The probable magnitude of floods of any recurrence interval between 1.1 and 50 years for any stream in the Great Basin can be determined by methods presented in this report.
The Great Basin comprises nearly all of Nevada, western Utah, eastern California, and parts of Idaho, Oregon, and Wyoming. The physiography of the basin is a series of mountain ranges and desert valleys, which trend in a north-south direction. Extreme variations in climate from arid to humid are attributed to the mountains, which, in general, are at right angles to the prevailing westerly winds. The area is subject to cloudburst floods and mud-rock flows, and this situation often results in high rates of runoff and heavy erosion from small drainage basins. The greater part of the basin is desert, and because of the paucity of flood data, the flood characteristics are poorly defined.
Two sets of curves are provided for estimating the magnitude and frequency of floods: (1) curves that represent the ratio of a flood of any frequency to the mean annual flood, and (2) curves that relate the mean annual flood to the size of the drainage basin and, where significant, to the mean altitude of the basin. Using these curves, a flood of a selected frequency can be determined for any site within the range of the base data. Separate 50-year flood graphs are shown for most of the larger rivers that are affected by regulation or diversion.
The report also contains station descriptions and lists of peak discharges for 364 gaging stations at which flood records have been collected for 5 or more years.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1684","usgsCitation":"Butler, E., Reid, J., and Berwick, V., 1966, Magnitude and frequency of floods in the United States: Part 10. The Great Basin: U.S. Geological Survey Water Supply Paper 1684, Report: xii, 256 p.; 2 Plates: 23.00 in. x 32.69 in. and 23.00 in. x 32.70 in., https://doi.org/10.3133/wsp1684.","productDescription":"Report: xii, 256 p.; 2 Plates: 23.00 in. x 32.69 in. and 23.00 in. x 32.70 in.","numberOfPages":"270","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":430340,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24893.htm","linkFileType":{"id":5,"text":"html"}},{"id":25830,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1684/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the Great Basin showing hydrologic areas and location of gaging stations for which records are used in this report"},{"id":25831,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1684/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the Great Basin showing flood regions"},{"id":25832,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1684/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137865,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1684/report-thumb.jpg"}],"country":"United States","state":"California, Idaho, Nevada, Oregon, Utah, Wyoming","otherGeospatial":"Great Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.5921906626617,\n 32.58022804975384\n ],\n [\n -114.8513857745231,\n 32.6826323709157\n ],\n [\n -115.11687526317692,\n 38.430852245878754\n ],\n [\n -115.00681719621164,\n 39.44994435719141\n ],\n [\n -113.44432614039764,\n 37.767024727496846\n ],\n [\n -112.1682495264217,\n 37.55678413745511\n ],\n [\n -110.41480397149783,\n 41.662006507462394\n ],\n [\n -110.22811202576386,\n 42.246052724133136\n ],\n [\n -112.33588442607666,\n 42.57859964105248\n ],\n [\n -115.25776514378205,\n 41.56547182165073\n ],\n [\n -117.63454158924608,\n 41.66183397616126\n ],\n [\n -120.20937590707965,\n 43.4154688719461\n ],\n [\n -121.07443218592334,\n 43.57819853867787\n ],\n [\n -122.23188537008474,\n 42.64018449777984\n ],\n [\n -121.49938521409749,\n 42.2128983444282\n ],\n [\n -120.08064165281732,\n 41.001363389988626\n ],\n [\n -120.78412839492441,\n 39.88709203731142\n ],\n [\n -119.8758968405352,\n 38.93783308698025\n ],\n [\n -118.59892075047432,\n 36.32652672353966\n ],\n [\n -118.82750928759143,\n 34.784869099915454\n ],\n [\n -116.91926306887294,\n 33.77775647465552\n ],\n [\n -116.5921906626617,\n 