The Aurora area is a glaciated upland of drift-mantled slopes, channels, swamps, and glacial-lake plains. It covers about 24 square miles of the eastern part of the Mesabi Iron Range in northeastern Minnesota. A deep narrow channel along the Embarrass River, the principal outlet of a former large glacial lake north of the Embarrass Mountains, lies partly within the area.
\nThe deposits in the report area consist of bedrock and unconsolidated glacial drift. The 'bedrock belongs to the Animikie Group of late Preeambrian age and consists of taconite (an iron-rich silicate rock) in the northern part and slightly metamorphosed argillite in the middle and southern parts. Bedrock is exposed only in the open-pit iron mines. Large quantities of ground water are pumped from porous and permeable ore zones in the St. James Mine. Small quantities of ground water are obtainable from openings along bedding planes and fractures in the argillite. Unconsolidated deposits consisting of till and water-laid glacial and alluvial materials mantle the bedrock to depths ranging from about 20 feet in the north-central part of the Aurora area to more than 300 feet near the Embarrass River. Thick deposits of sand and gravel in the Embarrass channel are capable of yielding large quantites of water. At places along the Partridge River glaeiofluvial deposits (glacial sediments deposited in running water) could yield moderate to large quantities of water. Sandy to bouldery till yields small quantities of water to domestic wells.
\nWell yields in the Aurora area range from less than 5 gpm (gallons per minute) to about 250 gpm from a well tapping an ore body. The specific capacity of wells penetrating ore zones ranges from about 7 gpm per foot of drawdown to 25 gpm per foot of drawdown. Although no attempt has been made to develop a high-yield well in the sand and gravel deposits of the Embarrass channel, more than 5,000 gpm is pumped from sumps which collect water from these deposits in the Embarrass mine. Most domestic wells yield about 5 gpm and are drilled and finished in sand or gravel in either the bouldery till or glaciofluvial deposits.
\nGround water from the unconsolidated deposits is hard and commonly contains large, undesirable amounts of iron and manganese. Water from the 'bedrock aquifers contains less iron and manganese than does water from the unconsolidated deposits.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1809U","collaboration":"Prepared in cooperation with the Department of Iron Range Resources and Rehabilitaion","usgsCitation":"Maclay, R.W., 1966, Reconnaissance of the geology and ground-water resources in the Aurora area, St. Louis county, Minnesota: U.S. Geological Survey Water Supply Paper 1809, Document: 20 p.; Plate: 24.0 x 19.5 inches, https://doi.org/10.3133/wsp1809U.","productDescription":"Document: 20 p.; Plate: 24.0 x 19.5 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":138265,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809u/report-thumb.jpg"},{"id":27830,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1809u/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27831,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809u/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Minnesota","county":"St. Louis County","city":"Aurora","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -92.308333,\n 47.545833\n ],\n [\n -92.308333,\n 47.483333\n ],\n [\n -92.166667,\n 47.483333\n ],\n [\n -92.166667,\n 47.545833\n ],\n [\n -92.308333,\n 47.545833\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a64e4b07f02db637b63","contributors":{"authors":[{"text":"Maclay, Robert W.","contributorId":13210,"corporation":false,"usgs":true,"family":"Maclay","given":"Robert","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":144798,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2175,"text":"wsp1807 - 1966 - Ground-water resources of Sheridan County, Wyoming","interactions":[],"lastModifiedDate":"2012-02-02T00:05:24","indexId":"wsp1807","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":"1807","title":"Ground-water resources of Sheridan County, Wyoming","docAbstract":"Sheridan County is in the north-central part of Wyoming and is an area of about 2,500 square miles. The western part of the county is in the Bighorn Mountains, and the eastern part is in the Powder River structural basin. Principal streams are the Powder and Tongue Rivers, which are part of the Yellowstone River system. The climate is semiarid, and the mean annual precipitation at Sheridan is about 16 inches. \r\n\r\nRocks of Precambrian age are exposed in the central part of the Bighorn Mountains, and successively younger rocks are exposed eastward. Rocks of Tertiary age, which are the most widespread, are exposed throughout a large part of the Powder River structural basin. Deposits of Quaternary age underlie the flood plains and terraces along the larger streams, particularly in the western part of the basin. \r\n\r\nAquifers of pre-Tertiary age are exposed in the western part of the county, but they dip steeply and are deeply buried just a few miles east of their outcrop. Aquifers that might yield large supplies of water include the Bighorn Dolomite, Madison Limestone, Amsden Formation, and Tensleep Sandstone. The Flathead Sandstone, Sundance Formation, Morrison Formation, Cloverly Formation,. Newcastle Sandstone, Frontier Formation, Parkman Sandstone, Bearpaw Shale, .and Lance Formation may yield small or, under favorable conditions, moderate supplies of water. \r\n\r\nFew wells tap aquifers of pre-Tertiary age, and these are restricted to the outcrop area. The meager data available indicate that the water from the Lance Formation, Bearpaw Shale, Parkman Sandstone, Tensleep Sandstone and Amsden Formation, and Flathead Standstone is of suitable quality for domestic or stock purposes, and that water from the Tensleep Sandstone and Amsden Formation and the Flathead Sandstone is of good quality for irrigation. Samples could not be obtained from other aquifers of pre-Tertiary age; so the quality of water in these aquifers could not be determined. \r\n\r\nAdequate supplies of ground water for stock or domestic use can be developed throughout much of the report area from the Fort Union and Wasatch Formations of Tertiary age; larger supplies might be obtained from the coarse-grained sandstone facies of the Wasatch Formation near Moncreiffe Ridge. Four aquifer tests were made at wells tapping formations of Tertiary age, and the coefficients of permeability determined ranged from 2.5 to 7.9 gallons per day per square foot. The depths to which wells must be drilled to penetrate an aquifer differ within relatively short distances because of the lenticularity of the aquifers. Water in aquifers of Tertiary age may occur under water-table, artesian, or a combination of artesian and gas-lift conditions. \r\n\r\nWater from the Fort Union is usable for domestic purposes, but the iron and dissolved-solids content impair the quality at some localities. Water from the Fort Union Formation is not recommended for irrigation because of sodium and bicarbonate content. The water is regarded as good to fair for stock use. Water from the Wasatch Formation generally contains dissolved solids in excess of the suggested domestic standards, but this water is usable in the absence of other supplies. The development of irrigation supplies from the Wasatch Formation may be possible in some areas, but the water quality should be carefully checked. Water of good to very poor quality for stock supplies is obtained, depending upon the location. Hydrogen sulfide, commonly present in water of the Fort Union and Wasatch Formations, becomes an objectionable characteristic when the water is used for human consumption. \r\n\r\nDeposits of Quaternary age generally yield small to moderate supplies of water to wells. Two pumping tests were conducted, and the coefficients of permeability of the aquifers tested were 380 and 1,100 gallons per day per square foot. Usable supplies of ground water can be developed from the deposits of Quaternary age, principally along the valleys of perennial strea","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1807","usgsCitation":"Lowry, M.E., and Cummings, T.R., 1966, Ground-water resources of Sheridan County, Wyoming: U.S. Geological Survey Water Supply Paper 1807, iv, 77 p. :illus., maps (1 fold. col. in pocket) ;24 cm., https://doi.org/10.3133/wsp1807.","productDescription":"iv, 77 p. :illus., maps (1 fold. col. in pocket) ;24 cm.","costCenters":[],"links":[{"id":138198,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1807/report-thumb.jpg"},{"id":27788,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1807/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27789,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1807/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d694","contributors":{"authors":[{"text":"Lowry, Marlin E.","contributorId":52552,"corporation":false,"usgs":true,"family":"Lowry","given":"Marlin","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":144773,"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":144772,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":38849,"text":"pp543D - 1966 - Geologic effects of the March 1964 earthquake and associated seismic sea waves on Kodiak and nearby islands, Alaska","interactions":[],"lastModifiedDate":"2022-02-17T19:34:30.778879","indexId":"pp543D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1966","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":"543","chapter":"D","title":"Geologic effects of the March 1964 earthquake and associated seismic sea waves on Kodiak and nearby islands, Alaska","docAbstract":"Kodiak Island and the nearby islands constitute a mountainous landmass with an aggregate area of 4,900 square miles that lies at the western border of the Gulf of Alaska and from 20 to 40 miles off the Alaskan mainland. Igneous and metamorphic rocks underlie most of the area except for a narrow belt of moderately to poorly indurated rocks bordering the Gulf of Alaska coast and local accumulations of unconsolidated alluvial and marine deposits along the streams and coast. The area is relatively undeveloped and is sparsely inhabited. About 4,800 of the 5,700 permanent residents in the area live in the city of Kodiak or at the Kodiak Naval Station.\n\nThe great earthquake, which occurred on March 27, 1964, at 5:36 p.m. Alaska standard time (March 28,1964, 0336 Greenwich mean time), and had a Richter magnitude of 8.4-8.5, was the most severe earthquake felt on Kodiak Island and its nearby islands in modern times. Although the epicenter lies in Prince William Sound 250 miles northeast of Kodiak—the principal city of the area—the areal distribution of the thousands of aftershocks that followed it, the local tectonic deformation, and the estimated source area of the subsequent seismic sea wave, all suggest that the Kodiak group of islands lay immediately adjacent to, and northwest of, the focal region from which the elastic seismic energy was radiated. The duration of strong ground motion in the area was estimated at 2½ minutes. Locally, the tremors were preceded by sounds audible to the human ear and were reportedly accompanied in several places by visible ground waves.