components. It is texturally a medium-grained pellet phosphorite.

","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(66)90131-1","issn":"00167037","usgsCitation":"Gulbrandsen, R.A., 1966, Chemical composition of phosphorites of the Phosphoria Formation: Geochimica et Cosmochimica Acta, v. 30, no. 8, p. 769-778, https://doi.org/10.1016/0016-7037(66)90131-1.","productDescription":"10 p.","startPage":"769","endPage":"778","numberOfPages":"10","costCenters":[],"links":[{"id":218620,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"30","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f566e4b0c8380cd4c1e8","contributors":{"authors":[{"text":"Gulbrandsen, R. A.","contributorId":48543,"corporation":false,"usgs":true,"family":"Gulbrandsen","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":357756,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":12440,"text":"ofr663 - 1966 - Rare earths in phosphorites: Geochemistry and potential recovery","interactions":[],"lastModifiedDate":"2022-09-02T15:18:08.158692","indexId":"ofr663","displayToPublicDate":"1966-01-01T00:00:00","publicationYear":"1966","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":"66-3","title":"Rare earths in phosphorites: Geochemistry and potential recovery","docAbstract":"

Rare earths are but trace constituents of marine apatite. However, as millions of tones of such apatite are dissolved annually to make phosphoric acid, an opportunity exists for greatly increasing RE output as by-product of fertilizer production. New, complete, quantitative analysis of RE in representative apatite concentrates reveal that the potential for by-product RE equals current production. The RE assemblage in marine apatite is unusual, showing depletion in cerium and relative enrichment in the heavier lanthonons, a favorable distribution for RE technology and utilization.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr663","usgsCitation":"Altschuler, Z., Berman, S., and Cuttitta, F., 1966, Rare earths in phosphorites: Geochemistry and potential recovery: U.S. Geological Survey Open-File Report 66-3, 31 p., https://doi.org/10.3133/ofr663.","productDescription":"31 p.","costCenters":[],"links":[{"id":406144,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1966/0003/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":143733,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1966/0003/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db649291","contributors":{"authors":[{"text":"Altschuler, Z. S.","contributorId":42962,"corporation":false,"usgs":true,"family":"Altschuler","given":"Z. S.","affiliations":[],"preferred":false,"id":166143,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Berman, Sol","contributorId":32532,"corporation":false,"usgs":true,"family":"Berman","given":"Sol","email":"","affiliations":[],"preferred":false,"id":166142,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cuttitta, Frank","contributorId":20731,"corporation":false,"usgs":true,"family":"Cuttitta","given":"Frank","email":"","affiliations":[],"preferred":false,"id":166141,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1000079,"text":"1000079 - 1966 - Life history of the gizzard shad, Dorosoma cepedianum (Le Sueur), in western Lake Erie","interactions":[],"lastModifiedDate":"2012-03-02T17:16:05","indexId":"1000079","displayToPublicDate":"1966-01-01T00:00:00","publicationYear":"1966","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1663,"text":"Fishery Bulletin","printIssn":"0090-0656","active":true,"publicationSubtype":{"id":10}},"title":"Life history of the gizzard shad, Dorosoma cepedianum (Le Sueur), in western Lake Erie","docAbstract":"The rapid increase in the stocks of gizzard shad in Lake Erie since 1950 unquestionably had an important effect on the ecology of the lake. The present study, based on almost 24,000 fish collected by various means in 1952-55 in or near the island area of western Lake Erie was undertaken to provide information on the role of shad in the bionomics of the region.