32.58022804975384\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6495b5","contributors":{"authors":[{"text":"Butler, E.","contributorId":44124,"corporation":false,"usgs":true,"family":"Butler","given":"E.","email":"","affiliations":[],"preferred":false,"id":143176,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reid, J.K.","contributorId":54577,"corporation":false,"usgs":true,"family":"Reid","given":"J.K.","email":"","affiliations":[],"preferred":false,"id":143175,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Berwick, V.K.","contributorId":70368,"corporation":false,"usgs":true,"family":"Berwick","given":"V.K.","email":"","affiliations":[],"preferred":false,"id":143177,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":931,"text":"wsp1798B - 1966 - Fluvial sediment in the little Arkansas River basin, Kansas","interactions":[],"lastModifiedDate":"2013-08-12T12:35:55","indexId":"wsp1798B","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":"1798","chapter":"B","title":"Fluvial sediment in the little Arkansas River basin, Kansas","docAbstract":"Characteristics and transport of sediment in the Little Arkansas River basin in south-central Kansas were studied to determine if the water from the river could be used as a supplemental source for municipal supply or would provide adequate recharge to aquifers that are sources of municipal and agricultural water supplies. During periods when overland 1low contributed a significant amount to streamflow, the suspended sediment in the Little Arkansas River at Valley Center averaged about 85 percent of clay, about 13 percent of silt, and about 2 percent of sand. The average annual suspended-sediment discharge for the water years 1958, 1959, 1960, and 1961 was about 306,000 tons, and about 80 percent of the load was transported during 133 days of the 1,461-day period. The average daily water discharge of 352 cubic feet per second for the period 1958-61 was more than the long-term (i}9-year) average of 245 cfs; therefore, the average annual sediment load for 1958-61 was probably greater than the average annual load for the same long-term period. \n\nStudies of seepage in a part of the channel of Kisiwa Creek indicated that an upstream gravel-pit operation yielded clays which, when deposited in the channel, reduced seepage. A change in plant operation and subsequent runoff that removed the deposited clays restored natural seepage conditions. Experiments by the Wichita Water Department showed that artificial recharge probably cannot be accomplished by using raw turbid water that is injected into wells or by using pits. Recharge by raw turbid water on large permeable areas or by seepage canals may be feasible. \n\nStudies of chemical quality of surface water at several sites in the Little Arkansas River basin indicate that Turkey. Creek is a major contributor of chloride and other dissolved solids to the Little Arkansas River and that the dissolved-solids content is probably highest during low-flow periods when suspended-sediment concentration is low. Data collected by the Wichita Water Department indicate that chloride concentrations are diminishing with time at sampled locations. and they receive recharge from rainwater and snowmelt moving through overlying alluvium and from storage in the De Chelly sandstone which encloses the east half of the diatreme. \n\nThe quality of water from all areas is suitable for domestic use. However, special treatment may be necessary to make the water suitable for pulp processing.","language":"ENGLISH","publisher":"U.S. Geological Survey ;","doi":"10.3133/wsp1798B","usgsCitation":"Albert, C., and Stramel, G., 1966, Fluvial sediment in the little Arkansas River basin, Kansas: U.S. Geological Survey Water Supply Paper 1798, v, 30 p. :ill., maps, diagrs. (1 fold in pocket) ;24 cm., https://doi.org/10.3133/wsp1798B.","productDescription":"v, 30 p. :ill., maps, diagrs. (1 fold in pocket) ;24 cm.","costCenters":[],"links":[{"id":137978,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1798b/report-thumb.jpg"},{"id":25405,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1798b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":276512,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1798b/plate-2.pdf"},{"id":276511,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1798b/plate-1.