Fresh ground water (200 parts per million total dissolved solids and upwards) occurs in portions of Pleistocene sandstone aquifers beneath basins and wadis in north Kuwait where the mean rainfall is about five inches per year. The fresh water is surrounded and underlain by brackish water (> 4000 ppm TDS). Drilling and testing show that fresh water saturation is restricted to wadis and basin areas; in Rawdatain basin it attains a maximum thickness of about 110 feet and a lateral extent of about seven miles.
The fresh ground water represents recharge localized, during infrequent, torrential rain storms, in areas of concentrated runoff where sediments in the vadose zone are moderately permeable and depth to the water table is generally less than a hundred feet. Concentration of runoff appears to be the primary control in the localization of recharge. The fresh water percolates downward to the ground-water reservoir following rare storms, then flows in the direction of hydraulic gradient and gradually becomes brackish.
Theoretical delineation of the recharge area and ground-water flow pattern in Rawdatain was confirmed by tritium and C14 dating of the water.
Brackish ground-water conditions prevail from water table downward in areas where rainfall infiltrates essentially where it falls, permeability of sediments in the vadose zone is low, or the water table is several hundred feet below land surface. In these areas, rainfall is retained and lost within the soil zone or becomes mineralized during deep percolation.
","language":"English","publisher":"Elsevier","doi":"10.1016/0022-1694(65)90038-7","issn":"00221694","usgsCitation":"Bergstrom, R., and Aten, R., 1965, Natural recharge and localization of fresh ground water in Kuwait: Journal of Hydrology, v. 2, no. 3, p. 213-231, https://doi.org/10.1016/0022-1694(65)90038-7.","productDescription":"19 p.","startPage":"213","endPage":"231","numberOfPages":"19","costCenters":[],"links":[{"id":219390,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Kuwait","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[47.97452,29.97582],[48.18319,29.53448],[48.09394,29.3063],[48.41609,28.552],[47.70885,28.52606],[47.45982,29.00252],[46.56871,29.09903],[47.30262,30.05907],[47.97452,29.97582]]]},\"properties\":{\"name\":\"Kuwait\"}}]}","volume":"2","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a6351e4b0c8380cd7241c","contributors":{"authors":[{"text":"Bergstrom, R.E.","contributorId":66413,"corporation":false,"usgs":true,"family":"Bergstrom","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":359369,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Aten, R.E.","contributorId":18105,"corporation":false,"usgs":true,"family":"Aten","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":359368,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1853,"text":"wsp1750B - 1964 - Summary of floods in the United States during 1959","interactions":[],"lastModifiedDate":"2017-09-06T17:51:01","indexId":"wsp1750B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"1750","chapter":"B","title":"Summary of floods in the United States during 1959","docAbstract":"This report describes the most outstanding floods that occurred in the United States during 1959.
The floods of January-February in Ohio and adjacent States were the most outstanding floods of the year 1959 with respect to area affected, number of streams having maximum discharge of record, rare occurrence of peaks, and great amount of damage caused.
Floods in the Rock River basin in southern Wisconsin and northern Illinois during late March and early April produced maximum stages and discharges on many streams. The Rock River at Watertown, Wisc., was the highest in 40 years and Lake Mendota at Madison, Wisc., reached its maximum stage since 1916. Many towns were flooded and thousands of persons were forced from their homes.
What is possibly the greatest 24-hour rainfall ever to be noted in Iowa fell August 5-6. The resulting floods inundated an 80-block area in Fort Madison, Iowa, and caused damage estimated at $600,000 in the city. A total of 130,000 acres of land was inundated.
Major floods occurred in Texas in the upper Trinity, middle Brazos, middle Colorado, upper Guadalupe, and upper Nueces River basins in early October, following heavy general rains that covered most of Texas. The peak stage on North Bosque River near Clifton was the highest known since 1887. More than \\$1 million in damage was reported for Houston.
In addition to the 4 floods mentioned above, 22 others of lesser magnitude are considered important enough to report in this annual summary.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1750B","usgsCitation":"Hendricks, E.L., 1964, Summary of floods in the United States during 1959: U.S. Geological Survey Water Supply Paper 1750, vi, 101 p., https://doi.org/10.3133/wsp1750B.","productDescription":"vi, 101 p.","numberOfPages":"101","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":27072,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1750b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138488,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1750b/report-thumb.jpg"}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b04e4b07f02db69927b","contributors":{"authors":[{"text":"Hendricks, E. L.","contributorId":50126,"corporation":false,"usgs":true,"family":"Hendricks","given":"E.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":144252,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":6428,"text":"pp483H - 1964 - Giant Upper Cretaceous oysters from the Gulf coast and Caribbean","interactions":[],"lastModifiedDate":"2014-08-05T13:28:30","indexId":"pp483H","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"483","chapter":"H","title":"Giant Upper Cretaceous oysters from the Gulf coast and Caribbean","docAbstract":"Two unusually massive ostreid species, representing the largest and youngest Mesozoic members of their respective lineages, occur in Upper Cretaceous sediment of the gulf coast and Caribbean areas. Their characteristics and significance, as well as the morphologic terminology of ostreids in general, are discussed.
\nCrassostrea cusseta Sohl and Kauffman n. sp. is the largest known ostreid from Mesozoic rocks of North America; it occurs sporadically in the Cusseta Sand and rarely in the Blufftown Formation of the Chattahoochee River region in Georgia and Alabama. It is especially notable in that it lacks a detectable posterior adductor muscle scar on large adult shells. C. cusseta is the terminal Cretaceous member of the C. soleniscus lineage in gulf coast sediments; the lineage continues, however, with little basic modification, throughout the Cenozoic, being represented in the Eocene by C. gigantissima (Finch) and probably, in modern times, by C. virginica (Gmelin). The C. soleniscus lineage is the first typically modern crassostreid group recognized in the Mesozoic.
\nArctostrea aguilerae (Böse) occurs in Late Campanian and Early Maestrichtian sediments of Alabama, Mississippi, Texas(?), Mexico, and Cuba. The mature shell of this species is larger and more massive than that of any other known arctostreid. Arctostrea is well represented throughout the Upper Jurassic and Cretaceous of Europe, but in North America, despite the great numbers and diversity of Cretaceous oysters, only A. aguilerae and the Albian form A. carinata are known. The presence of A. aquilerae in both the Caribbean and gulf coast faunas is exceptional, as the Late Cretaceous faunas of these provinces are generally distinct and originated in different faunal realms.
","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/pp483H","usgsCitation":"Sohl, N.F., and Kauffman, E.G., 1964, Giant Upper Cretaceous oysters from the Gulf coast and Caribbean: U.S. Geological Survey Professional Paper 483, p. H1-H22, https://doi.org/10.3133/pp483H.","productDescription":"p. H1-H22","numberOfPages":"39","costCenters":[],"links":[{"id":117932,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0483h/report-thumb.jpg"},{"id":33838,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0483h/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac5e4b07f02db679f3f","contributors":{"authors":[{"text":"Sohl, Norman F.","contributorId":27906,"corporation":false,"usgs":true,"family":"Sohl","given":"Norman","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":152706,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kauffman, Erle G.","contributorId":107756,"corporation":false,"usgs":true,"family":"Kauffman","given":"Erle","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":152707,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":245,"text":"wsp1660B - 1964 - Summary of floods in the United States during 1958","interactions":[],"lastModifiedDate":"2017-09-06T17:48:22","indexId":"wsp1660B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"1660","chapter":"B","title":"Summary of floods in the United States during 1958","docAbstract":"This report describes the most outstanding floods that occurred in the United States during 1958.
A series of storms from January 23 to February 16 brought large amounts of precipitation to northern California and produced damaging floods, particularly in the Lower Sacramento Valley where losses totaled about \\$12 million.
Major floods, notable because of the large area affected, occurred on many small streams in central and south Texas, following heavy general rains in late February. Extensive flooding occurred along the Gulf Coastal plain on the lower reaches of the major streams from the Brazos River to the Nueces River. Two lives were lost, and property damage exceeded \\$1 million.
Damaging floods of April 1-7 followed one of the wettest winters in California history. Swollen streams overflowed their banks throughout the central part of the State, and discharge peaks on many streams exceeded those .of the floods of December 1955. Most severely flooded was the San Francisco Bay area. Total flood damage was estimated at \\$23 million.