\r\nThe annulus of the gizzard shad scale is a valid year-mark. It is laid down in May-July, a little later in the older than in the younger fish. The body-scale relation is linear with an intercept of 22.1 mm. on the axis of standard length. Age-groups 0, I, and II were abundantly represented in the samples. Age-group III was much less well represented, and older fish were extremely scarce. The oldest shad seen belonged to the VI-group.\r\nThe seasonal growth was most rapid in July-August and growth was much reduced or nil in January-April. Males attained the following average standard lengths (in millimeters) at the end of the indicated years of life: 1-141; 2-273; 3-313; 4-343; 5-349. For females these values were 1-140; 2-285; 3-335; 4-364; 5-386.\r\nThe weight of the gizzard shad increased as the 3.07053 power of the length. The length-weight relation varied seasonally, annually, and, near the spawning season, according to sex and state of gonads.\r\nOnly a few precocious male and female gizzard shad attain sexual maturity as age-group I. Almost all males and a good percentage of females mature at age II and only rarely are III-group shad immature. Development of the egg and seasonal changes of the ovary are described. Egg production is highest in the II group-average of 378,900 per individual and 689 per gram of body weight. Spawning takes place from early June into July and is most intensive near mid-June. Heaviest spawning is at water temperatures of 67A?F. or more. Early development to the attainment of the adult shape is described; particular attention is given to the development of the alimentary tract.\r\nThe anatomy of the digestive tract in the adult is described, and comments are offered on the function of such organs as the pharyngeal pouches and the caeca. Tests were made for digestive enzymes in different parts of the tract. The gizzard shad is a filter feeder. Food varies widely with season and locality but consists mostly of phytoplankton and zooplankton.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Fishery Bulletin","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"U.S. Fish and Wildlife Service","collaboration":"Out-of-print","usgsCitation":"Bodola, A., 1966, Life history of the gizzard shad, Dorosoma cepedianum (Le Sueur), in western Lake Erie: Fishery Bulletin, v. 65, no. 2, p. 391-425.","productDescription":"p. 391-425","startPage":"391","endPage":"425","numberOfPages":"34","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":133029,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"65","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b16e4b07f02db6a53f8","contributors":{"authors":[{"text":"Bodola, Anthony","contributorId":86732,"corporation":false,"usgs":true,"family":"Bodola","given":"Anthony","email":"","affiliations":[],"preferred":false,"id":308045,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15761,"text":"ofr65142 - 1965 - Geology and ore deposits of the central York Mountains, western Seward Peninsula, Alaska","interactions":[{"subject":{"id":15761,"text":"ofr65142 - 1965 - Geology and ore deposits of the central York Mountains, western Seward Peninsula, Alaska","indexId":"ofr65142","publicationYear":"1965","noYear":false,"title":"Geology and ore deposits of the central York Mountains, western Seward Peninsula, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":35708,"text":"b1287 - 1969 - Geology and ore deposits of the Central York Mountains, western Seward Peninsula, Alaska","indexId":"b1287","publicationYear":"1969","noYear":false,"title":"Geology and ore deposits of the Central York Mountains, western Seward Peninsula, Alaska"},"id":1}],"supersededBy":{"id":35708,"text":"b1287 - 1969 - Geology and ore deposits of the Central York Mountains, western Seward Peninsula, Alaska","indexId":"b1287","publicationYear":"1969","noYear":false,"title":"Geology and ore deposits of the Central York Mountains, western Seward Peninsula, Alaska"},"lastModifiedDate":"2024-05-20T19:22:29.519521","indexId":"ofr65142","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"65-142","title":"Geology and ore deposits of the central York Mountains, western Seward Peninsula, Alaska","docAbstract":"