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6ae50a","contributors":{"authors":[{"text":"Albert, C.D.","contributorId":23923,"corporation":false,"usgs":true,"family":"Albert","given":"C.D.","email":"","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":142874,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stramel, G.J.","contributorId":47768,"corporation":false,"usgs":true,"family":"Stramel","given":"G.J.","affiliations":[],"preferred":false,"id":142875,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2669,"text":"wsp1819J - 1966 - Special sediment investigations Mississippi River at St. Louis, Missouri, 1961-63","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"wsp1819J","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":"J","title":"Special sediment investigations Mississippi River at St. Louis, Missouri, 1961-63","docAbstract":"Four sets of comprehensive hydraulic and sediment data were obtained during 1961-63 for the Mississippi River at St. Louis at ranges of mean velocity from 3.3 to 5.6 feet per second, of mean depth from 22 to 37 feet, of width from 1,570 to 1,670 feet, of mean water-surface slope from 0.000054 to 0.000109, and of suspended-sediment concentration from 314 to 928 parts per million. The suspended sediment consisted of 9-46 percent sand, 30-46 percent silt, and 20-56 percent clay. The median size of bed material was about 0.42 millimeter for three sets of measurements and about 0.18 millimeter for the other set. A dune bed form was present during all four data-collection periods. Data obtained on consecutive days indicate that the turbulence constant can be computed from either streamflow-measurement notes or from vertical-velocity profiles. Constants computed from streamflow-measurement notes averaged 0.34, and those from vertical-velocity profiles averaged 0.35. The coefficients of vertical distribution of concentration for selected size ranges of suspended sands (expressed as z1, the slope, of the line relating the logarithms of concentration and a depth parameter) plotted against corresponding fall velocities indicate that on the average, the z1's are proportional to about the 0.7 power of the fall velocity. The data also indicate that the relation of z1 to fall velocity may vary with the mean velocity of flow.","language":"ENGLISH","publisher":"U.S. Geological Survey ;","doi":"10.3133/wsp1819J","usgsCitation":"Scott, C.H., and Stephens, H.D., 1966, Special sediment investigations Mississippi River at St. Louis, Missouri, 1961-63: U.S. Geological Survey Water Supply Paper 1819, iii, 35 p. :ill., maps (1 fold. in pocket) ;24 cm., https://doi.org/10.3133/wsp1819J.","productDescription":"iii, 35 p. :ill., maps (1 fold. in pocket) ;24 cm.","costCenters":[],"links":[{"id":138251,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1819j/report-thumb.jpg"},{"id":29017,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1819j/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29018,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1819j/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29019,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1819j/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29020,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1819j/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ae4b07f02db5fb82a","contributors":{"authors":[{"text":"Scott, Cloyd H.","contributorId":106871,"corporation":false,"usgs":true,"family":"Scott","given":"Cloyd","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":145584,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stephens, Howard D.","contributorId":47347,"corporation":false,"usgs":true,"family":"Stephens","given":"Howard","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":145583,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"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":42919,"text":"ofr66122 - 1966 - Water resources of the Western Oswego River basin, N.Y. -interim report","interactions":[],"lastModifiedDate":"2015-10-21T09:53:07","indexId":"ofr66122","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":"66-122","title":"Water resources of the Western Oswego River basin, N.Y. -interim report","docAbstract":"This report contains a tabulation of data collection sites established by the U.S. Geological Survey in the Western Oswego River basin. Information on the types of data collected at each site is also provided.
\nStatistical summaries are furnished for selected stream-gaging stations in the form of duration, flood frequency, and low-flow frequency curves.
\nClimatological data on long-term average precipitation is provided in the form of an isohyetal map of the study area.
\nSelected results of computerized data on flow passing Mud Lock and. on Cayuga Lake levels are presented.