The storms and floods of April-May in Louisiana and adjacent States outranked all other floods in the United States during 1958 with respect to intensity of rain over a large area, number of streams having maximum discharge of record, rare occurrence of peaks, and great amount (\\$21 million) of resultant damage.
Heavy rains on June 8-15 caused one of the greatest summer floods of record in central Indiana. Peak discharges were high and of rare occurrences. Failure of numerous levees along the Wabash River caused great damage. Crop damage alone was estimated at \\$48 million.
Intense rains of July 1-2 caused record-breaking floods in southwestern Iowa. Rapid rises and the great magnitude of the floods on small streams resulted in 18 deaths and many injuries. Six towns and cities along the East Nishnabotna River and its tributaries were particularly hard hit; rural damage was also high. Total damage was estimated at \\$15 million.
Heavy rains (as much as 40 inches during the last 2 weeks in September) from the middle of September to the middle of October caused destructive floods along the Rio Grande in Texas and Mexico. Many communities were isolated by the flood waters, and damage to crops was great.
In addition to the 7 floods mentioned above, 21 others of lesser magnitude are reported in this annual summary.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1660B","collaboration":"Prepared in cooperation with Federal, State, and local agencies","usgsCitation":"Hendricks, E.L., 1964, Summary of floods in the United States during 1958: U.S. Geological Survey Water Supply Paper 1660, vi, 97 p., https://doi.org/10.3133/wsp1660B.","productDescription":"vi, 97 p.","numberOfPages":"104","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":136589,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1660b/report-thumb.jpg"},{"id":24852,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1660b/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b04e4b07f02db6992a6","contributors":{"authors":[{"text":"Hendricks, E. L.","contributorId":50126,"corporation":false,"usgs":true,"family":"Hendricks","given":"E.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":142137,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221905,"text":"70221905 - 1964 - Veins of hypogene manganese oxide minerals in the southwestern United States","interactions":[],"lastModifiedDate":"2021-07-14T12:54:13.95994","indexId":"70221905","displayToPublicDate":"1964-07-14T07:43:40","publicationYear":"1964","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":"Veins of hypogene manganese oxide minerals in the southwestern United States","docAbstract":"Characteristic minerals are psilomelane, hollandite, cryptomelane, and coronadite, more rarely ramsdellite and pyrolusite. Host rocks are Mn-deficient; 80 percent of examples are middle to late Tertiary layered volcanics. Though deposits are shallow, mostly mined to only 100-200 feet (maximum 500 feet), a hypogene origin is indicated by their persistent association with barite and fluorite, a peripheral position in the zonal pattern of some metal-mining districts, alteration of plagioclase to K-spar, and abundance of W, Pb, Cu, Mo, Ti, As, Sb. They represent the subzone of Mn-bearing epithermal vein deposits lying nearest the surface, succeeded in depth by four other subzones: barite, fluorite, gold-silver, and base metals.
A well drilled for geothermal power near Salton Sea in Imperial Valley, Calif., is 5,232 feet deep; it is the deepest well in the world (1962) in a high-temperature hot spring area. In the lower half of the hole temperatures are too high to measure with available equipment, but are at loast 270°C, and may be as much as 370°C. For comparison, maximum temperature heretofore reported at depth (1962) for hot spring areas is 295°C.
The well taps a very saline brine of Na-Ca-K-Cl type (about 185,000 ppm Cl) with exceptionally high potassium, and with the highest content of minor alkali elements known for natural waters; Fe, Mn, Zn, Pb, Cu, Ag, and some other metals are also exceptionally high. This brine may be connate, but present evidence favors a source in the magma chamber at depth that supplied late Quaternary rhyolite domes of the area. If the latter is correct, the brine is an undiluted magmatic water that is residual from the separation of a more volatile phase high in CO2, H2S, and with some alkali halides. Elsewhere, the hypothesized volatile phase may account for near-surface hot spring activity of most thermal areas of volcanic association. The residual brine of high salinity may ordinarily remain relatively deep in the volcanic systems because of high specific gravity and low content of volatiles, seldom appearing at the surface except in a greatly diluted form.
The hot springs of Arima, Japan, may be a rare example of this type of magmatic water discharging at the surface in moderate concentration (Cl as much as 42,000 ppm). Independent evidence from fluid inclusions in minerals of high-temperature base-metal deposits also favors the existence of magmatic water high in Na, Ca, and Cl, and low in CO2 and other volatile components.
During a three-month production test several tons of material precipitated in the horizontal discharge pipe from the well. Amorphous silica with iron and manganese, and bornite are the dominant recognized components. This material contains the astonishingly high contents of about 20 percent copper, 2 percent silver, and notable sulfur, arsenic, bismuth, lead, antimony, and some other minor elements. Total quantities of all elements in the original whole brine are not yet known, but calculated amounts corresponding to 1 to 3 ppm of copper and 0.1 to 0.3 ppm of silver were precipitated from the brine to form the pipe deposits. The brine, therefore, may be man’s first sample of an « active » ore solution.
Equally fascinating to many geologists is the possibility that in the lower part of the hole temperatures are so high and pressures are sufficient for young sedimentary rocks to be undergoing transformation into rocks with mineral assemblages of the greenschist facies of metamorphism. Drill cores from 4,400 to 5,000 feet in depth contain chlorite, albite, K-feldspar, epidote, mica, and quartz, with some indication of increase in metamorphic grade downward. Regional geological and geophysical studies favor a depth of about 20,000 feet to pre-Tertiary basement rocks in the general area. A shallow basement or local upfaulting of old metamorphic rocks are not likely possibilities for the thermal area.
","language":"English","publisher":"Springer","doi":"10.1007/BF02597534","usgsCitation":"White, D.E., 1964, Deep geothermal brine near Salton Sea, California: Bulletin Volcanologique, v. 27, p. 369-370, https://doi.org/10.1007/BF02597534.","productDescription":"2 p.","startPage":"369","endPage":"370","costCenters":[],"links":[{"id":387170,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Salton Sea","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -116.16668701171875,\n 33.07082934859187\n ],\n [\n -115.55145263671876,\n 33.07082934859187\n ],\n [\n -115.55145263671876,\n 33.58259116393916\n ],\n [\n -116.16668701171875,\n 33.58259116393916\n ],\n [\n -116.16668701171875,\n 33.07082934859187\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"27","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"White, Donald E.","contributorId":76787,"corporation":false,"usgs":true,"family":"White","given":"Donald","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":819271,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2353,"text":"wsp1600 - 1964 - Geology and ground-water conditions of Clark County, Washington, with a description of a major alluvial aquifer along the Columbia River","interactions":[],"lastModifiedDate":"2023-03-23T21:07:44.77317","indexId":"wsp1600","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","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":"1600","title":"Geology and ground-water conditions of Clark County, Washington, with a description of a major alluvial aquifer along the Columbia River","docAbstract":"This report presents the results of an investigation of the ground-water resources of the populated parts of Clark County. Yields adequate for irrigation can be obtained from wells inmost farmed areas in Clark County, Wash. The total available supply is sufficient for all foreseeable irrigation developments. In a few local areas aquifers are fine-grained, and yields of individual wells are low. An enormous ground-water supply is available from a major alluvial aquifer underlying the flood plain of the Columbia River in the vicinity of Vancouver, Camas, and Washougal, where the aquifer is recharged, in part, by infiltration from the river. Yields of individual wells are large, ranging to as much as 4,000 gpm (gallons per minute). Clark County lies along the western flank of the Cascade Range. in the structural lowland (Willamette-Puget trough) between those mountains and the Coast Ranges to the west. The area covered by the report includes the urban, the suburban, and most of the agricultural lands in the county. These lands lie on a Series of nearly fiat plains and benches which rise steplike from the level of the Columbia River (a few feet above sea level) to about 800 feet above sea level. Clark County is-drained by the Columbia River (the trunk stream of the Pacific Northwest) and its tributaries. The Columbia River forms the southern and western boundaries of the county. Although the climate of the county is considered to be humid, the precipitation ranging from about 37 to more than 110 inches annually in various parts of the county, the unequal seasonal distribution (about 1.5 inches total for ;July and