\n\nIntensity and felt duration of the shocks during the main earthquake and aftershock sequence varied markedly within the area and were strongly influenced by the local geologic environment. Estimated Mercalli intensities in most areas underlain by unconsolidated Quaternary deposits ranged from VIII to as high as IX. In contrast, intensities in areas of upper Tertiary rock ranged from VII to VIII, and in areas of relatively well indurated lower Tertiary and Mesozoic rocks, from VI to VII.\n\nLocal subsidence of as much as 10 feet was widespread in noncohesive granular deposits through compaction, flow, and sliding that resulted from vibratory loading during the earthquake. This phenomenon, which was largely restricted to saturated beach and alluvial deposits or artificial fill, was locally accompanied by extensive cracking of the ground and attendant ejection of water and water-sediment mixtures.\n\nNumerous landslides, including a wide variety of rockfalls, rockslides, and flows along steep slopes, were triggered by the long-duration horizontal and vertical accelerations during the earthquake. The landslides are most numerous in a narrow belt along the southeast coast of Kodiak Island and the nearby offshore islands. Their abundance appears to be related to an area underlain predominantly by Tertiary rocks.\n\nTemporary and permanent changes of level occurred after the earthquake in some wells, lakes, and streams throughout the area; ice was cracked, and the salinity of a few wells increased. Permanent change of water level at some localities appears to be related to readjustments of fracture porosity by earthquake-induced movements of bedrock blocks. Increased salinity of wells in coastal areas resulted from encroachment of seawater into aquifiers after subsidence during the earthquake, and to flooding of watersheds by seismic sea waves.\n\nVertical displacements, both downward and upward, occurred throughout the area as a result of crustal warping along a northeast-trending axis. Most of Kodiak and all of Afognak, Shuyak, and adjacent islands are within a regional zone of subsidence whose trough plunges gently northeastward and approximately coincides with the mountainous backbone of Kodiak Island. Subsidence in excess of 6 feet occurred throughout the northern part of the zone-a maximum subsidence of 6½ feet having occurred on Marmot and, eastern Afognak Islands. Southeast of the axis of tectonic tilting, uplift of at least 2lh feet occurred in a narrow zone that includes most of the southeasterly capes of Kodiak Island, the southeastern half of Sitkalidak Island, and Sitkinak Island. The uplift is inferred to extend offshore over much or all of the continental shelf adjacent to the Kodiak group of islands. Within the affected area, tectonic subsidence, which was locally augmented by surficial subsidence of unconsolidated. deposits, caused widespread inundation of shorelines and attendant damage to intertidal organisms, nearshore terrestrial vegetation, and salmon-spawning areas.\n\nThe most devastating effect of the earthquake on Kodiak Island and nearby islands resulted from seismic sea waves that probably originated along a linear zone of differential uplift in the Gulf of Alaska. A train of at least seven seismic sea waves, having initial periods of 50–55 minutes, struck along all the southeast coast of the island group from 38 to 63 minutes after the earthquake. The southeast shores were repeatedly washed by destructive waves having runup heights along exposed coasts of perhaps as much as 40 feet above existing tide level, and of 8–20 feet along protected shores. Runup heights of the waves were much less on the northwest and southwest sides of the islands, and no wave damage was incurred there. Locally, high-velocity currents that accompanied the waves caused intense erosion and redistribution of unconsolidated natural and artificial shore deposits and of shallow sea-floor deposits.\n\nThe Alaska earthquake was the greatest natural catastrophe to befall the Kodiak Island area in historic time. The combination of seismic shock and the earthquake-related tectonic deformation and seismic sea waves took 18 lives, destroyed property worth about $45 million, and resulted in estimated losses of income to the fishing industry of an additional $5 million.\n\nMost of the damage and all of the loss of life were directly attributable to the seismic sea waves that crippled the city of Kodiak, wiped out the village of Kaguyak, and destroyed most of the village of Old Harbor and parts of the villages of Afognak and Uzinki. Bridges and segments of the highways in the vicinity of the city of Kodiak were washed out, and parts of the Kodiak Naval Station were inundated and damaged. Especially serious to all the damaged communities was the loss of fishing boats, seafood processing plants, and other waterfront installations, which had been the mainstay of the economy.\n\nAdditional heavy losses resulted from the combined regional tectonic and local surficial subsidence that occurred during the earthquake. Widespread shoreline flooding by high tides necessitated raising, protecting, or removing many installations otherwise undamaged by the earthquake or waves.\n\nStructural damage attributable to seismic shock during the earthquake was relatively light and was restricted to areas underlain by saturated unconsolidated deposits. The chief structural failure in the area as a result of shaking was the collapse of part of a cannery built on saturated beach deposits that were partially liquefied during the earthquake. Minor structural damage resulted from differential settlement and cracking of the ground on natural granular deposits and artificial fills. The overwhelming majority of structures are constructed on indurated bedrock; none of these sustained damage other than small losses resulting from shifting about and breakage of their contents.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"The Alaska earthquake, March 27, 1964: Regional effects (Professional Paper 543)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp543D","usgsCitation":"Plafker, G., and Kachadoorian, R., 1966, Geologic effects of the March 1964 earthquake and associated seismic sea waves on Kodiak and nearby islands, Alaska: U.S. Geological Survey Professional Paper 543, vi, 46 p., https://doi.org/10.3133/pp543D.","productDescription":"vi, 46 p.","numberOfPages":"58","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":277742,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/pp543D.gif"},{"id":65810,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0543d/pp543d_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":396126,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_99029.htm"},{"id":277741,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0543d/index.html"}],"country":"United States","state":"Alaska","otherGeospatial":"Afognak Island, Kodiak Island, Marmot Island, Rasberry Island, Shuyak Island, Sitkalidak Island, Sitkinak Island, Spruce Island, Tugidak Island, Uganik Island","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -155,\n 56.3778\n ],\n [\n -151.6917,\n 56.3778\n ],\n [\n -151.6917,\n 58.6444\n ],\n [\n -155,\n 58.6444\n ],\n [\n -155,\n 56.3778\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a633d","contributors":{"authors":[{"text":"Plafker, George","contributorId":3920,"corporation":false,"usgs":false,"family":"Plafker","given":"George","email":"","affiliations":[],"preferred":false,"id":220538,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kachadoorian, Reuben","contributorId":24336,"corporation":false,"usgs":true,"family":"Kachadoorian","given":"Reuben","email":"","affiliations":[],"preferred":false,"id":220539,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":3820,"text":"cir524 - 1966 - The changing pattern of ground-water development on Long Island, New York","interactions":[],"lastModifiedDate":"2017-08-27T17:57:37","indexId":"cir524","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1966","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":"524","title":"The changing pattern of ground-water development on Long Island, New York","docAbstract":"Ground-water development on Long Island has followed a pattern that has reflected changing population trends, attendant changes in the use and disposal of water, and the response of the hydrologic system to these changes. The historic pattern of development has ranged from individually owned shallow wells tapping glacial deposits to large-capacity public-supply wells tapping deep artesian aquifers. Sewage disposal has ranged from privately owned cesspools to modern large-capacity sewage-treatment plants discharging more than 70 mgd of water to the sea. \r\n\r\nAt present (1965), different parts of long Island are characterized by different stages of ground-water development. In parts of Suffolk County in eastern long Island, development is similar to the earliest historical stages. Westward toward New York City, ground-water development becomes more intensive and complex, and the attendant problems become more acute. The alleviation of present problems and those that arise in the future will require management decisions based on the soundest possible knowledge of the hydrologic system, including an understanding of the factors involved in the changing pattern of ground-water development on the island.