\nData being collected in the course of the ground-water studies includes test borings, information on existing wells, and geologic mapping. Preliminary analysis of this data indicates that the areas with the greatest potential for development of large ground-water supplies are portions of the basin underlain by carbonate rocks, the unconsolidated deposits in the northern portion of the basin, and the unconsolidated deposits south of the four lakes.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr66122","collaboration":"Prepared in cooperation with New York State Conservation Department Division of Water Resources.","usgsCitation":"Shampine, W.J., Crain, L.J., Shipley, R.C., and Hood, J.B., 1966, Water resources of the Western Oswego River basin, N.Y. -interim report: U.S. Geological Survey Open-File Report 66-122, ii, 27 p., https://doi.org/10.3133/ofr66122.","productDescription":"ii, 27 p.","numberOfPages":"29","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":172998,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr66122.jpg"},{"id":310236,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1966/0122/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New York","otherGeospatial":"Western Oswego River Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.882080078125,\n 41.81636125072054\n ],\n [\n -77.882080078125,\n 43.369119087738554\n ],\n [\n -75.90728759765625,\n 43.369119087738554\n ],\n [\n -75.90728759765625,\n 41.81636125072054\n ],\n [\n -77.882080078125,\n 41.81636125072054\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f4e4b07f02db5f02e5","contributors":{"authors":[{"text":"Shampine, William J.","contributorId":89891,"corporation":false,"usgs":true,"family":"Shampine","given":"William","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":227404,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Crain, Leslie J.","contributorId":59048,"corporation":false,"usgs":true,"family":"Crain","given":"Leslie","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":227406,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Shipley, Richard C.","contributorId":89209,"corporation":false,"usgs":true,"family":"Shipley","given":"Richard","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":227407,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Hood, James B. Jr.","contributorId":32227,"corporation":false,"usgs":true,"family":"Hood","given":"James","suffix":"Jr.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":227405,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"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":3511,"text":"cir532 - 1966 - The interior of the Earth, an elementary description","interactions":[],"lastModifiedDate":"2017-08-27T18:00:50","indexId":"cir532","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":"532","title":"The interior of the Earth, an elementary description","docAbstract":"Evidence on the structure and composition of the earth's interior comes from (1) observations of surface rocks, (2) geophysical data from earthquakes, flow of heat from the interior, the magnetic field, and gravity, (3) laboratory experiments on surface rocks and minerals, and (4) comparison of the earth with other planets, the sun, stars, and meteorites.\r\n\r\nThe major structural components in the earth that are separated by sharp discontinuities are the crust, the mantle, and the core. The crust forms a very thin surface skin, the mantle is a thick shell that extends half the radius down into the earth, and the core occupies the central part. The crust and upper mantle are known to vary in physical and chemical characteristics, both horizontally and vertically; the lower mantle and core are generally assumed to be uniform because their diagnostic geophysical phenomena are masked by the physical properties of the upper layers.