August in the agricultural area) makes irrigation highly desirable for most .crops and essential for some specialized crops. Consolidated rocks of Eocene to Miocene age, chiefly volcanic lava flows and pyroclastics but including some sedimentary strata, crop out in the foothills of the Cascades in the eastern part of the county and underlie the younger, unconsolidated rocks in the lowlands to the west At most places small to moderate quantities of water can be obtained from fractures in the older consolidated rocks. However, in the populated parts of the county, these rocks generally are overlain by considerable thicknesses of more permeable materials, and few wells have been drilled in them. Springs and dug wells yield an ample domestic supply at a number of outlying farms in the foothills. The younger (Pliocene to Recent) unconsolidated materials were deposited chiefly by streams in the basin formed by downwarping of the older rocks. However, some lake deposits and glacial drift also are included. The oldest unit of this group, the lower member of the Troutdale formation of Pliocene age, consists chiefly of clay, silt, and fine sand but includes lenses of coarser sand and, rarely, gravel. The maximum known thickness of the lower member of the Troutdale formation is about 660 feet. This unit is not a good aquifer because most of the strata are fine grained. However, at a few places drilled wells have penetrated lenses of coarser grained materials in these deposits and have obtained small to moderate amounts of water from them. The upper member of the Troutdale formation consists almost entirely of lightly to moderately cemented gravel, of which the most striking feature is the presence of a considerable percentage of quartzite pebbles. The average thickness of the upper member of the Troutdale may originally have been 300 to 400 feet. The member crops out over considerable areas in the county and, where conditions of topography and exposure are optimum, has beer very deeply weathered. It is suggested that the upper member of the Troutdale formation may prove to be of early Pleistocene age.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1600","usgsCitation":"Mundorff, M.J., 1964, Geology and ground-water conditions of Clark County, Washington, with a description of a major alluvial aquifer along the Columbia River: U.S. Geological Survey Water Supply Paper 1600, Report: vi, 268 p.; 3 Plates: 35.00 x 50.19 inches or smaller, https://doi.org/10.3133/wsp1600.","productDescription":"Report: vi, 268 p.; 3 Plates: 35.00 x 50.19 inches or smaller","costCenters":[],"links":[{"id":28281,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1600/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28280,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1600/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28279,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1600/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":414663,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24789.htm","linkFileType":{"id":5,"text":"html"}},{"id":28282,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1600/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137781,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1600/report-thumb.jpg"}],"country":"United States","state":"Washington","county":"Clark County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"MultiPolygon\",\"coordinates\":[[[[-122.2446,46.0551],[-122.2433,45.9563],[-122.2443,45.867],[-122.2482,45.8665],[-122.2479,45.7819],[-122.2476,45.7677],[-122.2471,45.7238],[-122.2468,45.6643],[-122.2464,45.6008],[-122.2463,45.5967],[-122.2464,45.5761],[-122.246,45.561],[-122.259,45.5604],[-122.2668,45.5598],[-122.2701,45.5598],[-122.2786,45.561],[-122.2903,45.5627],[-122.3072,45.5616],[-122.3157,45.5628],[-122.3164,45.5628],[-122.3261,45.5631],[-122.3374,45.5703],[-122.3434,45.5748],[-122.348,45.5766],[-122.3506,45.5774],[-122.3546,45.5797],[-122.3592,45.5805],[-122.367,45.5822],[-122.3794,45.5825],[-122.3878,45.582],[-122.3937,45.581],[-122.3963,45.5809],[-122.3963,45.5823],[-122.3931,45.5833],[-122.3918,45.5842],[-122.3912,45.5865],[-122.3945,45.5869],[-122.3964,45.586],[-122.399,45.5845],[-122.4062,45.5858],[-122.4249,45.5819],[-122.4353,45.5799],[-122.4386,45.5799],[-122.4503,45.582],[-122.4575,45.5828],[-122.466,45.5845],[-122.4811,45.5866],[-122.4876,45.5869],[-122.4967,45.5886],[-122.5111,45.5916],[-122.5177,45.5933],[-122.5217,45.5947],[-122.5269,45.5955],[-122.5321,45.5968],[-122.5486,45.602],[-122.5656,45.6041],[-122.5827,45.6093],[-122.5951,45.6109],[-122.6181,45.6174],[-122.6245,45.616],[-122.6251,45.6137],[-122.6322,45.6122],[-122.6414,45.6125],[-122.6459,45.6129],[-122.6538,45.615],[-122.6663,45.6194],[-122.6829,45.6269],[-122.6935,45.6322],[-122.6981,45.6358],[-122.7041,45.6394],[-122.7147,45.6451],[-122.7259,45.6477],[-122.7384,45.6512],[-122.745,45.6533],[-122.7517,45.6587],[-122.7531,45.6614],[-122.7545,45.6637],[-122.7591,45.6673],[-122.7618,45.67],[-122.764,45.6759],[-122.7654,45.6795],[-122.7682,45.6836],[-122.7684,45.6891],[-122.763,45.7056],[-122.7626,45.7102],[-122.7608,45.7148],[-122.7603,45.7208],[-122.758,45.73],[-122.7571,45.7423],[-122.7567,45.7492],[-122.7582,45.7547],[-122.7584,45.7602],[-122.7587,45.7688],[-122.7608,45.7743],[-122.7636,45.7788],[-122.7671,45.7856],[-122.7732,45.7919],[-122.7733,45.7965],[-122.778,45.7992],[-122.7807,45.8032],[-122.7841,45.8064],[-122.7848,45.8087],[-122.7876,45.8118],[-122.7883,45.815],[-122.7858,45.8187],[-122.7859,45.8215],[-122.7873,45.8237],[-122.7868,45.8274],[-122.7863,45.832],[-122.7838,45.8362],[-122.782,45.8412],[-122.7821,45.8426],[-122.7828,45.8449],[-122.7797,45.849],[-122.7791,45.8504],[-122.7786,45.8541],[-122.7767,45.8573],[-122.7703,45.8615],[-122.7599,45.864],[-122.7522,45.8655],[-122.7413,45.8735],[-122.7347,45.8722],[-122.7216,45.8697],[-122.7183,45.8706],[-122.7204,45.8747],[-122.7284,45.8796],[-122.7346,45.8878],[-122.7329,45.896],[-122.7427,45.8959],[-122.7453,45.8949],[-122.748,45.8972],[-122.7501,45.9003],[-122.7482,45.9031],[-122.7404,45.9046],[-122.7386,45.9087],[-122.7381,45.9152],[-122.7382,45.9179],[-122.7349,45.918],[-122.7284,45.9185],[-122.7246,45.9204],[-122.7201,45.9251],[-122.7203,45.9296],[-122.7217,45.9333],[-122.7166,45.9352],[-122.7133,45.9343],[-122.7067,45.9326],[-122.7049,45.9327],[-122.6942,45.9381],[-122.6856,45.9392],[-122.6853,45.9398],[-122.6677,45.941],[-122.667,45.9397],[-122.6656,45.9374],[-122.6615,45.9333],[-122.6594,45.9288],[-122.6536,45.9303],[-122.6504,45.9344],[-122.6467,45.9395],[-122.6421,45.9391],[-122.6329,45.9393],[-122.6224,45.9385],[-122.6192,45.9386],[-122.6152,45.9382],[-122.6133,45.9387],[-122.6081,45.9411],[-122.5927,45.95],[-122.5804,45.9561],[-122.5699,45.9549],[-122.5601,45.9555],[-122.5512,45.9625],[-122.5455,45.9686],[-122.5378,45.9732],[-122.5341,45.9815],[-122.5263,45.9849],[-122.51,45.9865],[-122.5059,45.9815],[-122.4975,45.9835],[-122.4957,45.989],[-122.4786,45.9883],[-122.4596,45.9868],[-122.4471,45.9851],[-122.4377,45.9756],[-122.4253,45.9772],[-122.4009,45.9739],[-122.3884,45.9699],[-122.3758,45.9641],[-122.3633,45.9638],[-122.3613,45.9598],[-122.3547,45.9603],[-122.3449,45.96],[-122.3345,45.9638],[-122.3288,45.9689],[-122.3243,45.9731],[-122.3239,45.9818],[-122.3194,45.9841],[-122.3144,45.992],[-122.3231,46.0001],[-122.3253,46.0092],[-122.3261,46.0124],[-122.3157,46.0158],[-122.3139,46.0227],[-122.3101,46.0287],[-122.3024,46.0356],[-122.2947,46.0412],[-122.2924,46.0504],[-122.2762,46.0589],[-122.2671,46.0603],[-122.2565,46.0587],[-122.2446,46.0551]]],[[[-122.3248,45.5604],[-122.3221,45.5595],[-122.3189,45.5596],[-122.3163,45.5596],[-122.313,45.5592],[-122.3091,45.5583],[-122.3039,45.558],[-122.2987,45.5576],[-122.2941,45.5576],[-122.2902,45.5581],[-122.2883,45.5577],[-122.283,45.5564],[-122.2791,45.556],[-122.2784,45.5555],[-122.2791,45.5546],[-122.283,45.5537],[-122.2849,45.5532],[-122.2901,45.5531],[-122.2973,45.5535],[-122.3038,45.5534],[-122.3103,45.5538],[-122.3161,45.5546],[-122.322,45.5559],[-122.3273,45.5576],[-122.3299,45.559],[-122.33,45.5608],[-122.328,45.5613],[-122.3248,45.5604]]],[[[-122.4104,45.5743],[-122.4215,45.5742],[-122.4312,45.5745],[-122.4352,45.5754],[-122.4385,45.5776],[-122.4359,45.5781],[-122.432,45.5781],[-122.4268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Maurice John","contributorId":41404,"corporation":false,"usgs":true,"family":"Mundorff","given":"Maurice","email":"","middleInitial":"John","affiliations":[],"preferred":false,"id":145066,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2511,"text":"wsp1768 - 1964 - Hydrology of the Babylon-Islip area, Suffolk County, Long Island, New York","interactions":[],"lastModifiedDate":"2023-03-14T20:23:08.28216","indexId":"wsp1768","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","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":"1768","title":"Hydrology of the Babylon-Islip area, Suffolk County, Long Island, New York","docAbstract":"The report area comprises 270 square miles, and includes most of the Towns of Babylon and Islip, and parts of the Towns of Huntington, Smithtown, and Brookhaven, in southwestern Suffolk County, New York. \r\n\r\nAlmost all the water used in the area is obtained from wells screened in permeable zones of the ground-water reservoir which consists of unconsolidated deposits of gravel, sand, silt, and clay as much as 1,800 feet thick. The ground-water reservoir contains three principal aquifers. From the surface down these are (a) surficial deposits of sand and gravel of Pleistocene age, (b) sands of the Magothy (?) Formation of Cretaceous age, and (c) the Lloyd Sand Member of the Raritan Formation of Cretaceous age. At present only the upper two aquifers are tapped by wells. Natural replenishment