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir524","usgsCitation":"Heath, R., Foxworthy, B., and Cohen, P.M., 1966, The changing pattern of ground-water development on Long Island, New York: U.S. Geological Survey Circular 524, iii, 10 p. :illus., maps. ;27 cm., https://doi.org/10.3133/cir524.","productDescription":"iii, 10 p. :illus., maps. ;27 cm.","costCenters":[],"links":[{"id":30890,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1966/0524/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139237,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1966/0524/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a68e4b07f02db63b226","contributors":{"authors":[{"text":"Heath, Ralph C.","contributorId":53359,"corporation":false,"usgs":true,"family":"Heath","given":"Ralph C.","affiliations":[],"preferred":false,"id":147671,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Foxworthy, B. L.","contributorId":45686,"corporation":false,"usgs":true,"family":"Foxworthy","given":"B. L.","affiliations":[],"preferred":false,"id":147670,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cohen, Philip M.","contributorId":67860,"corporation":false,"usgs":true,"family":"Cohen","given":"Philip","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":147672,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2348,"text":"wsp1819H - 1966 - Fluvial sediment and chemical quality of water in the Little Blue River basin, Nebraska and Kansas","interactions":[],"lastModifiedDate":"2012-02-02T00:05:20","indexId":"wsp1819H","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":"1819","chapter":"H","title":"Fluvial sediment and chemical quality of water in the Little Blue River basin, Nebraska and Kansas","docAbstract":"The Little Blue River drains about 3,37)0 square miles in south-central Nebraska and north-central Kansas. The uppermost bedrock in the basin is limestone and shale of Permian age and sandstone, shale, and limestone of Cretaceous age. Bedrock is exposed in many places in the lower one-third of the basin but elsewhere is buried beneath a thin to thick mantle of younger sediments, mostly of Quaternary age. These younger sediments are largely fluvial and eolian deposits but also include some glacial till. Consisting in large part of sand and gravel, the fluvial deposits are an important source of ground-water supplies throughout much of the upper two-thirds of the basin. Loess, an eolian deposit of clayey silt, is by far the most widespread surficial deposit. The climate is continental. Temperatures ranging from -38 ? F to 118 ? F have been recorded in the basin. Average annual precipitation as low as 10.31 and as high as 49.32 inches has been recorded. During most years in the period 1956-62, when nearly all the water-quality data were obtained, annual precipitation and annual runoff were greater than normal. Flow-duration data indicate, however, that the flow distribution for the period was near normal. The Little Blue River has the same suspended-sediment characteristics as nearly all unregulated streams in the Great Plains--a wide range in concentrations, low concentrations during low-flow periods, and high concentrations during almost all periods of significant overland runoff. The maximum instantaneous concentration normally occurs many hours before maximum water discharge during any given rise in stage; the maximum daily mean concentration during any given year normally occurs at a moderate stream stage, not during a major flood. \r\n\r\nSuspended-sediment data for Little Blue River near Deweese, Nebr., which receives drainage from the upstream third of the basin, approximately, show that during the 1!}57-61 water years concentrations of 100 ppm (parts per million) or less prevailed about 42 percent of the time and concentrations of 1,000 ppm or less prevailed about 85 percent of the time. Observed concentrations ranged from 2 to 21,000 ppm: daily mean concentrations ranged from 2 to 13,800 ppm.\r\n\r\nThe discharge-weighted suspended-sediment concentration was computed as about 2,800 ppm at Little Blue River near Deweese, about 3,300 ppm near Fairbury (Endicott), and about 3,000 ppm at Waterville. These stations receive drainage from about one-third, two-thirds, and nearly all the basin, respectively. Water-utilization problems resulting from high concentrations are not significant in the basin ; use of water from the Little Blue River is quantitatively negligible. Concentrations and, consequently, discharges of sediment are greater at a given water discharge on a rising stage than at the same discharge on the falling stage of the same runoff event. Also, a wide range in sediment discharge occurs at similar water discharges during different runoff events. Daily sediment discharges at Little Blue River near Deweese ranged from about 1,400 to 16,000 tons at daily mean water discharges of about 500 cfs (cubic feet per second) and from almost 7,500 to 28,000 tons at water discharges of about 1,000 cfs. \r\n\r\nThe estimated long-term sediment discharge at Little Blue River near Deweese is about 400,000 tons per year: near Fairbury, about 1,200,000 tons per year: and at Waterville, about 1.900,000 tons per year. The high sediment discharge from the downstream part of the basin is due to greater precipitation and runoff--not to higher concentrations of suspended sediment--in the downstream parts of the basin. \r\n\r\nNearly all the suspended sediment is silt and clay. The streambed material is mainly medium sand to gravel. The median particle size of bed material observed was about 0.73 mm near Deweese and about 0.77 mm near Fairbury. A few computations of total sediment discharge of Little Blue River near Deweese indicate that suspended-sedim","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1819H","usgsCitation":"Mundorff, J.C., and Waddell, K., 1966, Fluvial sediment and chemical quality of water in the Little Blue River basin, Nebraska and Kansas: U.S. Geological Survey Water Supply Paper 1819, v, 45 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1819H.","productDescription":"v, 45 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":137766,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1819h/report-thumb.jpg"},{"id":28270,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1819h/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d6e4b07f02db5de61f","contributors":{"authors":[{"text":"Mundorff, J. C.","contributorId":63374,"corporation":false,"usgs":true,"family":"Mundorff","given":"J.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":145059,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Waddell, K.M.","contributorId":59009,"corporation":false,"usgs":true,"family":"Waddell","given":"K.M.","email":"","affiliations":[],"preferred":false,"id":145058,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":36022,"text":"b1209 - 1966 - Rapid modal analysis of some felsic rocks from calibrated X-ray diffraction patterns","interactions":[],"lastModifiedDate":"2012-02-02T00:09:32","indexId":"b1209","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1966","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":"1209","title":"Rapid modal analysis of some felsic rocks from calibrated X-ray diffraction patterns","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/b1209","usgsCitation":"Tatlock, D.B., 1966, Rapid modal analysis of some felsic rocks from calibrated X-ray diffraction patterns: U.S. Geological Survey Bulletin 1209, 41 p. illus. ;24 cm., https://doi.org/10.3133/b1209.","productDescription":"41 p. illus. ;24 cm.","costCenters":[],"links":[{"id":166766,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1209/report-thumb.jpg"},{"id":63967,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1209/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649402","contributors":{"authors":[{"text":"Tatlock, Donald Bruce","contributorId":17250,"corporation":false,"usgs":true,"family":"Tatlock","given":"Donald","email":"","middleInitial":"Bruce","affiliations":[],"preferred":false,"id":215632,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2183,"text":"wsp1613F - 1966 - Salt-water encroachment in southern Nassau and southeastern Queens Counties, Long Island, New York","interactions":[],"lastModifiedDate":"2012-02-02T00:05:24","indexId":"wsp1613F","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":"1613","chapter":"F","title":"Salt-water encroachment in southern Nassau and southeastern Queens Counties, Long Island, New York","docAbstract":"Test drilling, extraction of water from cores, electric logging, water sampling, and water-level measurements from 1958 to 1961 provided a suitable basis for a substantial refinement in the definition of the positions, chloride concentrations, and rates of movement of salty water in the intermediate and deep deposits of southern Nassau County and southeastern Queens County. \r\n\r\nFilter-press, centrifugal, and dilution methods were used to extract water from cores for chloride analysis at the test-drilling sites. Chloride analysis of water extracted by these methods, chloride analyses of water from wells, and the interpretation of electric logs helped to define the chloride content of the salty water. New concepts of environmental-water head and zerovels, developed during the investigation, proved useful for defining hydraulic gradients and ratee of flow in ground water of variable density in a vertical direction and in horizontal and inclined planes, respectively. Hydraulic gradients in and between fresh and salty water were determined from water levels from data at individual and multiple-observation wells. \r\n\r\nSalty ground water occurs in southern Nassau and southeastern Queens Counties as three wedgelike extensions that project landward in unconsolidated deposits from a main body of salty water that lies seaward of the barrier beaches in Nassau County and of Jamaica Bay in Queens County. Salty water occurs not only in permeable deposits but also in the shallow and deep clay deposits. The highest chloride content of the salty ground water in the main body and the wedges is about 16,000 ppm, which is about 1,000 to 2,000 ppm less than the chloride content of ocean water. \r\n\r\nThe shallow salty water in the Pleistocene and Recent deposits is connected freely with the bays, tidal estuaries, and ocean. The intermediate wedge is found only in the southwestern part of Nassau County in the upper part of the Magothy (?) Formation, in the Jamneco Gravel, and in the overlying clay deposits. It extends from the seaward areas inland about 2 miles into Island Park. The deep wedge extends into southeastern Queens County and southern Nassau County principally in the deeper parts of the Magothy (?) Formation and in the underlying clay member of the Raritan Formation. The leading edge of the deep wedge is at the base of the Magothy (?) Formation. This edge is apparently at the shoreline east of Lido Beach and extends inland about 4 miles to Woodmere and about 7 miles to South Ozone Park. Zones of diffusion as much as 6 miles wide and about 500 feet thick were delineated in the frontal part of the salty-water wedges. These thick and broad zones of diffusion were probably formed during the past 1,000 or more years in heterogeneous unconsolidated deposits by long- and short-term changes in sea level and in fresh-water outflow to the sea and by dispersion caused by the movements of the water and its salt mass. Changes in sea level and fresh-water outflow together produced appreciable advances and recessions of the salt-water front. The chemical compositions of the diffused water in all wedges are modified to some extent by base exchange and other physical and chemical processes and also by diffusion. \r\n\r\nThe intermediate wedge of salty water is moving landward at a rate of less than 20 feet a year in the vicinity of Island Park and, thus, has moved less than 1,000 feet since 1900. The leading edge of the deep wedge has advanced landward at about 300 feet a :ear in Woodmere in southwestern Nassau County and about 160 feet a year at South Ozone Park in southeastern Queens County, principally under the influence of local withdrawals near the toe of the wedge. Between Hewlett and Lido Beach, the deep wedge is moving inland at the rate of about 10 feet a year under the influence of regional withdrawals in inland areas. Regional encroachment of the deep wedge is apparently retarded appreciably by cyclic flow, that is, by the return seaward in the