In the central York Mountains, carbonate rocks of Lower and Middle Ordovician age and aggregating at least 8,000 feet thick are thrust northward over slate and argillaceous limestone of pre-Ordovician age which were intruded by gabbro in pre-Ordovician time. Normal faults of four distinct systems cut the thrust plates, and in Late Cretaceous time, stocks of biotite granite, abnormally rich in beryllium, tin, boron and certain other trace elements, pierced the thrust plates. In part following the intrusion of the granites, a strong set of normal faults developed striking N. 60°-85° E. through the central York Mountains and locally these faults cut the granites. Dikes of granite, rhyolite porphyry, and lamprophyre were injected into some of these faults, the lamprophyres being younger. Trace elements in the lamprophyres prove they are mafic rocks probably derived from the lama, and that they cannot be related genetically to granite. Shortly after the intrusion of lamprophyre dikes, ore deposits of tin, beryllium, and fluorite were formed from solutions probably derived from deeply-buried hot granite where the granite was ruptured by normal faults. Ore shoots were localized beneath thrust faults where the faults are intruded by dikes, and a major ore-bearing structure, the Rapid River fault, is mineralized for half its length for a distance of eight miles. The tin deposits contain cassiterite and stannite in topaz greisen with abundant sulfides of copper, lead, zinc, and iron, as well as wolframite. The beryllium deposits contain fluorite, chrysoberyl, diaspore, muscovite, and tourmaline, with trace to small amounts of euclase, bertrandite, helvite, phenikite(?), todorokite and hematite. Beryl occurs sparingly in late veins of quartz and fluorite. Chrysoberyl is the earliest and commonest beryllium mineral, followed by euclase and bertrandite, and then phenakite(?) and beryl. Helvite is restricted to banded skarns near granite, and which consist of magnetite and fluorite. Throughout the district, a strong zonation is displayed from tin deposits in greisen through transitional veins of sulfide minerals with fluorite and chrysoberyl to fluorite-beryllium deposits and thence to barren veins of silica and fluorite with trace amounts of beryllium. This zonal arrangement of deposits probably will be found elsewhere in the world where greisen tin deposits occur in carbonate rocks. The geochemical cycle of the trace elements Be, Sn, W, B, Li, Cu, Pb, Zn and Nb shows that these elements were enriched in the biotite granites and were strongly fractionated among the minerals of granites. Fran the granites, these rare elements moved outward into contact rocks and ore deposits. During the supergene cycle, clear geochemical anomalies were formed in stream sediments, soils and plants near ore deposits, and geochemical prospecting led to the discovery of the beryllium lodes. With the possible exception of zinc and niobium, the rare elements that are associated in the rocks and ores remain associated in the supergene processes. Fixation of zinc in clay soil and tundra plants may account for the relatively small amount of zinc in strew sediments.