of the ground-water reservoir in the area takes place entirely by infiltration of precipitation and averages about 215 mgd (million gallons per day). Average ground-water runoff to streams above tidewater is 114 mgd, and it is estimated that an additional 54 mgd is discharged into tidal reaches of streams. Ground-water evapotranspiration is computed to be about 10 mgd and submarine outflow from the area is estimated to be 18 mgd. The average streamflow of the area above tidewater is 120 mgd. Because of the permeable soils and low relief, direct runoff is only about 5 percent of the average streamflow. Streams are perennial along their middle and lower reaches and exhibit well-sustained low flows. Flooding rarely occurs although continued urbanization may result in minor flooding problems as additional storm sewers are constructed. \r\n\r\nWater in most of the area is generally of good quality; however, it may be contaminated locally. Some streams and parts of the water-table aquifer contain low concentrations of synthetic detergents and other dissolved constituents from domestic and industrial wastes. Salty water occurs in parts of the water-table aquifer in the area under and bordering Great South Bay and under the barrier beaches. Present information, however, indicates that submarine outflow in the artesian aquifers is sufficient to maintain the fresh water-salt water interface some distance seaward of the barrier beaches. \r\n\r\nGround-water withdrawals in 1960 averaged 39 mgd, most of which was returned to the ground through cesspools, leaching beds, and recharge wells; pumpage did not appreciably affect the natural water balance of the groundwater reservoir. If withdrawals continue to be artificially recharged, pumpage can be increased at least fivefold before consumptive losses materially reduce ground-water levels. However, if the area were completely sewered in the future, an adequate supply of ground water for a substantially increased population could not be obtained without (a) reducing the amount of ground water in storage in the reservoir or (b) recharging treated-sewage effluent.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1768","usgsCitation":"Pluhowski, E.J., and Kantrowitz, I.H., 1964, Hydrology of the Babylon-Islip area, Suffolk County, Long Island, New York: U.S. Geological Survey Water Supply Paper 1768, Report: v, 119 p.; 8 Plates: 30.00 x 32.00 inches or smaller, https://doi.org/10.3133/wsp1768.","productDescription":"Report: v, 119 p.; 8 Plates: 30.00 x 32.00 inches or smaller","costCenters":[],"links":[{"id":28672,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1768/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28671,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1768/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28670,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1768/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28669,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1768/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28668,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1768/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28667,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1768/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28666,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1768/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28665,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1768/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28664,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1768/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138711,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1768/report-thumb.jpg"},{"id":414130,"rank":11,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24946.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"New York","county":"Suffolk County","otherGeospatial":"Babylon-Islip area, Long Island","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -73.479,\n 40.883\n ],\n [\n -73.479,\n 40.604\n ],\n [\n -73,\n 40.604\n ],\n [\n -73,\n 40.883\n ],\n [\n -73.479,\n 40.883\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a13e4b07f02db601ef4","contributors":{"authors":[{"text":"Pluhowski, Edward J.","contributorId":87911,"corporation":false,"usgs":true,"family":"Pluhowski","given":"Edward","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":145316,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kantrowitz, Irwin H.","contributorId":93472,"corporation":false,"usgs":true,"family":"Kantrowitz","given":"Irwin","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":145317,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2233,"text":"wsp1779C - 1964 - Chemical quality of surface water in the West Branch Susquehanna River basin, Pennsylvania","interactions":[],"lastModifiedDate":"2023-03-22T18:45:31.751873","indexId":"wsp1779C","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","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":"1779","chapter":"C","title":"Chemical quality of surface water in the West Branch Susquehanna River basin, Pennsylvania","docAbstract":"The West Branch Susquehanna River is 228 miles long and drains 6,913 square miles of mountainous area in central Pennsylvania. Much of this area is forestcovered wilderness, part of which is reserved as State game land. Wild animals, such as deer, bear, turkey and grouse, are sheltered there, and many streams contain trout and other game fish. This helps to make the region one of the best hunting and fishing areas in Pennsylvania. The Congress has approved Federal funds for the construction of several reservoirs to prevent flooding of the main river and several of its tributaries. Water stored behind the dams will not be withdrawn below a minimum level designated as conservation pools. These pools will be available for recreation. Several headwater streams, such as Clearfield, Moshannon, and at times Sinnemahoning Creek, that carry drainage from coal mines are acid and contain high concentrations of dissolved solids, especially sulfates. These streams acidify the West Branch Susquehanna River downstream as far as Jersey Shore. One of the most influential tributaries affecting the quality of the West Branch Susquehanna River after they merge is Bald Eagle Creek. Bald Eagle Creek enters the main river downstream from Lock Haven which is approximately 100 river miles from the river's source. Because of its alkaline properties, water of Bald Eagle Creek can neutralize acidic water. Many streams draining small areas and several draining large areas such as Pine Creek, Lycoming Creek, and Loyalsock Creek are clear nearly neutral water low in dissolved solids whose pH is about 7.0 most of the time. These streams have a diluting and neutralizing effect on the quality of the West Branch Susquehanna River, so that from Williamsport downstream the river water is rarely acid, and for most of the time it is of good chemical quality.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1779C","usgsCitation":"McCarren, E.F., 1964, Chemical quality of surface water in the West Branch Susquehanna River basin, Pennsylvania: U.S. Geological Survey Water Supply Paper 1779, Report; iv, 40 p.; 1 Plate: 21.00 x 16.62 inches, https://doi.org/10.3133/wsp1779C.","productDescription":"Report; iv, 40 p.; 1 Plate: 21.00 x 16.62 inches","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":27992,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1779c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":414560,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24956.htm","linkFileType":{"id":5,"text":"html"}},{"id":27991,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137748,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1779c/report-thumb.jpg"}],"country":"United States","state":"Pennsylvania","otherGeospatial":"Susquehanna River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -78.667,\n 41.75\n ],\n [\n -78.667,\n 40.583\n ],\n [\n -76.25,\n 40.583\n ],\n [\n -76.25,\n 41.75\n ],\n [\n -78.667,\n 41.75\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dfe4b07f02db5e3b11","contributors":{"authors":[{"text":"McCarren, Edward F.","contributorId":106472,"corporation":false,"usgs":true,"family":"McCarren","given":"Edward","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":144863,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1000315,"text":"1000315 - 1964 - Age and growth of the round whitefish in Lake Michigan","interactions":[],"lastModifiedDate":"2013-02-04T11:32:48","indexId":"1000315","displayToPublicDate":"1964-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3624,"text":"Transactions of the American Fisheries Society","active":true,"publicationSubtype":{"id":10}},"title":"Age and growth of the round whitefish in Lake Michigan","docAbstract":"The round whitefish, though rarely abundant, is widely distributed in northern waters. It is one of the least studied of the coregonines; the present report is but the second for Great Lakes waters. Commercial production in Lake Michigan has been tightly confined to the northern portion. The period 1924-30 showed the best production: 200,000 to 359,000 pounds. Since 1956, production has been around 10,000 pounds or less. The present age and growth study is based on 208 fish collected by gill net in December 1951. The relation between total length in inches (L) and the weight in ounces (W) is described by the equation log W = -2.7232 + 3.2940 log L. Age-group III made up 66.3 percent, and age-group IV, 20.6 percent of the sample; age-groups V, VI, and VII combined contributed only 5.9 percent. The average length for all fish in the sample was 14.5 inches. Growth was calculated from a previously published linear body-scale relation with an intercept of 1.1 inches on the axis of fish length. The increments of calculated length declined steadily from a maximum of 4.6 inches the first year to 1.0 inch the eighth. A 3-year-old Lake Michigan fish (12.3 inches) is as long as a 5-year-old Lake Superior fish, and an 8-year-old Lake Michigan fish (18.9 inches) is 0.9 inch longer than the oldest (12 years) from Lake Superior. The smallest mature males and females were in the length intervals 12.0-12.4 inches and 13.0-13.4 inches, respectively. All males over 1.4 inches and all females over 14.9 inches were mature. The youngest mature males were in age-group II; 36 percent of II-group males but none of the females were mature. All fish older than age-group III were mature.