upper","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1613F","usgsCitation":"Lusczynski, N., and Swarzenski, W.V., 1966, Salt-water encroachment in southern Nassau and southeastern Queens Counties, Long Island, New York: U.S. Geological Survey Water Supply Paper 1613, iv, 76 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1613F.","productDescription":"iv, 76 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138239,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1613f/report-thumb.jpg"},{"id":27807,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1613f/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27808,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1613f/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27809,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1613f/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27810,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1613f/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27811,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1613f/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27812,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1613f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66c894","contributors":{"authors":[{"text":"Lusczynski, N.J.","contributorId":10779,"corporation":false,"usgs":true,"family":"Lusczynski","given":"N.J.","affiliations":[],"preferred":false,"id":144787,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Swarzenski, Wolfgang V.","contributorId":30213,"corporation":false,"usgs":true,"family":"Swarzenski","given":"Wolfgang","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":144788,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":68531,"text":"ha212 - 1966 - Annual runoff in the conterminous United States","interactions":[],"lastModifiedDate":"2018-02-16T13:44:01","indexId":"ha212","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1966","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"212","title":"Annual runoff in the conterminous United States","docAbstract":"Runoff is that part of precipitation that appears as a flow of water in surface streams. As a source of water for modern society, it constitutes one of our basic renewable resources. This map of average annual runoff portrays the latest information on the geographic distribution of the average runoff of surface streams.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ha212","usgsCitation":"Busby, M., 1966, Annual runoff in the conterminous United States: U.S. Geological Survey Hydrologic Atlas 212, 1 Plate: 38.5 x 30.5 inches, https://doi.org/10.3133/ha212.","productDescription":"1 Plate: 38.5 x 30.5 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true},{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":186461,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":90135,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/212/plate-1.pdf","text":"Hydrologic Investigations Atlas HA-212","linkFileType":{"id":1,"text":"pdf"}}],"scale":"7500000","country":"United States","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"geometry\": {\n \"type\": \"MultiPolygon\",\n \"coordinates\": [\n [\n [\n \n [\n -94.81758,\n 49.38905\n ],\n [\n -94.64,\n 48.84\n ],\n [\n -94.32914,\n 48.67074\n ],\n [\n -93.63087,\n 48.60926\n ],\n [\n -92.61,\n 48.45\n ],\n [\n -91.64,\n 48.14\n ],\n [\n -90.83,\n 48.27\n ],\n [\n -89.6,\n 48.01\n ],\n [\n -89.27292,\n 48.01981\n ],\n [\n -88.37811,\n 48.30292\n ],\n [\n -87.43979,\n 47.94\n ],\n [\n -86.46199,\n 47.55334\n ],\n [\n -85.65236,\n 47.22022\n ],\n [\n -84.87608,\n 46.90008\n ],\n [\n -84.77924,\n 46.6371\n ],\n [\n -84.54375,\n 46.53868\n ],\n [\n -84.6049,\n 46.4396\n ],\n [\n -84.3367,\n 46.40877\n ],\n [\n -84.14212,\n 46.51223\n ],\n [\n -84.09185,\n 46.27542\n ],\n [\n -83.89077,\n 46.11693\n ],\n [\n -83.61613,\n 46.11693\n ],\n [\n -83.46955,\n 45.99469\n ],\n 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,{"id":1158,"text":"wsp1816 - 1966 - Water in the Humboldt River Valley near Winnemucca, Nevada","interactions":[],"lastModifiedDate":"2012-02-02T00:05:12","indexId":"wsp1816","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":"1816","title":"Water in the Humboldt River Valley near Winnemucca, Nevada","docAbstract":"Most of the work of the interagency Humboldt River Research Project in the Winnemucca reach of the Humboldt River valley has been completed. More than a dozen State and Federal agencies and several private organizations and individuals participated in the study. The major objective of the project, which began in 1959, is to evaluate the water resources of the entire Humboldt River basin. However, because of the large size of the basin, most of the work during the first 5 years of the project was done in the Winnemucca area. The purpose of this report is to summarize briefly and simply the information regarding the water resources of the Winnemucca area-especially the quantitative aspects of the flow system-given in previous reports of the project. \r\n\r\nThe Winnemucca reach of the Humboldt River valley, which is in north-central Nevada, is about 200 miles downstream from the headwaters of the Humboldt River and includes that part of the valley between the Comus and Rose Creek gaging stations. Average annual inflow to the storage area (the valley lowlands) in the Winnemucca reach in water years 1949-62 was about 250,000 acre-feet. Of this amount, about 68 percent was Humboldt River streamflow, as measured at the Comus gaging station, 23 percent was precipitation directly on the storage area, 6 percent was ground-water inflow, and about 3 percent was tributary streamflow. Average annual streamflow at the Rose Creek gaging station during the same period was about 155,000 acre-feet, or about 17,000 acre-feet less than that at the Comus gaging station. Nearly all the streamflow lost was consumed by evapotranspiration in the project area. Total average annual evapotranspiration loss during the period was about 115,000 acre-feet, or about 42 percent of the total average annual outflow. \r\n\r\nThe most abundant ions in the ground and surface water in the area are commonly sodium and bicarbonate. Much of the water has a dissolved-solids content that ranges from 500 to 750 parts per million; however, locally, the dissolved-solids content of the ground water is more than 5,000 parts per million. \r\n\r\nThe chemical quality of the Humboldt River, especially during periods of low flow, reflects the chemical quality of ground-water inflow from tributary areas that discharges into the river. Almost all water in the project area is moderately hard to very hard; otherwise, it is generally suitable for most uses. \r\n\r\nIncreased ground-water development, the conjunctive use of ground and surface water, and increased irrigation efficiency would probably conserve much of the water presently consumed by nonbeneficial evapotranspiration. Intensive ground-water development, especially from the highly permeable medial gravel subunit, will, however, decrease the flow of the Humboldt River to the extent that some pumpage may not be offset by a corresponding decrease in natural evapotranspiration losses. Such streamflow depletions will therefore infringe upon downstream surface-water rights. \r\n\r\nThe results of this study indicate that the Humboldt River and ground water in the unconsolidated deposits beneath and adjacent to the river in the Winnemucca area are closely related. Somewhat similar conditions probably exist elsewhere in the Humboldt River valley. Additional detailed studies are needed-both upstream and downstream from the Winnemucca area-to adequately define the flow system and the interrelations among the components of the system in the remainder of the valley. Before proceeding with additional detailed studies, however, a 1-year overall appraisal of the water resources of the basin should be considered. A major objective of this study would be to provide information that would help select the next subarea of the valley to be studied in detail and to decide which of the methods of study used in the Winnemucca area could be most effectively used in the future studies.","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1816","usgsCitation":"Cohen, P.M., 1966, Water in the Humboldt River Valley near Winnemucca, Nevada: U.S. Geological Survey Water Supply Paper 1816, vi, 69 p. :illus., maps (1 fold. col. in pocket) ;24 cm., https://doi.org/10.3133/wsp1816.","productDescription":"vi, 69 p. :illus., maps (1 fold. col. in pocket) ;24 cm.","costCenters":[],"links":[{"id":137331,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1816/report-thumb.jpg"},{"id":25965,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1816/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25966,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1816/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f6e4b07f02db5f1650","contributors":{"authors":[{"text":"Cohen, Philip M.","contributorId":67860,"corporation":false,"usgs":true,"family":"Cohen","given":"Philip","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":143276,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2192,"text":"wsp1823 - 1966 - Sedimentation and chemical quality of surface water in the Heart River drainage basin, North Dakota","interactions":[],"lastModifiedDate":"2018-03-12T15:33:39","indexId":"wsp1823","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":"1823","title":"Sedimentation and chemical quality of surface water in the Heart River drainage basin, North Dakota","docAbstract":"The Heart River drainage basin of southwestern North Dakota comprises an area of 3,365 square miles and lies within the Missouri Plateau of the Great Plains province. Streamflow of the Heart River and its tributaries during 1949-58 was directly proportional to .the drainage area. After the construction of Heart Butte Dam in 1949 and Dickinson Dam in 1950, the mean annual streamflow near Mandan was decreased an estimated 10 percent by irrigation, evaporation from the two reservoirs, and municipal use.
Processes that contribute sediment to the Heart River are mass wasting, advancement of valley heads, and sheet, lateral stream, and gully erosion. In general, glacial deposits, terraces, and bars of Quaternary age are sources of sand and larger sediment, and the rocks of Tertiary age are sources of clay, silt. and sand. The average annual suspended-sediment discharges near Mandan were estimated to be 1,300,000 tons for 1945-49 and 710,000 tons for 1970-58.
The percentage composition of ions in water of the Heart River, based on average concentrations in equivalents per million for selected ranges of streamflow, changes with flow and from station to station. During extremely low flows the water contains a large percentage of sodium and about equal percentages of bicarbonate and .sulfate, and during extremely high flows the water contains a large percentage of calcium plus magnesium and bicarbonate. The concentrations, in parts per million, of most of the ions vary inversely with flow.