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir532","usgsCitation":"Robertson, E.C., 1966, The interior of the Earth, an elementary description: U.S. Geological Survey Circular 532, iii, 10 p. :illus. ;26 cm., https://doi.org/10.3133/cir532.","productDescription":"iii, 10 p. :illus. ;26 cm.","costCenters":[],"links":[{"id":30525,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1966/0532/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123911,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1966/0532/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a85e4b07f02db64d4c1","contributors":{"authors":[{"text":"Robertson, Eugene C.","contributorId":71139,"corporation":false,"usgs":true,"family":"Robertson","given":"Eugene","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":147063,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":42918,"text":"ofr66120 - 1966 - Summer base-flow recession curves for Iowa streams","interactions":[],"lastModifiedDate":"2016-02-22T10:25:58","indexId":"ofr66120","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":"66-120","title":"Summer base-flow recession curves for Iowa streams","docAbstract":"Base-flow recession. curves for the summer months (June through September) were developed in this study for gaging stations on interior Iowa streams having five or more years of record. The tabulated data enables the user, starting with a known base flow at a gage, to estimate base flows for up to 20 days in the future. Rainfall during the period o£ the forecast will require that a new estimate be made after the stream again reaches base flow.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Iowa City","doi":"10.3133/ofr66120","collaboration":"Prepared in cooperation with the Iowa Natural Resources Council","usgsCitation":"Saboe, C., 1966, Summer base-flow recession curves for Iowa streams: U.S. Geological Survey Open-File Report 66-120, 27 p., https://doi.org/10.3133/ofr66120.","productDescription":"27 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"links":[{"id":264294,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1966/0120/report.pdf","size":"1885","linkFileType":{"id":1,"text":"pdf"}},{"id":264295,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1966/0120/report-thumb.jpg"}],"country":"United States","state":"Iowa","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-91.217706,43.50055],[-91.216035,43.481142],[-91.233367,43.455168],[-91.200359,43.412701],[-91.198953,43.389835],[-91.21477,43.365874],[-91.20662,43.352524],[-91.132813,43.32803],[-91.107237,43.313645],[-91.07371,43.274746],[-91.071698,43.261014],[-91.058644,43.257679],[-91.066398,43.239293],[-91.12217,43.197255],[-91.1462,43.152405],[-91.1562,43.142945],[-91.175253,43.134665],[-91.179457,43.067427],[-91.156562,42.978226],[-91.14543,42.958211],[-91.14988,42.941955],[-91.1438,42.922877],[-91.146177,42.90985],[-91.100565,42.883078],[-91.097656,42.859871],[-91.091837,42.851225],[-91.09406,42.830813],[-91.078665,42.827678],[-91.069549,42.769628],[-91.060261,42.761847],[-91.065783,42.753387],[-91.056297,42.747341],[-91.051275,42.737001],[-91.035418,42.73734],[-91.026786,42.724228],[-91.000128,42.716189],[-90.977735,42.696816],[-90.949213,42.685573],[-90.923634,42.6855],[-90.88743,42.67247],[-90.731132,42.643437],[-90.706303,42.634169],[-90.692031,42.610366],[-90.686975,42.591774],[-90.661527,42.567999],[-90.654127,42.5499],[-90.643927,42.540401],[-90.636927,42.513202],[-90.655927,42.491703],[-90.654027,42.478503],[-90.624328,42.458904],[-90.567968,42.440389],[-90.560439,42.432897],[-90.555018,42.416138],[-90.477279,42.383794],[-90.462619,42.367253],[-90.443874,42.355218],[-90.416535,42.325109],[-90.430884,42.27823],[-90.419326,42.254467],[-90.400653,42.239293],[-90.391108,42.225473],[-90.356964,42.205445],[-90.328273,42.201047],[-90.282173,42.178846],[-90.234919,42.165431],[-90.209479,42.15268],[-90.197342,42.128163],[-90.167533,42.122475],[-90.161159,42.106372],[-90.168358,42.075779],[-90.164485,42.042105],[-90.151579,42.030633],[-90.140061,42.003252],[-90.146225,41.981329],[-90.164135,41.956178],[-90.163847,41.944934],[-90.152659,41.933058],[-90.153584,41.906614],[-90.181401,41.844647],[-90.181973,41.80707],[-90.278633,41.767358],[-90.310708,41.742214],[-90.317668,41.72269],[-90.313435,41.698082],[-90.334525,41.679559],[-90.343452,41.646959],[-90.339528,41.598633],[-90.343228,41.587833],[-90.41283,41.565333],[-90.461432,41.523533],[-90.500633,41.518033],[-