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Transactions of the American Fisheries Society","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Taylor & Francis","publisherLocation":"London, UK","doi":"10.1577/1548-8659(1964)93[46:AAGOTR]2.0.CO;2","collaboration":"Out-of-print","usgsCitation":"Mraz, D., 1964, Age and growth of the round whitefish in Lake Michigan: Transactions of the American Fisheries Society, v. 93, no. 1, p. 46-52, https://doi.org/10.1577/1548-8659(1964)93[46:AAGOTR]2.0.CO;2.","productDescription":"7 p.","startPage":"46","endPage":"52","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":266922,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1577/1548-8659(1964)93[46:AAGOTR]2.0.CO;2"},{"id":132989,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"93","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae4e4b07f02db689b6b","contributors":{"authors":[{"text":"Mraz, Donald","contributorId":21502,"corporation":false,"usgs":true,"family":"Mraz","given":"Donald","email":"","affiliations":[],"preferred":false,"id":308378,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":5220460,"text":"5220460 - 1963 - A survey of fungi associated with lesioned and chlorotic sago pondweed (Potamogeton pectinatus)","interactions":[],"lastModifiedDate":"2017-07-05T15:46:54","indexId":"5220460","displayToPublicDate":"2010-06-16T12:17:32","publicationYear":"1963","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3085,"text":"Plant Disease Reporter","active":true,"publicationSubtype":{"id":10}},"displayTitle":"A survey of fungi associated with lesioned and chlorotic sago pondweed (Potamogeton pectinatus)","title":"A survey of fungi associated with lesioned and chlorotic sago pondweed (Potamogeton pectinatus)","docAbstract":"Isolations from 1000 Potamogeton pectinatus plants collected from six major stands in Back Bay, Virginia and 13 in Currituck Sound, North Carolina yielded Pythium spp. consistently and in relatively high frequency. Although specific determination of these isolates was unsuccessful, they were separated into three groups according to morphological and cultural characteristics. Rhizoctonia solani Kuehn was isolated in rare instances. In inoculation studies, isolates of R. solani were pathogenic to P. pectinatus, whereas inoculations with Pythium spp. proved inconclusive, even though one group of isolates exhibited pathogenic tendencies.
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.
","language":"English","publisher":"Hawaiian Volcano Observatory","usgsCitation":"Hawaiian Volcano Observatory, 1963, Hawaiian Volcano Observatory record book 1963, 14 p.","productDescription":"14 p.","costCenters":[{"id":336,"text":"Hawaiian Volcano Observatory","active":false,"usgs":true}],"links":[{"id":503196,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70274625/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":503195,"rank":1,"type":{"id":22,"text":"Related Work"},"url":"https://pubs.usgs.gov/publication/70274518","text":"Hawaiian Volcano Observatory record books"},{"id":503197,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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- Geology of the Spruce Pine district, Avery, Mitchell, and Yancey Counties, North Carolina","interactions":[{"subject":{"id":14551,"text":"ofr53143 - 1953 - Geologic map of the Spruce Pine district, North Carolina","indexId":"ofr53143","publicationYear":"1953","noYear":false,"title":"Geologic map of the Spruce Pine district, North Carolina"},"predicate":"SUPERSEDED_BY","object":{"id":33809,"text":"b1122A - 1962 - Geology of the Spruce Pine district, Avery, Mitchell, and Yancey Counties, North Carolina","indexId":"b1122A","publicationYear":"1962","noYear":false,"chapter":"A","title":"Geology of the Spruce Pine district, Avery, Mitchell, and Yancey Counties, North Carolina"},"id":1}],"lastModifiedDate":"2021-10-21T11:52:04.898019","indexId":"b1122A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"1122","chapter":"A","title":"Geology of the Spruce Pine district, Avery, Mitchell, and Yancey Counties, North Carolina","docAbstract":"The Spruce Pine pegmatite district, a northeastward-trending belt 25 miles \r\nlong and 10 miles wide, lies in parts of Avery, Mitchell, and Yancey Counties in the Blue Ridge Province of western North Carolina. The most abundant \r\nrocks in the district are interlayered mica and amphibole gneisses and schists, all of which are believed to be of Precambrian age. These rocks are cut by small bodies of dunite and associated rocks of Precambrian (?) age, large bodies of alaskite and associated pegmatite of early Paleozoic age, and basaltic and diabasic dikes and sills of Triassic (?) age. The rocks of the district have been weathered to saprolite that is locally 50 feet thick.\r\n\r\nThe major structure in the area is a southwestward-plunging asymmetrical \r\nsynclinorium that has its steeper limb on the northwest side.\r\n\r\nFeldspar, muscovite as sheet and scrap (ground) mica, and kaolin from the \r\nalaskite and associated pegmatite account for over 90 percent of the total \r\nmineral production of the district. Amounts of other pegmatite minerals, \r\nincluding quartz, beryl, columbite-tantalite, rare-earth and uranium minerals \r\nare an extremely small part of the mineral resources. Actual or potential \r\nproducts from other rocks are olivine, vermiculite, asbestos, talc, chromium and nickel, soapstone, mica schist, garnet, kyanite, dolomite marble, and construction materials.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to Economic Geology (1960)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b1122A","isbn":"0607643226","usgsCitation":"Brobst, D.A., 1962, Geology of the Spruce Pine district, Avery, Mitchell, and Yancey Counties, North Carolina: U.S. Geological Survey Bulletin 1122, Report: iv, 26 p.; 2 Plates 52 x 30 inches and 52 x 27 inches, https://doi.org/10.3133/b1122A.","productDescription":"Report: iv, 26 p.; 2 Plates 52 x 30 inches and 52 x 27 inches","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":61716,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1122a/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":61715,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1122a/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":61714,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1122a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":165925,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1122a/report-thumb.jpg"},{"id":109360,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20822.htm","linkFileType":{"id":5,"text":"html"},"description":"20822"}],"scale":"24000","country":"United States","state":"North Carolina","county":"Avery County, Mitchell County, Yancey County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -82.292,35.822 ], [ -82.292,36.078 ], [ -81.938,36.078 ], [ -81.938,35.822 ], [ -82.292,35.822 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e47e","contributors":{"authors":[{"text":"Brobst, Donald Albert","contributorId":36117,"corporation":false,"usgs":true,"family":"Brobst","given":"Donald","email":"","middleInitial":"Albert","affiliations":[],"preferred":false,"id":211971,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":61978,"text":"mr27 - 1962 - Magnesite and brucite in the United States, exclusive of Alaska and Hawaii","interactions":[{"subject":{"id":45985,"text":"ofr6156 - 1961 - Magnesite and brucite in the United States","indexId":"ofr6156","publicationYear":"1961","noYear":false,"title":"Magnesite and brucite in the United States"},"predicate":"SUPERSEDED_BY","object":{"id":61978,"text":"mr27 - 1962 - Magnesite and brucite in the United States, exclusive of Alaska and Hawaii","indexId":"mr27","publicationYear":"1962","noYear":false,"title":"Magnesite and brucite in the United States, exclusive of Alaska and Hawaii"},"id":1}],"lastModifiedDate":"2023-01-24T19:21:38.71232","indexId":"mr27","displayToPublicDate":"1962-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":324,"text":"Mineral Investigations Resource Map","code":"MR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"27","title":"Magnesite and brucite in the United States, exclusive of Alaska and Hawaii","docAbstract":"The important deposits of magnesite (MgCO3) and brucite (MgO.H2O) in the United States (exclusive of Alaska and Hawaii) are shown on the accompanying map. Single deposits and groups of deposits are shown by geometric symbols according to four size categories based on estimated production plus reserves. These categories are: less than 10,000 tons, 10,000 to 100,000 tons, 100,000 to 1,000,000 tons, and more than 1,000,000 tons. Occurrences of mineralogic interest only are not shown. All map locations are numbered consecutively in each State and keyed to the locality index. The geographical coordinates in the locality index represent the centers of the geometric symbols. Thus, the same coordinates are assigned to all deposits covered by a group symbol.