The water in the reservoirs--Edward Arthur Patterson Lake and Lake Tschida--during normal or above-normal runoff is of suitable quality for public use. Generally, because of medium or high salinity hazards, the successful long-term use of Heart River water for irrigation will depend on a moderate amount of leaching, adequate drainage, ,and the growing of crops that have moderate or good salt tolerance.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1823","usgsCitation":"Maderak, M.L., 1966, Sedimentation and chemical quality of surface water in the Heart River drainage basin, North Dakota: U.S. Geological Survey Water Supply Paper 1823, Report: v, 42 p.; Plate: 18.48 x 12.99 inches, https://doi.org/10.3133/wsp1823.","productDescription":"Report: v, 42 p.; Plate: 18.48 x 12.99 inches","costCenters":[{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":247119,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1823/plate-1.pdf","size":"1078","linkFileType":{"id":1,"text":"pdf"}},{"id":138275,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1823/report-thumb.jpg"},{"id":27833,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1823/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fbcd0","contributors":{"authors":[{"text":"Maderak, Marion L.","contributorId":103248,"corporation":false,"usgs":true,"family":"Maderak","given":"Marion","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":144801,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":22776,"text":"ofr6619 - 1966 - Progress report on analog model construction, Orange County, California","interactions":[],"lastModifiedDate":"2013-05-22T15:03:30","indexId":"ofr6619","displayToPublicDate":"1994-01-01T00:00:00","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":"66-19","title":"Progress report on analog model construction, Orange County, California","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey, Water Resources Division,","doi":"10.3133/ofr6619","issn":"0094-9140","usgsCitation":"Cordes, E.H., Wall, J.R., and Moreland, J.A., 1966, Progress report on analog model construction, Orange County, California: U.S. Geological Survey Open-File Report 66-19, 49 p. ill., maps ;27 cm., https://doi.org/10.3133/ofr6619.","productDescription":"49 p. ill., maps ;27 cm.","costCenters":[],"links":[{"id":155915,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1966/0019/report-thumb.jpg"},{"id":272567,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1966/0019/report.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9be4b07f02db65def1","contributors":{"authors":[{"text":"Cordes, E. H.","contributorId":49002,"corporation":false,"usgs":true,"family":"Cordes","given":"E.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":188857,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wall, J. R.","contributorId":59863,"corporation":false,"usgs":true,"family":"Wall","given":"J.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":188858,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Moreland, Joe A.","contributorId":48171,"corporation":false,"usgs":true,"family":"Moreland","given":"Joe","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":188856,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1126,"text":"wsp1663E - 1966 - Hydrology of the Upper Capibaribe Basin, Pernambuco, Brazil - A reconnaissance in an Area of Crystalline Rocks","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1663E","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":"1663","chapter":"E","title":"Hydrology of the Upper Capibaribe Basin, Pernambuco, Brazil - A reconnaissance in an Area of Crystalline Rocks","docAbstract":"The upper Capibaribe basin is the western three-fourths, approximately, of the valley of the river that empties into the Atlantic Ocean at Recife, the capital of the State of Pernambuco, Brazil. It is the part of the drainage basin that is within the Drought Polygon of northeast Brazil, and it totals about 5,400 square kilometers. It receives relatively abundant precipitation in terms of the annual average, yet is regarded as hot subhumid to semiarid because the precipitation is uneven from year to year and place to place. The dependable water supply, therefore, is small. \r\n\r\nThe basin has water, which could be put to better use than at present, but the opportunities for augmenting the usable supply are not great. The streams are intermittent and therefore cannot be expected to fill surface reservoirs and to keep them filled. The ground-water reservoirs have small capacity--quickly filled and quickly drained. \r\n\r\nA rough estimate based on the records for 1964 suggests that, of 4,700 million cubic meters of precipitation in the upper Capibaribe basin, 2,700 million cubic meters (57 percent) left the basin as runoff and 2,000 million cubic meters {43 percent) went into underground storage or was evaporated or transpired. The bedrock of the upper Capibaribe basin is composed of granite, gneiss, schist, and other varieties of crystalline rocks, which have only insignificant primary permeability. They are permeable mainly where fractured. The principal fracture zones, fortunately, are in the valleys, where water accumulates and can feed into them, but the volume of fractured rock is small in relation to the basin as a whole. A well in a large water-filled fracture zone may yield up to 20,000 liters per hour, but the average well yields less than one-fourth this amount, and some wells yield none. \r\n\r\nThe saprolite, or weathered rock, is many meters thick at some places especially in the eastern half of the upper Capibaribe basin. It contains water locally, but ordinarily will yield only small quantities to wells. The alluvium probably is the most productive aquifer in the basin, but is limited to narrow bands along the rivers that generally are no more than a few hundred meters wide and 5 meters thick. The alluvium contains variable amounts of silty sand capable of yielding small to moderate quantities of water to wells. Wells driven or dug into the alluvium could solve many small water problems. The chemical quality of the water in the upper Capibaribe basin ranges from good to bad and generally presents a major problem that cannot be solved solely by applying geological criteria. Mineralized water is widespread in the area, both in streams and underground, and .the choice of aquifers is small. All known aquifers contain, at one place or another, water that is mineralized, leaving no alternative for a natural supply of good-quality water. \r\n\r\nAlthough much of the available water is unsatisfactory for human consumption, it is generally acceptable for animals and therefore meets one of the principal water needs. Some of the ground water could be made potable by diluting it with rainwater, which could be collected during rainy seasons and temporarily stored in cisterns or reservoirs.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1663E","usgsCitation":"Chada Filho, L.G., Dias Pessoa, M., and Sinclair, W.C., 1966, Hydrology of the Upper Capibaribe Basin, Pernambuco, Brazil - A reconnaissance in an Area of Crystalline Rocks: U.S. Geological Survey Water Supply Paper 1663, iv, 44 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1663E.","productDescription":"iv, 44 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138097,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1663e/report-thumb.jpg"},{"id":25902,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1663e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25903,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1663e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ee4b07f02db5fdb3f","contributors":{"authors":[{"text":"Chada Filho, Luiz Goncalves","contributorId":48161,"corporation":false,"usgs":true,"family":"Chada Filho","given":"Luiz","email":"","middleInitial":"Goncalves","affiliations":[],"preferred":false,"id":143220,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dias Pessoa, Mario","contributorId":10778,"corporation":false,"usgs":true,"family":"Dias Pessoa","given":"Mario","email":"","affiliations":[],"preferred":false,"id":143218,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sinclair, William C.","contributorId":14798,"corporation":false,"usgs":true,"family":"Sinclair","given":"William","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":143219,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"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":2637,"text":"wsp1826 - 1966 - Water resources of the Ipswich River basin, Massachusetts","interactions":[],"lastModifiedDate":"2012-02-02T00:05:28","indexId":"wsp1826","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":"1826","title":"Water resources of the Ipswich River basin, Massachusetts","docAbstract":"Water resources of the Ipswich River basin are at resent {1960) used principally for municipal supply to about 379,000 person's in 16 towns and cities in or near the river basin. By the year 2000 municipal use of water in this region will probably be more than twice the current use, and subsidiary uses of water, especially for recreation, also will have increased greatly. To meet the projected needs, annual pumpage of water from the Ipswich River could be increased from current maximums of about 12 mgd (million galleons a day) to about 45 mgd without reducing average base flows in the river, provided that the increased withdrawals would be restricted to periods of high streamflow. \r\n\r\nIn addition, considerably more pumpage could be derived from streamflow by utilizing base-flow discharge; however, the magnitude of such use could be determined only in relation to factors such as concurrent ground-water use, the disposal of waste water, and the amount of streamflow required to dilute the pollution load to acceptable levels. Under present conditions, little or no increase in diversion of streamflow would be warranted in the upstream rafts of the basin during the summer and early fall of each year, and only a moderate increase could be made in the lower reaches of the stream during the same period. \r\n\r\nAnnual rainfall in the basin averages about 42.5 inches, and represents the water initially available for use. Of this amount, an average of about 20.5 inches is returned to the a.tmosphere by evapotranspiration. The remainder, about 22 inches, runs off as streamflow in the Ipswich River or is diverted from the basin by pumpage. The average annual stream runoff, amounting to about 47 billion gallons, is a measure of the water actually available for man's use. The amounts of water used by municipalities in recent years are less than 10 percent of the available supply. \r\n\r\nLarge supplies of ground water may be obtained under water-table conditions from the stratified glacial drift that forms .the principal ground-water reservoir of the basin. Stratified drift deposits fill valleys in about 31 percent of the basin. Thicknesses of the deposits are generally less than 50 feet, but at places may be as great as 200 feet. \r\n\r\nBetween 1931 and 1960 recoverable annual recharge to stratified drift aquifers averaged about 10 inches, equal to 42 mgd. The least possible recharge during any of these years was probably more than 41inches, or 25 mgd. Therefore, ground-water withdrawals from the basin could be sustained at a rate at least five times greater than the 1960 rate of 4.9 mgd. In the lower Ipswich basin. withdrawal of ground water could be sustained at a rate eight or nine times greater than the 1960 rate of 1.86 mgd. There are 1 or more favorable sites for further exploration for ground water in each of the 10 communities that occupy the major part of the river ,basin. Small but reliable supplies of ground water for domestic use may be withdrawn from bedrock almost anywhere it. the basin. Ground-water levels show no long-term trend since 1939, and although large fluctuations in water levels occur during each year, the ground-water reservoir at most places in the Ipswich River basin is replenished annually to its full capacity. During parts of most years potential recharge is unable to enter the already-saturated ground-water reservoirs, and most of this 'rejected recharge' enters streams as surface runoff. \r\n\r\nThe chemical quality of both ground and surface water is generally satisfactory for most uses, although excessive concentrations of iron and manganese occur locally, and at places the hardness of the water is objectionable. \r\n\r\nThe surface- and ground-water resources of the basin are closely related. Because most areas favorable for further development of ground water are adjacent to stream channels, large increases in the withdrawal of ground water during low-flow periods will result in reductions of streamflow. The magnitude of t","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1826","usgsCitation":"Sammel, E.A., Baker, J.A., and Brackley, R.A., 1966, Water resources of the Ipswich River basin, Massachusetts: U.S. Geological Survey Water Supply Paper 1826, viii, 83 p. :illus., maps (2 fold. col. in pocket) ;24 cm., https://doi.org/10.3133/wsp1826.","productDescription":"viii, 83 p. :illus., maps (2 fold. col. in pocket) ;24 cm.","costCenters":[],"links":[{"id":138727,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1826/report-thumb.jpg"},{"id":28954,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1826/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28955,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1826/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28956,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1826/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e7397","contributors":{"authors":[{"text":"Sammel, Edward A.","contributorId":78320,"corporation":false,"usgs":true,"family":"Sammel","given":"Edward","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":145540,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Baker, John Augustus","contributorId":48159,"corporation":false,"usgs":true,"family":"Baker","given":"John","email":"","middleInitial":"Augustus","affiliations":[],"preferred":false,"id":145538,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brackley, Richard A.","contributorId":61792,"corporation":false,"usgs":true,"family":"Brackley","given":"Richard","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":145539,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":52540,"text":"ofr6643 - 1966 - Extent and frequency of floods on Delaware River in vicinity of Belvidere, New Jersey","interactions":[{"subject":{"id":52540,"text":"ofr6643 - 1966 - Extent and frequency of floods on Delaware River in vicinity of Belvidere, New Jersey","indexId":"ofr6643","publicationYear":"1966","noYear":false,"title":"Extent and frequency of floods on Delaware River in vicinity of Belvidere, New Jersey"},"predicate":"SUPERSEDED_BY","object":{"id":68431,"text":"ha263 - 1967 - Floods on Delaware River in the vicinity of Belvidere, New Jersey","indexId":"ha263","publicationYear":"1967","noYear":false,"title":"Floods on Delaware River in the vicinity of Belvidere, New Jersey"},"id":1}],"supersededBy":{"id":68431,"text":"ha263 - 1967 - Floods on Delaware River in the vicinity of Belvidere, New Jersey","indexId":"ha263","publicationYear":"1967","noYear":false,"title":"Floods on Delaware River in the vicinity of Belvidere, New Jersey"},"lastModifiedDate":"2016-10-21T10:51:04","indexId":"ofr6643","displayToPublicDate":"1994-01-01T00:00:00","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":"66-43","title":"Extent and frequency of floods on Delaware River in vicinity of Belvidere, New Jersey","docAbstract":"A stream overflowing its banks is a natural phenomenon. This natural phenomenon of flooding has occurred on the Delaware River in the past and will occur in the future. T' o resulting inundation of large areas can cause property damage, business losses and possible loss of life, and may result in emergency costs for protection, rescue, and salvage work. For optimum development of the river valley consistent with the flood risk, an evaluation of flood conditions is necessary. Basic data and the interpretation of the data on the regimen of the streams, particularly the magnitude of floods to be expected, the frequency of their occurrence, and the areas inundated, are essential for planning and development of flood-prone areas.