Datable Pleistocene events in the York Mountains begin with the Yarmouth Interglaciation when the York Terrace, a wide marine platform, was cut. In Illinoian time, the York Terrace was uplifted almost 400 feet, and during the Sangamon Interglaciation a second marine platform (Lost River Terrace) was cut and is not deformed. During Wisconsin time the widespread York Glaciation was followed by the more restricted Mint River Glaciation. Because uplift of the York Terrace extended into the Bering Strait, it is probable that prior to the uplift in Illinoian time the Bering Strait was a seaway and a barrier to land migration rather than a land bridge.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr65142","usgsCitation":"Sainsbury, C., 1965, Geology and ore deposits of the central York Mountains, western Seward Peninsula, Alaska: U.S. Geological Survey Open-File Report 65-142, Report: 149 p.; 15 Plates: 20.55 x 27.89 inches or smaller; 8 Tables: 20.88 x 30.29 inches or smaller, https://doi.org/10.3133/ofr65142.","productDescription":"Report: 149 p.; 15 Plates: 20.55 x 27.89 inches or smaller; 8 Tables: 20.88 x 30.29 inches or smaller","costCenters":[],"links":[{"id":428957,"rank":25,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-10A.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428956,"rank":24,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-10B.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428955,"rank":23,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-10C.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428954,"rank":22,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-2-1-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428953,"rank":21,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-2-1-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428952,"rank":20,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-22.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428951,"rank":19,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-28.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428950,"rank":18,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-29.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428949,"rank":17,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-36-1-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428948,"rank":16,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-36-1-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428947,"rank":15,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-36-1-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428946,"rank":14,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-37.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428945,"rank":13,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-38.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428944,"rank":12,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-39-1-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428943,"rank":11,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-39-1-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428942,"rank":10,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1965/0142/figure-40.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428941,"rank":9,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1965/0142/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428940,"rank":8,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1965/0142/Table-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428939,"rank":7,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1965/0142/Table-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428938,"rank":6,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1965/0142/Table-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428937,"rank":5,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1965/0142/Table-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428936,"rank":4,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1965/0142/Table-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428935,"rank":3,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1965/0142/Table-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":428934,"rank":2,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/of/1965/0142/Table-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":148935,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1965/0142/report-thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"central York Mountains, western Seward Peninsula","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -167.56430004060184,\n 65.60933402498489\n ],\n [\n -167.56430004060184,\n 65.36714034542257\n ],\n [\n -166.82167890236178,\n 65.36714034542257\n ],\n [\n -166.82167890236178,\n 65.60933402498489\n ],\n [\n -167.56430004060184,\n 65.60933402498489\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad7e4b07f02db6843c4","contributors":{"authors":[{"text":"Sainsbury, C.L.","contributorId":99968,"corporation":false,"usgs":true,"family":"Sainsbury","given":"C.L.","email":"","affiliations":[],"preferred":false,"id":171659,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2875,"text":"wsp1809C - 1965 - Ground-water in the upper Star Valley, Wyoming","interactions":[{"subject":{"id":52369,"text":"ofr63129 - 1963 - Ground water in the upper Star Valley, Wyoming","indexId":"ofr63129","publicationYear":"1963","noYear":false,"title":"Ground water in the upper Star Valley, Wyoming"},"predicate":"SUPERSEDED_BY","object":{"id":2875,"text":"wsp1809C - 1965 - Ground-water in the upper Star Valley, Wyoming","indexId":"wsp1809C","publicationYear":"1965","noYear":false,"chapter":"C","title":"Ground-water in the upper Star Valley, Wyoming"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:35","indexId":"wsp1809C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1809","chapter":"C","title":"Ground-water in the upper Star Valley, Wyoming","docAbstract":"The upper Star Valley covers about 55 square miles of lowland in the westernmost part of Wyoming. The altitude of the floor of the valley is 6,000-6,700 feet. The climate is cool; the growing season, short. Annual precipitation averages about 18 inches, and total precipitation in July and August averages 2.2 inches. Additional supplies of water are needed for irrigation of pasture and hay. The principal water-bearing formation is a thick body of gravel of Pleistocene age. Consolidated to semiconsolidated sedimentary formations of Paleozoic to Tertiary age form the surrounding mountains and underlie the gravel. These bedrock formations yield small amounts of water to wells on the margins of the valley. \r\n\r\nMost of the recharge to the gravel aquifer is received at the heads of alluvial fans by infiltration from tributaries that drain the surrounding mountains. Snow upon the valley floor provides a significant amount of recharge. Water moves toward the Salt River, which flows northward through the valley and which has large gains due to ground-water inflow. \r\n\r\nOn the east side of the valley, the water table is 100-200 feet below land surface at a distance of half a mile from the mountain front. On the west side of the valley, the depth to water is rarely more than 30 feet. Depth to water decreases toward the center of the valley. \r\n\r\nThe gravel aquifer can provide sufficient water for supplemental irrigation. Irrigation supplies of several hundreds of gallons per minute have been developed at two localities on the west side of the valley. Two pumping tests showed values for transmissibility of 82,500 and 370,000 gallons per day per foot in the vicinity of a well on the east side of the valley and a well on the west side, respectively. \r\n\r\nThe ground water is of good quality for irrigation usage through most of the valley. Hardness of the water exceeds 200 parts per million, however, and this characteristic makes the water somewhat undesirable for domestic and industrial use. Water beneath the northwestern part of the valley has relatively high content of sodium and chloride.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1809C","usgsCitation":"Walker, E.H., 1965, Ground-water in the upper Star Valley, Wyoming: U.S. Geological Survey Water Supply Paper 1809, iv, 27 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1809C.","productDescription":"iv, 27 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138978,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809c/report-thumb.jpg"},{"id":29503,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29504,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809c/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa9e4b07f02db66826e","contributors":{"authors":[{"text":"Walker, Eugene H.","contributorId":24761,"corporation":false,"usgs":true,"family":"Walker","given":"Eugene","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":145943,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221206,"text":"70221206 - 1965 - Chemical characteristics of oceanic basalts and the upper mantle","interactions":[],"lastModifiedDate":"2021-06-04T21:52:17.917781","indexId":"70221206","displayToPublicDate":"1965-07-01T16:49:24","publicationYear":"1965","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Chemical characteristics of oceanic basalts and the upper mantle","docAbstract":"