The map was compiled from published reports and data in the files of the United States Geological Survey. The names, geographic coordinates, and geologic types of deposits are given in the locality index. The principal published reports used in compiling the map are listed in the selected references.
The main types of commercial deposits of magnesite in the United States are: (1) replacement bodies in limestone and dolomite; (2) replacements and veins in serpentine; and (3) sedimentary beds. Other magnesite deposits of varied origin and less common occurrence include beds associated with talc, chlorite, and mica schists; and veins and lenses in altered tuffs.
Brucite is a relatively rare mineral of secondary origin which usually accompanies other magnesian minerals, particularly magnesite and hydromagnesite, and is associated with carbonate rocks and serpentine.
Magnesite was first mined in California in 1886, and the State was the only domestic producer until the development of the Washington deposits began in 1916. In recent years, the main production of magnesite has been from Stevens County, Washington, and Nye County, Nevada. Production in California has been intermittent since 1945. Magnesite deposits in Texas were mined during and immediately after World War II. At present (1961) the only brucite deposits being worked are those at Gabbs, Nye County, Nevada. They have been mined almost continuously since 1935.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mr27","usgsCitation":"Gildersleeve, B., 1962, Magnesite and brucite in the United States, exclusive of Alaska and Hawaii: U.S. Geological Survey Mineral Investigations Resource Map 27, Report: 4 p.; 1 Plate: 63.55 x 40.06 inches, https://doi.org/10.3133/mr27.","productDescription":"Report: 4 p.; 1 Plate: 63.55 x 40.06 inches","costCenters":[],"links":[{"id":412282,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mr/27/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":412281,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/mr/27/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":179997,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mr/27/report-thumb.jpg"}],"scale":"3168000","country":"United States","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -127.25,24.25 ], [ -127.25,49.25 ], [ -66.5,49.25 ], [ -66.5,24.25 ], [ -127.25,24.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db64924b","contributors":{"authors":[{"text":"Gildersleeve, Benjamin","contributorId":14468,"corporation":false,"usgs":true,"family":"Gildersleeve","given":"Benjamin","email":"","affiliations":[],"preferred":false,"id":266643,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":62035,"text":"mr28 - 1962 - Thorium and rare earths in the United States, exclusive of Alaska and Hawaii","interactions":[{"subject":{"id":44016,"text":"ofr61112 - 1961 - Thorium and rare earths in the United States","indexId":"ofr61112","publicationYear":"1961","noYear":false,"title":"Thorium and rare earths in the United States"},"predicate":"SUPERSEDED_BY","object":{"id":62035,"text":"mr28 - 1962 - Thorium and rare earths in the United States, exclusive of Alaska and Hawaii","indexId":"mr28","publicationYear":"1962","noYear":false,"title":"Thorium and rare earths in the United States, exclusive of Alaska and Hawaii"},"id":1}],"lastModifiedDate":"2025-05-22T18:13:54.120275","indexId":"mr28","displayToPublicDate":"1962-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":324,"text":"Mineral Investigations Resource Map","code":"MR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"28","title":"Thorium and rare earths in the United States, exclusive of Alaska and Hawaii","docAbstract":"The accompanying map shows the location of the principal deposits of thorium and rare-earth minerals in the United States (excluding Alaska and Hawaii). Symbols of different shapes are used to depict deposits of different geologic types, and sizes of symbols denote the relative importance of the deposits. Because of scale limitations a symbol may represent groups of deposits too closely spaced to permit them to be distinguished separately. Some districts of considerable extent arc shown by a shaded pattern.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mr28","usgsCitation":"Olson, J.C., and Adams, J.W., 1962, Thorium and rare earths in the United States, exclusive of Alaska and Hawaii: U.S. Geological Survey Mineral Investigations Resource Map 28, Report: 16 p.; 1 Plate: 63.96 × 40.50 inches, https://doi.org/10.3133/mr28.","productDescription":"Report: 16 p.; 1 Plate: 63.96 × 40.50 inches","costCenters":[],"links":[{"id":486414,"rank":4,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/mr/28/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":180165,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mr/28/report-thumb.jpg"},{"id":408404,"rank":2,"type":{"id":36,"text":"NGMDB Index 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W.","contributorId":118270,"corporation":false,"usgs":true,"family":"Adams","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":854760,"contributorType":{"id":3,"text":"Compilers"},"rank":2}],"authors":[{"text":"Olson, J. C.","contributorId":55403,"corporation":false,"usgs":true,"family":"Olson","given":"J.","middleInitial":"C.","affiliations":[],"preferred":false,"id":937956,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Adams, J. W.","contributorId":118270,"corporation":false,"usgs":true,"family":"Adams","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":937957,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":6084,"text":"pp412 - 1961 - Salinity and hydrology of closed lakes","interactions":[],"lastModifiedDate":"2017-02-22T14:30:23","indexId":"pp412","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"412","title":"Salinity and hydrology of closed lakes","docAbstract":"Lakes without outlets, called closed lakes, are exclusively features of the arid and semiarid zones where annual evaporation exceeds rainfall. The number of closed lakes increases with aridity, so there are relatively few perennial closed lakes, but \"dry\" lakes that rarely contain water are numerous.
Closed lakes fluctuate in level to a much greater degree than the open lakes of the humid zone, because variations in inflow can be compensated only by changes in surface area. Since the variability of inflow increases with aridity, it is possible to derive an approximate relationship for the coefficient of variation of lake area in terms of data on rates of evaporation, lake area, lake depth, and drainage area.
The salinity of closed lakes is highly variable, ranging from less than 1 percent to over 25 percent by weight of salts. Some evidence suggests that the tonnage of salts in a lake solution is substantially less than the total input of salts into the lake over the period of existence of the closed lake. This evidence suggests further that the salts in a lake solution represent a kind of long-term balance between factors of gain and loss of salts from the solution.
Possible mechanisms for the loss of salts dissolved in the lake include deposition in marginal bays, entrapment in sediments, and removal by wind. Transport of salt from the lake surface in wind spray is also a contributing, but seemingly not major, factor.
The hypothesis of a long-term balance between input to and losses from the lake solution is checked by deriving a formula for the equilibrium concentration and comparing the results with the salinity data. The results indicate that the reported salinities seemingly can be explained in terms of their geometric properties and hydrologic environment.