90.540935,41.526133],[-90.591037,41.512832],[-90.602137,41.506032],[-90.605937,41.494232],[-90.655839,41.462132],[-90.750142,41.449632],[-90.846558,41.455141],[-90.930016,41.421404],[-90.979815,41.434321],[-91.027787,41.423603],[-91.043988,41.415897],[-91.05101,41.387556],[-91.06652,41.365246],[-91.074841,41.305578],[-91.092034,41.286911],[-91.114186,41.250029],[-91.113648,41.241401],[-91.07298,41.207151],[-91.041536,41.166138],[-91.027214,41.163373],[-91.007586,41.166183],[-90.99496,41.160624],[-90.946627,41.096632],[-90.949383,41.072711],[-90.942253,41.034702],[-90.945949,41.006495],[-90.958142,40.979767],[-90.952233,40.954047],[-90.965344,40.921633],[-91.009536,40.900565],[-91.021562,40.884021],[-91.044653,40.868356],[-91.05643,40.848387],[-91.092993,40.821079],[-91.097649,40.805575],[-91.091703,40.779708],[-91.110424,40.745528],[-91.115735,40.725168],[-91.11194,40.697018],[-91.123928,40.669152],[-91.185428,40.638071],[-91.253074,40.637962],[-91.306524,40.626231],[-91.339719,40.613488],[-91.359873,40.601805],[-91.379752,40.57445],[-91.401482,40.559458],[-91.406373,40.551831],[-91.404125,40.539127],[-91.384531,40.530948],[-91.369059,40.512532],[-91.364211,40.500043],[-91.364915,40.484168],[-91.381769,40.442555],[-91.372554,40.4012],[-91.381958,40.387632],[-91.419422,40.378264],[-91.441243,40.386255],[-91.452458,40.375501],[-91.463895,40.375659],[-91.465116,40.385257],[-91.484507,40.3839],[-91.490977,40.393484],[-91.487829,40.403866],[-91.498093,40.401926],[-91.522333,40.409648],[-91.527057,40.416689],[-91.519012,40.431298],[-91.529132,40.434272],[-91.533548,40.440804],[-91.523271,40.450061],[-91.526155,40.458625],[-91.552691,40.458769],[-91.574746,40.465664],[-91.590817,40.492292],[-91.621353,40.510072],[-91.618028,40.53403],[-91.6219,40.542292],[-91.6887,40.55739],[-91.691557,40.564867],[-91.686357,40.580875],[-91.716769,40.59853],[-91.729115,40.61364],[-92.686693,40.589809],[-94.294813,40.571341],[-94.632032,40.571186],[-95.765645,40.585208],[-95.753148,40.59284],[-95.748626,40.603355],[-95.768926,40.621264],[-95.776251,40.647463],[-95.795489,40.662384],[-95.822913,40.66724],[-95.842801,40.677496],[-95.852615,40.702262],[-95.883178,40.717579],[-95.888907,40.731855],[-95.879027,40.753081],[-95.84662,40.768619],[-95.835232,40.779151],[-95.834523,40.787778],[-95.845342,40.811324],[-95.837186,40.835347],[-95.847084,40.854174],[-95.847785,40.864328],[-95.838735,40.872191],[-95.815933,40.879846],[-95.809474,40.891228],[-95.813458,40.901693],[-95.836438,40.921642],[-95.839743,40.93278],[-95.829074,40.975688],[-95.838908,40.986484],[-95.867286,41.001599],[-95.869486,41.009399],[-95.859918,41.025403],[-95.859654,41.035695],[-95.882415,41.060411],[-95.862587,41.088399],[-95.865888,41.117898],[-95.88208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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4affe4b07f02db697b62","contributors":{"authors":[{"text":"Saboe, C.W.","contributorId":51837,"corporation":false,"usgs":true,"family":"Saboe","given":"C.W.","email":"","affiliations":[],"preferred":false,"id":227403,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":52539,"text":"ofr6642 - 1966 - Hydrologic inventory of the Lompoc subarea, Santa Ynez River basin, Santa Barbara County, California, 1957-62","interactions":[],"lastModifiedDate":"2022-01-03T20:00:08.491215","indexId":"ofr6642","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":"66-42","title":"Hydrologic inventory of the Lompoc subarea, Santa Ynez River basin, Santa Barbara County, California, 1957-62","docAbstract":"Hydrologic data collected during the climatically near-average 6-year period of inventory 1957-62 provide the basis for making estimates of supply to and demand from the Lompoc subarea of the Santa Ynez River basin and changes in the quantity of water stored in the deposits of the basin. The hydrologic inventory presents gains or accretions to the water supply, as inflow, equated with loss by water demands, as outflow. The difference is the ground-water storage change. Items of inflow include precipitation, surface and subsurface inflow, irrigation return, and sewage effluent. Items of outflow include surface