Tholeiitic basalts (oceanic tholeiites) that form most of the deeply submerged volcanic features in the oceans are characterized by extremely low amounts of Ba, K, P, Pb, Sr, Th, U, and Zr as well as Fe2O3/FeO < 0.2 and Na/K > 10 in unaltered samples. Oceanic tholeiites also have rare earth abundance-distribution patterns and ratios of K/Rb (1300) and Sr87/Sr86 (0.702) similar to or overlapping those of calcium-rich (basaltic) achondritic meteorites. The close compositional similarities between the oceanic tholeiites and calcium-rich achondrites indicates the relatively primitive nature of the oceanic tholeiites. In contrast, the alkali-rich basalts that cap submarine and island volcanoes are relatively enriched in Ba, K, La, Nb, P, Pb, Pb206, Rb, Fe2O3, Sr, Sr87, Ti, Th, U, and Zr; i.e. in the same elements and isotopes that are concentrated in the sialic continental crusts by factors of 5 to 1000 more than the amounts readily inferred in the upper mantle. These analytical data coupled with the field relationships indicate that the alkali-rich basalts are derivative rocks, fractionated from the oceanic tholeiites by processes of magmatic differentiation, and that the oceanic tholeiites are the principal or only primary magma generated in the upper mantle under the oceans. Studies of the abundances and compositions of continental basalts show that essentially identical tholeiitic lavas, contaminated with Si, K, and the chemically coherent trace elements and radiogenic isotopes from the sial, also have been the predominant or only magma generated in the mantle under the continents. The chemical properties of oceanic tholeiites suggest that the upper mantle probably contains less than (in parts per million): Ba, 10; K, 1000; Pb, 0.4; Rb, 10; Th, 0.2; and U, 0.1. The Sr87/Sr86 must be less than 0.7015; Th/U about 2; K/Rb about 1500-2000; and Fe2O3/FeO less than 0.1. The integration of field and petrochemical data with seismic, density, and shock-wave studies suggests that the oceanic tholeiites are either complete melts of the upper mantle or are generated from a mix of this tholeiite and a magnesium-rich peridotite or dunite in proportions up to perhaps 1:4. The Mohorovičić discontinuity under the oceans appears to mark the transition downward from a largely tholeiitic oceanic crust to either tholeiite reconstituted to blueschist or greenschist or to the ultramafic residue left after expulsion of oceanic tholeiite.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1965)76[719:CCOOBA]2.0.CO;2","usgsCitation":"Engel, A., Engel, C.G., and Havens, R., 1965, Chemical characteristics of oceanic basalts and the upper mantle: Geological Society of America Bulletin, v. 76, no. 7, p. 719-734, https://doi.org/10.1130/0016-7606(1965)76[719:CCOOBA]2.0.CO;2.","productDescription":"16 p.","startPage":"719","endPage":"734","costCenters":[],"links":[{"id":386251,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"76","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Engel, A.E.J.","contributorId":241621,"corporation":false,"usgs":false,"family":"Engel","given":"A.E.J.","affiliations":[],"preferred":false,"id":817046,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Engel, Celeste G.","contributorId":23386,"corporation":false,"usgs":true,"family":"Engel","given":"Celeste","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":817047,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Havens, R.G.","contributorId":65889,"corporation":false,"usgs":true,"family":"Havens","given":"R.G.","email":"","affiliations":[],"preferred":false,"id":817048,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70274627,"text":"70274627 - 1965 - Hawaiian Volcano Observatory record book 1965","interactions":[],"lastModifiedDate":"2026-04-17T15:09:15.405904","indexId":"70274627","displayToPublicDate":"1965-01-01T11:05:42","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":3,"text":"Organization Series"},"title":"Hawaiian Volcano Observatory record book 1965","docAbstract":"