The time for accumulation of salts in the lake solution the ratio between mass of salts in the solution and the annual input may also be estimated from the geometric and hydrologic factors, in the absence of data on the salt content of the lake or of the inflow.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp412","usgsCitation":"Langbein, W.B., 1961, Salinity and hydrology of closed lakes: U.S. Geological Survey Professional Paper 412, iii, 20 p., https://doi.org/10.3133/pp412.","productDescription":"iii, 20 p.","numberOfPages":"25","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":33126,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0412/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":118191,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0412/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ee4b07f02db5fdfa9","contributors":{"authors":[{"text":"Langbein, Walter Basil","contributorId":40581,"corporation":false,"usgs":true,"family":"Langbein","given":"Walter","email":"","middleInitial":"Basil","affiliations":[],"preferred":false,"id":152078,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":4170,"text":"cir452 - 1961 - Floods of February-March 1961 in the southeastern states","interactions":[],"lastModifiedDate":"2022-10-03T21:47:25.212447","indexId":"cir452","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"452","title":"Floods of February-March 1961 in the southeastern states","docAbstract":"Widespread, prolonged, disastrous floods struck parts of Louisiana, Mississippi, Alabama, Georgia, and Florida following heavy rains Feb. 17-26, 1961. Three distinct low-pressure systems recurred in essentially the same area. Precipitation totaled more than 18 inches in some areas. Multiple floods of small streams became superimposed in the large rivers to produce rare, record-breaking peaks and prolonged inundation. \n\nFour lives were lost; one in Louisiana and three in Mississippi. Highways, railroads, urban areas, and farms were heavily damaged.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir452","usgsCitation":"Barnes, H.H., and Somers, W.P., 1961, Floods of February-March 1961 in the southeastern states: U.S. Geological Survey Circular 452, iii, 21 p., https://doi.org/10.3133/cir452.","productDescription":"iii, 21 p.","costCenters":[],"links":[{"id":407830,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_23952.htm","linkFileType":{"id":5,"text":"html"}},{"id":31279,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1961/0452/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123134,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1961/0452/report-thumb.jpg"}],"country":"United States","state":"Alabama, Florida, Georgia, Mississippi","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -91,\n 30\n ],\n [\n -83,\n 30\n ],\n [\n -83,\n 35\n ],\n [\n -91,\n 35\n ],\n [\n -91,\n 30\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b26e4b07f02db6b003e","contributors":{"authors":[{"text":"Barnes, Harry Hawthorne","contributorId":64630,"corporation":false,"usgs":true,"family":"Barnes","given":"Harry","email":"","middleInitial":"Hawthorne","affiliations":[],"preferred":false,"id":510668,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Somers, William Philip","contributorId":48544,"corporation":false,"usgs":true,"family":"Somers","given":"William","email":"","middleInitial":"Philip","affiliations":[],"preferred":false,"id":510667,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":44016,"text":"ofr61112 - 1961 - Thorium and rare earths in the United States","interactions":[{"subject":{"id":44016,"text":"ofr61112 - 1961 - Thorium and rare earths in the United States","indexId":"ofr61112","publicationYear":"1961","noYear":false,"title":"Thorium and rare earths in the United States"},"predicate":"SUPERSEDED_BY","object":{"id":62035,"text":"mr28 - 1962 - Thorium and rare earths in the United States, exclusive of Alaska and Hawaii","indexId":"mr28","publicationYear":"1962","noYear":false,"title":"Thorium and rare earths in the United States, exclusive of Alaska and Hawaii"},"id":1}],"supersededBy":{"id":62035,"text":"mr28 - 1962 - Thorium and rare earths in the United States, exclusive of Alaska and Hawaii","indexId":"mr28","publicationYear":"1962","noYear":false,"title":"Thorium and rare earths in the United States, exclusive of Alaska and Hawaii"},"lastModifiedDate":"2012-02-02T00:11:02","indexId":"ofr61112","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"61-112","title":"Thorium and rare earths in the United States","language":"ENGLISH","doi":"10.3133/ofr61112","issn":"ma","usgsCitation":"Olson, J.C., and Adams, J., 1961, Thorium and rare earths in the United States: U.S. Geological Survey Open-File Report 61-112, 1 map., https://doi.org/10.3133/ofr61112.","productDescription":"1 map.","costCenters":[],"links":[{"id":168831,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a54e4b07f02db62bcad","contributors":{"authors":[{"text":"Olson, Jerry Chipman","contributorId":57869,"corporation":false,"usgs":true,"family":"Olson","given":"Jerry","email":"","middleInitial":"Chipman","affiliations":[],"preferred":false,"id":228997,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Adams, J.W.","contributorId":101290,"corporation":false,"usgs":true,"family":"Adams","given":"J.W.","email":"","affiliations":[],"preferred":false,"id":228998,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70220637,"text":"70220637 - 1961 - Is the Tinaquillo, Venezuela, \"Pseudogabbro\" metamorphic or magmatic?","interactions":[],"lastModifiedDate":"2021-05-21T18:10:07.555568","indexId":"70220637","displayToPublicDate":"1961-12-31T13:05:18","publicationYear":"1961","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":"Is the Tinaquillo, Venezuela, \"Pseudogabbro\" metamorphic or magmatic?","docAbstract":"The \"pseudogabbro\" associated with peridotite at Tinaquillo, Venezuela, is believed to be of magmatic rather than metamorphic origin principally because: (1) there are major mineralogic and compositional differences between the \"pseudogabbro\" and the most highly metamorphosed country rock; (2) rocks intermediate in compositional between peridotite and \"pseudogabbro\" are present; (3) augen of lamellar pyroxene which occur in the \"pseudogabbro\" but not in the country rock are of a kind found elsewhere rarely except in igneous rocks; (4) gabbroic rocks are associated with peridotite elsewhere in Venezuela and in the Carribbean region; (5) textural and structural features of the kind found in the Tinaquillo rocks are characteristic of alpine-type peridotite-gabbro complexes.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1565:ITTVPM]2.0.CO;2","usgsCitation":"Thayer, T.P., and Brown, C., 1961, Is the Tinaquillo, Venezuela, \"Pseudogabbro\" metamorphic or magmatic?: Geological Society of America Bulletin, v. 72, no. 10, p. 1565-1569, https://doi.org/10.1130/0016-7606(1961)72[1565:ITTVPM]2.0.CO;2.","productDescription":"5 p.","startPage":"1565","endPage":"1569","costCenters":[],"links":[{"id":385857,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Venezuela","city":"Tinaquillo","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -70.64208984375,\n 9.286464684304082\n ],\n [\n -70.213623046875,\n 9.286464684304082\n ],\n [\n -70.213623046875,\n 9.535748998133627\n ],\n [\n -70.64208984375,\n 9.535748998133627\n ],\n [\n -70.64208984375,\n 9.286464684304082\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"72","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Thayer, T. P.","contributorId":64629,"corporation":false,"usgs":true,"family":"Thayer","given":"T.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":816267,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brown, C.","contributorId":21484,"corporation":false,"usgs":true,"family":"Brown","given":"C.","affiliations":[],"preferred":false,"id":816268,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":39004,"text":"pp354F - 1960 - Zones and zonal variations in welded ash flows","interactions":[],"lastModifiedDate":"2015-09-24T14:16:47","indexId":"pp354F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"354","chapter":"F","title":"Zones and zonal variations in welded ash flows","docAbstract":"Welded tuffs are recognized as special parts of ash flows, other pyroclastic flows, or, more rarely, air-fall deposits. Ash flows may be emplaced at any temperature below a maximum eruption temperature. Those emplaced above a minimum welding temperature may show any and all degrees of welding and crystallization.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/pp354F","usgsCitation":"Smith, R.L., 1960, Zones and zonal variations in welded ash flows: U.S. Geological Survey Professional Paper 354, Report: 11 p.; 2 Plates: 16.55 x 10.82 inches, https://doi.org/10.3133/pp354F.","productDescription":"Report: 11 p.; 2 Plates: 16.55 x 10.82 inches","startPage":"149","endPage":"159","numberOfPages":"16","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":113314,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0354f/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":113315,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0354f/plate-20.pdf","text":"Plate 20","linkFileType":{"id":1,"text":"pdf"}},{"id":169900,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0354f/report-thumb.jpg"},{"id":308541,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0354f/plate-21.pdf","text":"Plate 21","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4791e4b07f02db48b464","contributors":{"authors":[{"text":"Smith, R. L.","contributorId":93904,"corporation":false,"usgs":true,"family":"Smith","given":"R.","email":"","middleInitial":"L.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":220793,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47380,"text":"b1082F - 1960 - Geology and fluorspar deposits, Northgate district, Colorado","interactions":[{"subject":{"id":43620,"text":"ofr5182 - 1951 - Geologic maps of the Northgate fluorspar district, Colorado","indexId":"ofr5182","publicationYear":"1951","noYear":false,"title":"Geologic maps of the Northgate fluorspar district, Colorado"},"predicate":"SUPERSEDED_BY","object":{"id":47380,"text":"b1082F - 1960 - Geology and fluorspar deposits, Northgate district, Colorado","indexId":"b1082F","publicationYear":"1960","noYear":false,"chapter":"F","title":"Geology and fluorspar deposits, Northgate district, Colorado"},"id":1},{"subject":{"id":47380,"text":"b1082F - 1960 - Geology and fluorspar deposits, Northgate district, Colorado","indexId":"b1082F","publicationYear":"1960","noYear":false,"chapter":"F","title":"Geology and fluorspar deposits, Northgate district, Colorado"},"predicate":"IS_PART_OF","object":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"id":2}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2017-10-18T14:10:41","indexId":"b1082F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1082","chapter":"F","title":"Geology and fluorspar deposits, Northgate district, Colorado","docAbstract":"The fluorspar deposits in the Northgate district, Jackson County, Colo., are among the largest in Western United States. The mines were operated intermittently during the 1920's and again during World War II, but production during these early periods of operation was not large. Mining was begun on a larger scale in 1951, and the district has assumed a prominent position among the fluorspar producers in the United States.