This report presents information relative to the extent, depth, and frequency of floods on the Delaware River and its tributaries in the vicinity of Belvidere, N.J. Flooding on the tributaries detailed in the report pertains only to the effect of backwater from the Delaware River. Data are presented for several past floods with emphasis given to the floods of August 19, 1955 and May 24, 1942. In addition, information is given for a hypothetical flood based on the flood of August 19, 1955 modified by completed (since 1955) and planned flood-control works.
By use of relations presented in this report the extent, depth, and frequency of flooding can be estimated for any site along the reach of the Delaware River under study. Flood data and the evaluation of the data are presented so that local and regional agencies, organizations, and individuals may have a technical basis for making decisions on the use of flood-prone areas. The Delaware River Basin Commission and the U.S. Geological Survey regard this program of flood-plain inundation studies as a positive step toward flood-damage prevention. Flood-plain inundation studies, when followed by appropriate land-use regulations, are a valuable and economical supplement to physical works for flood control, such as dams and levees. Both physical works and flood-plain regulations are included in the comprehensive plans for development of the Delaware River basin.
Recommendations for land use, or suggestions for limitations of land use, are not made herein. Other reports on recommended general use and regulation of land in flood-prone areas are available (Dola, 1961; White, 1961; American Society of Civil Engineers Task Force on Flood Plain Regulations, 1962; and Goddard, 1963). The primary responsibility for planning for the optimum land use in the flood plain and the implementation of flood-plain zoning or other regulations to achieve such optimum use rest with the state and local interests. The preparation of this report was undertaken after consultation with representatives of the Lehigh-Northampton Counties, Pennsylvania, Joint Planning Commission and the Warren County, New Jersey, Regional Planning Board and after both had demonstrated their need for flood-plain information and their willingness to consider flood-plain regulations.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Trenton, New Jersey","doi":"10.3133/ofr6643","usgsCitation":"Farlekas, G.M., 1966, Extent and frequency of floods on Delaware River in vicinity of Belvidere, New Jersey: U.S. Geological Survey Open-File Report 66-43, Report: vii, 44 p.; Plate: 31.15 x 28.59 inches, https://doi.org/10.3133/ofr6643.","productDescription":"Report: vii, 44 p.; Plate: 31.15 x 28.59 inches","costCenters":[],"links":[{"id":173957,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr6643.PNG"},{"id":330308,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1966/0043/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":330309,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1966/0043/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New Jersey","city":"Belvidere","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.21034240722656,\n 40.74907763805906\n ],\n [\n -75.21034240722656,\n 40.88029480552824\n ],\n [\n -74.99473571777344,\n 40.88029480552824\n ],\n [\n -74.99473571777344,\n 40.74907763805906\n ],\n [\n -75.21034240722656,\n 40.74907763805906\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a06e4b07f02db5f8b2f","contributors":{"authors":[{"text":"Farlekas, George M.","contributorId":44963,"corporation":false,"usgs":true,"family":"Farlekas","given":"George","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":245518,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":5711,"text":"pp498A - 1966 - Hydrochemical facies and ground-water flow patterns in northern part of Atlantic Coastal Plain","interactions":[],"lastModifiedDate":"2017-06-05T21:55:49","indexId":"pp498A","displayToPublicDate":"1991-01-01T00:00:00","publicationYear":"1966","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":"498","chapter":"A","title":"Hydrochemical facies and ground-water flow patterns in northern part of Atlantic Coastal Plain","docAbstract":"The part of the Atlantic Coastal Plain that extends from New Jersey through Virginia was selected as a suitable field model in which to study the relationships between geology, hydrology, and chemical character of ground water. The ground-water flow pattern is the principal hydrologic control on the chemical character of the water. Within the Coastal Plain sediments, the proportions of clay, glauconitic sand, and calcareous material are the principal lithologic controls over the chemistry of the water.
\nA subsurface body of salt water extends from southern New Jersey through southern Virginia and occupies the deposits deeper than about 500 feet below land surface in the eastern part of the Coastal Plain. The position of its top is determined by the relative head, which in turn is influenced by topography, drainage density, and the thickness and permeability of the Coastal Plain sediments.
\nHydrochemical facies is a term used in this paper to denote the diagnostic chemical aspect of ground-water solutions occurring in hydrologic systems. The facies reflect the response of chemical processes operating within the lithologic framework and also the pattern of flow of the water. The distribution of these facies is shown in trilinear diagrams and isometric fence diagrams and on maps showing isopleths of chemical constituents within certain formations. The occurrence of the various facies within one formation or within a group of formations of uniform mineralogy indicates that the ground-water flow through the aquifer system modifies the distribution of the facies.
\nFlow patterns of fresh ground water shown on maps and in cross sections have been deduced from available water-level data. These patterns are controlled by the distribution of the higher landmasses and by the depth to either bedrock or to the salt-water interface. The mapping of hydrochemical facies shows that at shallow depths within the Coastal Plain (less than about 200 ft) the calcium-magnesium cation facies generally predominates. The bicarbonate anion facies occurs within more of the shallow Coastal Plain sediments than does the sulfate or the chloride facies. In deeper formations, the sodium chloride character predominates. The lower dissolved-solids content of the ground water in New Jersey indicates less upward vertical leakage than in Maryland and Virginia, where the shallow formations contain solutions of higher concentration.
","largerWorkTitle":"Hydrology of aquifer systems","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp498A","usgsCitation":"Back, W., 1966, Hydrochemical facies and ground-water flow patterns in northern part of Atlantic Coastal Plain: U.S. Geological Survey Professional Paper 498, Report: iv, 42 p.; 1 Plate: 54.00 x 41.50 inches, https://doi.org/10.3133/pp498A.","productDescription":"Report: iv, 42 p.; 1 Plate: 54.00 x 41.50 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":32282,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0498a/plate-1.pdf","text":"Plate 1","size":"7.25 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"},{"id":118160,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0498a/report-thumb.jpg"},{"id":104479,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4513.htm","linkFileType":{"id":5,"text":"html"},"description":"4513"},{"id":32283,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0498a/report.pdf","text":"Report","size":"5.06 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Delaware, Maryland, New Jersey, Pennsylvania, Virginia","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.03662109375,\n 41.50857729743935\n ],\n [\n -73.80615234375,\n 40.94671366508002\n ],\n [\n -73.89404296875,\n 40.41349604970198\n ],\n [\n -74.1357421875,\n 39.487084981687495\n ],\n [\n -74.6630859375,\n 38.8225909761771\n ],\n [\n -75.234375,\n 37.70120736474139\n ],\n [\n -75.6298828125,\n 37.00255267215955\n ],\n [\n -75.69580078125,\n 36.527294814546245\n ],\n [\n -80.33203125,\n 36.63316209558658\n ],\n [\n -79.16748046874999,\n 37.56199695314352\n ],\n [\n -78.046875,\n 38.75408327579141\n ],\n [\n -77.62939453125,\n 39.52099229357195\n ],\n [\n -77.05810546875,\n 40.094882122321174\n ],\n [\n -76.31103515625,\n 40.697299008636755\n ],\n [\n -75.6298828125,\n 41.36031866306708\n ],\n [\n -75.03662109375,\n 41.50857729743935\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a50e4b07f02db628ed5","contributors":{"authors":[{"text":"Back, William","contributorId":59007,"corporation":false,"usgs":true,"family":"Back","given":"William","email":"","affiliations":[],"preferred":false,"id":151470,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70112257,"text":"70112257 - 1966 - Ultraviolet investigations for lunar missions","interactions":[],"lastModifiedDate":"2017-03-27T13:42:54","indexId":"70112257","displayToPublicDate":"1990-06-12T10:10:00","publicationYear":"1966","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":653,"text":"Advances in Astronautical Sciences","active":true,"publicationSubtype":{"id":10}},"title":"Ultraviolet investigations for lunar missions","docAbstract":"Preliminary field tests of an active ultraviolet imaging system have shown that it is possible to produce linages of the terrain from distances as great as 75 feet by means of reflected ultraviolet light at wavelengths longer than 3300 A. Minerals that luminesce when exposed to ultraviolet energy have been detected from distances as great as 200 feet. With appropriate design modifications, it may be possible to utilize a similar system in detecting luminescing minerals from greater distances. Also, with a similar system and appropriate auxiliary equipment such as image intensifiers, it may be possible to discriminate between naturally occurring materials on the basis of reflected ultraviolet energy at wavelengths shorter than 3000 A. In this part of the spectrum image contrast for some rock types may exceed that from visible light. Information from these and related ultraviolet spectralanalysis studies may be useful in evaluating data obtained from passive ultraviolet systems in lunar orbit as well as from active systems on the lunar surface.