The Hawaiian Volcano Observatory (HVO) record books are annual journals in which field observations of eruptive activity at Kīlauea and Mauna Loa volcanoes, on the Island of Hawaiʻi, were compiled by HVO staff for most years from 1912 through early 1966. In addition to descriptive observations, the record books also contain hundreds of annotated photographs and sketches, as well as temperature and transit measurements. When photographs are included, the camera settings and film types used are noted. The field notes, sketches, and photographs used to compile the record books provide an unparalleled record of eruptive activity and were the basis for published newspaper reports and periodic bulletins, such as the Hawaiian Volcano Observatory bulletins and The volcano letter.  

HVO staff also painstakingly prepared a second copy of each early record book, virtually identical to the original, complete with photographs and sketches. The original version of the record book was kept at HVO, while the duplicate went to the Hawaiian Volcano Research Association, which was created by a group of Honolulu, Hawaiʻi, businessmen to promote HVO’s work. The Hawaiian Volcano Research Association, which dissolved decades ago, held the duplicate books in Honolulu, where they were more readily accessible to the public. After 1923, HVO stopped duplicating the books—at least, no duplicate records for subsequent years have been found. During the decade of the 1940s, preparation of the record books stopped altogether. In 1952, compilation of the record books resumed and continued, with long gaps, until early 1966. Entries in these later volumes are sparse, and these books are little more than photo albums of the episodic eruptions of Kīlauea. 

The original record books were held at HVO and, later, at Hawai‘i Volcanoes National Park. In 1972, the original record books for the years 1912 through 1939 were transferred to the Bishop Museum, in Honolulu, for safekeeping. These record books are now stored in archival boxes at that institution (accession number 172.265). The duplicate set of record books held by the Hawaiian Volcano Research Association were bound into volumes at an unknown date and turned over to the U.S. Geological Survey. This set of record books, spanning 1912 through 1923, is now housed in the rare book room of the U.S. Geological Survey Library in Reston, Virginia (catalog number 220(950) H3d). The record books for 1952 through early 1966 remain in storage at HVO. After 1955, typed annotations were no longer placed in the record books, and only photographs, most with captions, were included. Although the volumes titled “Record Book” end with the 1955 volume, the photograph albums that followed are similar, and the record book designation is retained for simplicity. Note that the photographs in these albums were not all originally arranged in chronological order. 

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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW"} ,{"id":70274626,"text":"70274626 - 1965 - Hawaiian Volcano Observatory record book 1963, 1964, and 1965","interactions":[],"lastModifiedDate":"2026-04-17T15:01:00.826486","indexId":"70274626","displayToPublicDate":"1965-01-01T10:58:20","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":3,"text":"Organization Series"},"title":"Hawaiian Volcano Observatory record book 1963, 1964, and 1965","docAbstract":"

The Hawaiian Volcano Observatory (HVO) record books are annual journals in which field observations of eruptive activity at Kīlauea and Mauna Loa volcanoes, on the Island of Hawaiʻi, were compiled by HVO staff for most years from 1912 through early 1966. In addition to descriptive observations, the record books also contain hundreds of annotated photographs and sketches, as well as temperature and transit measurements. When photographs are included, the camera settings and film types used are noted. The field notes, sketches, and photographs used to compile the record books provide an unparalleled record of eruptive activity and were the basis for published newspaper reports and periodic bulletins, such as the Hawaiian Volcano Observatory bulletins and The volcano letter.  

HVO staff also painstakingly prepared a second copy of each early record book, virtually identical to the original, complete with photographs and sketches. The original version of the record book was kept at HVO, while the duplicate went to the Hawaiian Volcano Research Association, which was created by a group of Honolulu, Hawaiʻi, businessmen to promote HVO’s work. The Hawaiian Volcano Research Association, which dissolved decades ago, held the duplicate books in Honolulu, where they were more readily accessible to the public. After 1923, HVO stopped duplicating the books—at least, no duplicate records for subsequent years have been found. During the decade of the 1940s, preparation of the record books stopped altogether. In 1952, compilation of the record books resumed and continued, with long gaps, until early 1966. Entries in these later volumes are sparse, and these books are little more than photo albums of the episodic eruptions of Kīlauea. 

The original record books were held at HVO and, later, at Hawai‘i Volcanoes National Park. In 1972, the original record books for the years 1912 through 1939 were transferred to the Bishop Museum, in Honolulu, for safekeeping. These record books are now stored in archival boxes at that institution (accession number 172.265). The duplicate set of record books held by the Hawaiian Volcano Research Association were bound into volumes at an unknown date and turned over to the U.S. Geological Survey. This set of record books, spanning 1912 through 1923, is now housed in the rare book room of the U.S. Geological Survey Library in Reston, Virginia (catalog number 220(950) H3d). The record books for 1952 through early 1966 remain in storage at HVO. After 1955, typed annotations were no longer placed in the record books, and only photographs, most with captions, were included. Although the volumes titled “Record Book” end with the 1955 volume, the photograph albums that followed are similar, and the record book designation is retained for simplicity. Note that the photographs in these albums were not all originally arranged in chronological order. 

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