Within the Northgate district, Precambrian metamorphic and igneous rocks crop out largely in the Medicine Bow Mountains, and later sedimentary rocks underlie North Park and fill old stream valleys in the mountains.
The metamorphic rocks constitute a gneiss complex that formed under progressively changing conditions of regional metamorphism. They consist principally of hornblende-plagioclase gneiss (hornblende gneiss), quartz monzonite gneiss, pegmatite, biotite-garnet-quartz-plagioclase gneiss (biotite-garnet gneiss), hornblende-biotite-quartz-plagioclase gneiss (hornblende-biotite gneiss) and mylonite gneiss.
The igneous rocks comprise some local fine-grained dacite porphyry dikes near the west margin of the district, and a quartz monzonitic stock and associated dikes in the central and eastern parts of the district.
The sedimentary rocks in the district range in age from Permian to Recent. Folded Permian and Mesozoic rocks underlie the basin of North Park, and consist in sequence from oldest to youngest, of Satanka(?) shale (0-50 feet of brick-red shale) and Forelle(?) limestone (8-15 feet of pink to light-gray laminated limestone) of Permian age, Chugwater formation of Permian and Triassic age (690 feet of red silty shale and sandstone), Sundance formation of Late Jurassic age (145 feet of sandstone containing some shale and limestone), Morrison formation of Late Jurassic age (445 feet of variegated shale and minor sandstone and limestone), Dakota group as used by Lee (1927), now considered to be of Early Cretaceous age in this area (200-320 feet of pebbly sandstone, sandstone, and shale), Ben ton shale of Early and Late Cretaceous age (665 feet of dark-gray thin-bedded shale), Niobrara formation of Late Cretaceous age (865 feet of yellow to gray limy siltstone and shale), and Pierre shale of Late Cretaceous age (more than 60 feet of dark-gray fissile shale). Unconformities separate the Chugwater and Sundance formations, and the Morrison formation and the Dakota group.
Nonmarine strata of the White River formation of Oligocene age and the North Park formation of Miocene and Pliocene (?) age fill Tertiary valleys cut in the Precambrian rocks of the mountain areas, and Quaternary terrace gravel, alluvium, and dune sand mantle much of the floor of North Park.
The main outlines of the modern Rocky Mountains formed during the Laramide orogeny in late Mesozoic and early Tertiary time. Most of the Laramide structures that can be recognized in the Northgate district involve the sedimentary rocks underlying North Park which are folded into northwest-trending anticlines and synclines. The folds are open and in most the beds dip 60° or less. Yet many anticlines are cut by reverse faults of widely different trends and directions of offset. Transverse faults offset some of the folds, and the character of folding commonly is markedly different on opposing sides of these faults. The North Park basin is cut off on the north by the east-trending Independence Mountain fault, a north-dipping reverse fault along which hard Precambrian rocks have been thrust up across the trend of the earlier Laramide structures. The North Park basin is still a major structure where it is interrupted by the Independence Mountain fault, and the original basin must have extended much farther north.
Disrupted gradients at the base of pre-White River valleys suggest that the Northgate district and adjacent areas may have been deformed in middle Tertiary time, but the evidence is not conclusive. A more definite period of deformation took place in Pliocene time following deposition of the North Park formation. North Park strata in south-central North Park were folded into a northwest-trending syncline, and the central part of the Northgate district probably was warped up along a north- or northwestward-trending axis.
Four north- to northwestward-trending faults cut the Precambrian rocks and White River formation on Pinkham Mountain and the area to the southeast. Similar faults 2½ and 15 miles west of the Northgate district cut rocks of the North Park formation, and all probably formed during the Pliocene period of deformation. The known commercial fluorspar deposits are localized along the two larger faults of the Northgate district, and they have been studied in detail.
The White River formation in early Oligocene time covered a hilly terrain drained by southward-flowing streams. By late Miocene, the northward-flowing streams had cut to about the same levels reached by the pre-White River streams and had partly exhumed and modified the older terrain. During late Miocene and early Pliocene (?) time, the Northgate area was buried beneath the clays, sands, and gravels of the North Park formation. Subsequent erosion removed the higher part of the North Park formation, cut a surface of low relief across the exhumed Precambrian rocks, and removed all topographic evidence of the Pliocene period of deformation. The present courses of the major streams were superimposed across the buried terrains during this period of erosion. Rejuvenation during middle Pleistocene caused all major streams to become incised in sharp canyons.
Copper minerals occur in small concentrations in some of the pegmatite masses in the gneiss complex. The copper-rich masses rarely exceed a few feet in diameter and constitute only a small part of the associated pegmatite body.
Vermiculite is exposed in prospect pits and mine workings along the west margin of the Northgate district. All the venniculite that was seen is associated with small masses of horablendite, massive chlorite, or serpentinite where these masses are near or are cut by pegmatite bodies. Some of the deposits may be potential producers of commercial-grade vermiculite, but most are small and erratic in shape or grade.
Fluorspar is the main mineral commodity that has been produced from the Northgate district. It was deposited during two distinct periods of mineralization, but only the younger deposits have been productive.
Small bodies of silicified breccia containing minor coarsely crystalline fluorite occur along the Independence Mountain fault, and in a few places along other Laramide faults. The fluorspar is an integral part of the fault breccia and apparently was deposited while the enclosing fault was still active.
The largest deposits of fluorspar in the Northgate district occur along the late Tertiary (?) faults on Pinkham Mountain. The fluorspar consists typically of botryoidal layers that formed as successive encrustations along open fractures, or as finely granular aggregates replacing and cementing fault gouge and White River formation. Many incompletely filled cavities, called water courses, still exist. Fluorite is the principal vein material; fragments of country rock constitute the chief impurity although finely granular quartz or chalcedony is common locally. Soft powdery manganese oxide coats many fractures and in places is associated with a fine white clay.
Fluorspar was deposited in or adjacent to open spaces along the late Tertiary (?) faults. Fractures in hard granitic rocks tended to remain open after faulting and were the favored sites for fluorspar deposition; fractures in the less competent hornblende and hornblende-biotite gneiss and schist generally were tight and little fluorspar was deposited. The White River rocks, although soft, were permeable and were widely impregnated or replaced by fluorspar.
Both of the main vein zones are along faults that have predominant rightlateral strike-slip displacement. As they theoretically should be, the vein zones are narrower and contain less fluorspar where the containing fault is deflected to the left than where the fault is deflected to the right and the fractures remained open.
The crustified, vuggy structure of the fluorspar and the common association with chalcedony or finely granular quartz suggest deposition in a very shallow environment, but no direct evidence bearing on the depth at which the fluorspar formed was seen. Fluorspar was deposited throughout a vertical range of 600 feet or more on each of the main vein zones, and for a vertical range of 1,050 feet for the district as a whole. None of the deposits had been bottomed at the time this report was prepared.
Exploration at depth beneath known ore bodies is favorable for developing large tonnages of fluorspar. The best possibilities for finding new ore bodies near the surface are along the northwestern and southeastern parts of the Fluorine-Camp Creek vein zone where large bodies of granitic rocks are intersected by the fault. These areas are generally mantled by a thick overburden, and have been inadequately tested so far.
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