","language":"English","publisher":"American Astronautical Society","publisherLocation":"Washington, D.C.","usgsCitation":"Hemphill, W.R., Fischer, W., and Dornbach, J., 1966, Ultraviolet investigations for lunar missions: Advances in Astronautical Sciences, v. 20, p. 397-415.","productDescription":"21 p.","startPage":"397","endPage":"415","numberOfPages":"21","costCenters":[{"id":222,"text":"Earth Resources Observation and Science (EROS) Center","active":true,"usgs":true}],"links":[{"id":288449,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"20","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"539acc5be4b0e83db6d09044","contributors":{"editors":[{"text":"Narin, Francis","contributorId":111682,"corporation":false,"usgs":true,"family":"Narin","given":"Francis","email":"","affiliations":[],"preferred":false,"id":509858,"contributorType":{"id":2,"text":"Editors"},"rank":1}],"authors":[{"text":"Hemphill, William R.","contributorId":21970,"corporation":false,"usgs":true,"family":"Hemphill","given":"William","email":"","middleInitial":"R.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":494584,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fischer, William A.","contributorId":47787,"corporation":false,"usgs":true,"family":"Fischer","given":"William A.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":494586,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dornbach, J.E.","contributorId":30547,"corporation":false,"usgs":true,"family":"Dornbach","given":"J.E.","email":"","affiliations":[],"preferred":false,"id":494585,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70207387,"text":"70207387 - 1966 - Jura tectonics as a décollement","interactions":[],"lastModifiedDate":"2019-12-18T14:11:54","indexId":"70207387","displayToPublicDate":"1966-12-31T14:08:51","publicationYear":"1966","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":"Jura tectonics as a décollement","docAbstract":"For many years the structure of the Jura Mountains was interpreted as a décollement whose origin was related to the Alps; in recent years, however, this mode of origin has been questioned. Most of the alternative explanations recognize a décollement to some extent, but attribute it to movement of the basement beneath. Surface and subsurface data are here reviewed to show that the Jura deformation was produced in a gliding sheet, in which the forces of gravity and inertia were generated within the total moving mass. Features of the folded Jura which support the décollement hypothesis are: (1) Nowhere are rocks older than Middle Triassic exposed, which strongly suggests that the folding does not extend to the older rocks. (2) Subsurface data in the Lons-le-Saunier region clearly show that the external border of the Jura has moved northwestward over the eastern margin of the Bresse Basin. (3) Lower Jurassic rocks rest on Upper Jurassic along a horizontal fault 1234 m deep in the Risoux well near the middle of the Jura. (4) The tabular areas, with their absence of folds, are expectable in a décollement. (5) High-angle tear faults, interpreted as not extending into the basement, are normal features of a décollement sheet. A continuous décollement around the southwestern end of the Swiss Plain can reasonably be inferred, connecting the internal Jura, the Salève, and the Subalpine folds as part of the décollement mass. Elsewhere, the internal border of décollement extends southeastward into the Molasse basin for an unknown distance and probably underlies the entire basin; if it does, a causal relation to the Alps is indicated. © 1966, The Geological Society of America, Inc.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1966)77[1265:JTAAD]2.0.CO;2","issn":" 00167606","usgsCitation":"Pierce, W.G., 1966, Jura tectonics as a décollement: Geological Society of America Bulletin, v. 77, no. 11, p. 1265-1276, https://doi.org/10.1130/0016-7606(1966)77[1265:JTAAD]2.0.CO;2.","productDescription":"12 p. ","startPage":"1265","endPage":"1276","costCenters":[],"links":[{"id":370427,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"77","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Pierce, W. G.","contributorId":11267,"corporation":false,"usgs":true,"family":"Pierce","given":"W.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":777882,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70217836,"text":"70217836 - 1966 - Field continuation and the step model in aeromagnetic interpretation","interactions":[],"lastModifiedDate":"2021-02-05T17:17:00.099885","indexId":"70217836","displayToPublicDate":"1966-12-31T11:15:31","publicationYear":"1966","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1806,"text":"Geophysical Prospecting","active":true,"publicationSubtype":{"id":10}},"title":"Field continuation and the step model in aeromagnetic interpretation","docAbstract":"Downward continuation of the field in the neighborhood of a singularity of a magnetic anomaly is used to render the anomaly more two‐dimensional, to make the bottom of the causal body more remote, and to obtain an auxiliary function, φ (O, z), by means of which the anomaly may be interpreted in terms of an equivalent vertical contact or step model. The concept of “apparent depth” is introduced and used in studying depth extent and susceptibility. The methods are illustrated with theoretical and practical examples.
","language":"English","publisher":"Wiley","doi":"10.1111/j.1365-2478.1966.tb02252.x","usgsCitation":"Henderson, R., 1966, Field continuation and the step model in aeromagnetic interpretation: Geophysical Prospecting, v. 14, no. 4, p. 528-546, https://doi.org/10.1111/j.1365-2478.1966.tb02252.x.","productDescription":"19 p.","startPage":"528","endPage":"546","costCenters":[],"links":[{"id":383053,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"14","issue":"4","noUsgsAuthors":false,"publicationDate":"2006-04-27","publicationStatus":"PW","contributors":{"authors":[{"text":"Henderson, Roland G.","contributorId":65139,"corporation":false,"usgs":true,"family":"Henderson","given":"Roland G.","affiliations":[],"preferred":false,"id":809868,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70219934,"text":"70219934 - 1966 - Tropical lakes, copropel, and oil shale","interactions":[],"lastModifiedDate":"2021-04-16T12:23:10.823743","indexId":"70219934","displayToPublicDate":"1966-12-31T07:19:20","publicationYear":"1966","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Tropical lakes, copropel, and oil shale","docAbstract":"During a long-continued study of the lacustrine beds of the Eocene Green River Formation, I have tried to interpret past events from observation of present-day processes. After a search of some 40 years, four lakes have been found that are producing a kind of organic ooze judged to be a modern analogue of the precursors of rich oil shale. Two of the lakes are in central Africa and two are in Florida. All four are shallow. The ooze in all four is predominantly algal, entirely in the form of minute fecal pellets, and does not decay in warm, wet, oxidizing environments.
Several of the most unusual, mummified microorganisms found in the oil shale of the Green River are illustrated as testament to the inference that the Eocene organic oozes also were resistant to decay.
Studies to determine why these algal oozes do not decay are in progress, but as yet no satisfactory explanation is available. The ooze from Mud Lake, Florida, contains very few living bacteria but a great many bacterial spores, suggesting some active inhibitor. Gentle and slow anaerobic decay takes place in the ooze 1 foot or more below the mud-water interface.
The algal ooze accumulates slowly. That at a depth of 3 feet below the mud-water interface has a C14 age of 2280 ± 200 years. If compacted, this 3-foot layer would amount to a layer only about 0.5 inch thick.
The air-dried algal mud (from Mud Lake) looks much like oil shale and has a C-H ratio essentially like that of the organic matter in oil shale. The oxygen of the mud, however, is roughly 5 times as high as in oil shale. The calorific value of dried Mud Lake algal ooze is about 6600 cal/g, whereas the organic matter from Green River oil shale averages about 9500 cal/g.
Analyses show that the dried algal ooze from Mud Lake contains small quantities of higher fatty acids (C12–C34), with C16 being dominant. It also contains some unsaturated fatty acids and about 0.3 per cent of n-alkanes, predominantly odd carbons, with C29 being dominant. A few qualitative analyses show that carotenoid pigments and terpenes are also present.
A possible source of hydrocarbons is the long branched side chain of the chlorophyll molecule. Small crustaceans liberate this in the form of phytol, which, by dehydration, can go over into a series of saturated and unsaturated hydrocarbons, including phytanc and pristane, both of which are common in Green River oil shale. Search for other precursors of hydrocarbons continues.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1966)77[1333:TLCAOS]2.0.CO;2","usgsCitation":"Bradley, W., 1966, Tropical lakes, copropel, and oil shale: GSA Bulletin, v. 77, no. 12, p. 1333-1337, https://doi.org/10.1130/0016-7606(1966)77[1333:TLCAOS]2.0.CO;2.","productDescription":"5 p.","startPage":"1333","endPage":"1337","costCenters":[],"links":[{"id":385151,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"77","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Bradley, W.H.","contributorId":220222,"corporation":false,"usgs":false,"family":"Bradley","given":"W.H.","email":"","affiliations":[],"preferred":false,"id":814404,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221299,"text":"70221299 - 1966 - Magnetic data on the structure of the central Arctic Region","interactions":[],"lastModifiedDate":"2021-06-09T13:34:02.726064","indexId":"70221299","displayToPublicDate":"1966-12-01T08:29:47","publicationYear":"1966","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":"Magnetic data on the structure of the central Arctic Region","docAbstract":"A study of 23,000 miles of total intensity aeromagnetic profiles in the central Arctic has been made by the U. S. Geological Survey and the U. S. Coast and Geodetic Survey. The profiles were flown at 20,000 feet above sea level and cover approximately 1,350,000 square miles of the Arctic Ocean between the North Pole and the North American continent. When the profiles are smoothed to remove crustal anomalies, the resulting contoured values differ from the U. S. Hydrographic Office Chart 1703 N for 1955 corrected to 1951 by as much as 2000 gammas in the northern part of the Arctic Archipelago. A nondipole regional focus east of Greenland has decreased in amplitude but has changed very little in position since 1907.5. There is a profound difference in the magnetic characteristics of the rocks on either side of the underwater Lomonosov Ridge across the Arctic Ocean. In the Eurasian Basin the high-altitude profiles are relatively smooth or show only minor anomalies, but on the North American side of the ridge there is a large area of closely spaced, high-amplitude anomalies which has been designated the Central Magnetic Zone. Although the anomaly trends parallel the Alpha Rise, this zone is far more extensive, including nearly half of the Canadian Basin on one side and probably all the Central Arctic Basin on the other side of the rise. The Lomonosov Ridge is marked by a persistent anomaly of moderate size that indicates the presence of magnetic material in the ridge. Probable block-fault structures along the flanks of the Alpha Rise are associated with blocklike magnetic anomalies of comparable widths. A characteristic magnetic pattern occurs over an area of jagged bottom topography in the Eurasian Basin. A similar magnetic pattern over part of the Lena Trough may indicate another area of jagged topography. The belt of epicenters associated with the Mid-Atlantic Ridge continues through this rugged part of the Eurasian Basin, but the absence of the typical high magnetic anomaly makes it doubtful that the mid-oceanic ridge extends through this part of the Arctic. Magnetic data indicate that the thick sections of sedimentary rocks in the Paleozoic geosynclinal belts of northern Ellesmere Island and northern Greenland continue out under the adjacent continental shelves north of Greenland, west of the Arctic Archipelago, north of the part of Alaska east of Barrow, and under part of the Chukchi Shelf, and that they make up the bulk of the Nansen Swell off Spitsbergen. Thick sedimentary fill is indicated in the magnetically flat areas of the Eurasian Basin next to the Lomonosov Ridge and in the southern part of the Canadian Basin. The magnetic profiles on the Eurasian side of the Lomonosov Ridge closely resemble typical magnetic profiles over both Atlantic and Pacific oceans, where as the profiles of the Central Magnetic Zone on the North American side of the Lomonosov Ridge are completely unlike the oceanic data and show a striking similarity to typical profiles over the Precambrian rocks of the Canadian Shield and its buried equivalent under the Central Stable Region of the United States. Therefore, it is concluded that the Arctic region consists of a probable oceanic area on the Eurasian side and a basin formed by downdropped continental rocks, presumably a Precambrian complex similar to that of the Canadian Shield, on the North American side of the ridge.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1966)77[619:MDOTSO]2.0.CO;2","usgsCitation":"King, E.R., Zietz, I., and Alldredge, L., 1966, Magnetic data on the structure of the central Arctic Region: Geological Society of America Bulletin, v. 77, no. 6, p. 619-646, https://doi.org/10.1130/0016-7606(1966)77[619:MDOTSO]2.0.CO;2.","productDescription":"28 p.","startPage":"619","endPage":"646","costCenters":[],"links":[{"id":386345,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"otherGeospatial":"Arctic Circle","volume":"77","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"King, E. R.","contributorId":93482,"corporation":false,"usgs":true,"family":"King","given":"E.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":817268,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zietz, I.","contributorId":59937,"corporation":false,"usgs":true,"family":"Zietz","given":"I.","email":"","affiliations":[],"preferred":false,"id":817269,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Alldredge, L.R.","contributorId":53457,"corporation":false,"usgs":true,"family":"Alldredge","given":"L.R.","email":"","affiliations":[],"preferred":false,"id":817270,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70221298,"text":"70221298 - 1966 - Geochronology of the St. Kevin granite and neighboring precambrian rocks, northern Sawatch Range, Colorado","interactions":[],"lastModifiedDate":"2021-06-09T13:28:44.469071","indexId":"70221298","displayToPublicDate":"1966-12-01T08:22:20","publicationYear":"1966","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":"Geochronology of the St. Kevin granite and neighboring precambrian rocks, northern Sawatch Range, Colorado","docAbstract":"Radiometric ages have been measured on rocks of a crystalline terrane that includes ancient gneisses and migmatites, two granitic batholiths (St. Kevin Granite and granite of Cross Creek), and various minor intrusive rocks. A whole-rock Rb-Sr isochron age on the St. Kevin Granite establishes it as 1390 ± 60 m.y. old. Mineral ages on the St. Kevin and numerous other rocks are either about the same as the St. Kevin whole-rock age or younger by as much as 200 m.y., even where the relative age is known to be older. Some minor Precambrian intrusive masses that are probably younger than St. Kevin Granite yield mica ages within analytical error of the St. Kevin age, indicating that these rocks can be younger than the granite by only a few tens of millions of years. The mica ages, both Rb-Sr and K-Ar, are thought to be minimal, but a K-Ar age of 2020 m.y. on horn-blende probably reflects excess argon. Mica ages from all rocks known geologically to be older than St. Kevin Granite are low and are interpreted as heating ages reflecting intrusion of the granite, in some cases modified further by heating during Laramide time. In this area, Precambrian intrusion and deformation had largely ended by 1200 or 1300 m.y. ago. Plutonism, represented here by the St. Kevin Granite and elsewhere by the Silver Plume and other granites, probably accounts for the numerous mineral ages of about 1300 m.y. previously reported from Colorado although weak regional metamorphism may also have been a factor.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1966)77[1109:GOTSKG]2.0.CO;2","usgsCitation":"Pearson, R.C., Hedge, C., Thomas, H., and Stern, T., 1966, Geochronology of the St. Kevin granite and neighboring precambrian rocks, northern Sawatch Range, Colorado: Geological Society of America Bulletin, v. 77, no. 10, p. 1109-1120, https://doi.org/10.1130/0016-7606(1966)77[1109:GOTSKG]2.0.CO;2.","productDescription":"12 p.","startPage":"1109","endPage":"1120","costCenters":[],"links":[{"id":386344,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Coloradao","otherGeospatial":"Sawatch Range","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -107.501220703125,\n 38.758366935612784\n ],\n [\n -106.32568359375,\n 38.758366935612784\n ],\n [\n -106.32568359375,\n 39.47436547486121\n ],\n [\n -107.501220703125,\n 39.47436547486121\n ],\n [\n -107.501220703125,\n 38.758366935612784\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"77","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Pearson, R. C.","contributorId":30978,"corporation":false,"usgs":true,"family":"Pearson","given":"R.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":817264,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hedge, C. E.","contributorId":73611,"corporation":false,"usgs":true,"family":"Hedge","given":"C. E.","affiliations":[],"preferred":false,"id":817265,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Thomas, H.H.","contributorId":67530,"corporation":false,"usgs":true,"family":"Thomas","given":"H.H.","email":"","affiliations":[],"preferred":false,"id":817266,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Stern, T.W.","contributorId":258270,"corporation":false,"usgs":false,"family":"Stern","given":"T.W.","email":"","affiliations":[],"preferred":false,"id":817267,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70221251,"text":"70221251 - 1966 - Use of analog model to predict streamflow depletion, big and little Blue River basin, Nebraska","interactions":[],"lastModifiedDate":"2021-06-08T16:50:02.742396","indexId":"70221251","displayToPublicDate":"1966-10-01T11:44:40","publicationYear":"1966","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Use of analog model to predict streamflow depletion, big and little Blue River basin, Nebraska","docAbstract":"The States of Nebraska and Kansas are negotiating a compact for apportionment of the waters of the Big and Little Blue Rivers. So that the negotiating officials could allocate the water equitably, the amount of streamflow depletion caused by ground‐water withdrawals upgradient from the State line needed to be determined. At the request of the Nebraska officials, the U. S. Geological Survey constructed an electric analog model which could be used to determine the amount of streamflow depletion expected to occur in the next 60 years. The model simulates hydraulic conditions in an area of 7,400 square miles which includes the entire area drained by the Big and Little Blue Rivers in Nebraska. The trans‐missibility of the aquifer (Pleistocene in age) ranges from less than 1,000 to as much as 300,000 gallons per day per foot, and the storage coefficient averages about 0.20. The transmissibility values are based on examination of test‐ hole samples from more than 400 test holes in and adjacent to the basin. Analysis of the model indicates that predicted maximum ground‐water withdrawals between 1962 and 2022 will not deplete the base flow of the Big or Little Blue Rivers by more than 5 percent.
","language":"English","publisher":"NGWA The Groundwater Association","doi":"10.1111/j.1745-6584.1966.tb01610.x","usgsCitation":"Emery, P.A., 1966, Use of analog model to predict streamflow depletion, big and little Blue River basin, Nebraska: Groundwater, v. 4, no. 4, p. 13-19, https://doi.org/10.1111/j.1745-6584.1966.tb01610.x.","productDescription":"7 p.","startPage":"13","endPage":"19","costCenters":[],"links":[{"id":386298,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nebraska","otherGeospatial":"Blue River Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -99.66796875,\n 39.9434364619742\n ],\n [\n -95.4052734375,\n 39.9434364619742\n ],\n [\n -95.4052734375,\n 41.705728515237524\n ],\n [\n -99.66796875,\n 41.705728515237524\n ],\n [\n -99.66796875,\n 39.9434364619742\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"4","issue":"4","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Emery, P. A.","contributorId":49392,"corporation":false,"usgs":true,"family":"Emery","given":"P.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":817170,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}