and subsurface outflow, evapotranspiration, and water pumped for irrigation and other uses. \r\n\r\nGround-water storage changes occurred as depletions of the shallow water body beneath the eastern and central parts of the Lompoc plain and beneath the upland part of the Lompoc subarea to the north and east. The estimated annual depletion of storage averaged 3,000 acre-feet. \r\n\r\nA near balance between inflow and outflow is indicated by a calculated difference of 5,000 acre-feet of accretion and an observed depletion of ground water in storage of about 3,000 acre-feet. The difference of 8,000 acre-feet between the two values, considering the magnitude of total inflow and outflow--110,000 and 105,000 acre-feet, is not significant. For the period of inventory, more water was discharged from the basin by flow in the Santa Ynez River than by pumping from wells. \r\n\r\nThe near balance between inflow and outflow for a period of near-average climatic conditions, in general, substantiates a previous estimate that perennial pumpage is as much as about 20,000 acre-feet. However, water in storage will be depleted if the progressive change in the ratio of irrigation pumpage to other pumpage continues. Even though the hydrologic balance is maintained, changes in chemical quality of the ground water, due to recycling of irrigation water and inflow of poor-quality connate water from the consolidated rocks, indicate that chemical equilibrium has not been reached. Perennial supply under the 1957-62 conditions of inventory is estimated to be between 24,000 and 26,000 acre-feet.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6642","usgsCitation":"Evenson, R.E., 1966, Hydrologic inventory of the Lompoc subarea, Santa Ynez River basin, Santa Barbara County, California, 1957-62: U.S. Geological Survey Open-File Report 66-42, Report: iv, 27 p.; 1 Plate: 30.86 × 18.94 inches, https://doi.org/10.3133/ofr6642.","productDescription":"Report: iv, 27 p.; 1 Plate: 30.86 × 18.94 inches","costCenters":[],"links":[{"id":110342,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_52174.htm","linkFileType":{"id":5,"text":"html"},"description":"52174"},{"id":86949,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1966/0042/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86948,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1966/0042/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":173956,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1966/0042/report-thumb.jpg"}],"country":"United States","state":"California","county":"Santa Barbara County","otherGeospatial":"Santa Ynez River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -120.66284179687499,\n 34.57895241036948\n ],\n [\n -120.3387451171875,\n 34.57895241036948\n ],\n [\n -120.3387451171875,\n 34.70549341022544\n ],\n [\n -120.66284179687499,\n 34.70549341022544\n ],\n [\n -120.66284179687499,\n 34.57895241036948\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b15e4b07f02db6a498c","contributors":{"authors":[{"text":"Evenson, R. E.","contributorId":19933,"corporation":false,"usgs":true,"family":"Evenson","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":245517,"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":70173975,"text":"70173975 - 1966 - Selected flow characteristics of streams in the Willamette River Basin, Oregon","interactions":[],"lastModifiedDate":"2016-06-21T14:07:14","indexId":"70173975","displayToPublicDate":"1967-01-01T00:00:00","publicationYear":"1966","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":375,"text":"Open-File Report","active":false,"publicationSubtype":{"id":6}},"title":"Selected flow characteristics of streams in the Willamette River Basin, Oregon","docAbstract":"Flow-duration, annual low-flow, and annual high-flow tables through September 30, 1963, are given in this report for 110 stream-gaging stations in the Willamette and Sandy River basins. These tables summarize the basic data needed to define the streamflow characteristics at the gaging stations. The content of each of the three summary tables is described, and techniques for preparing flow-duration curves, low-flow frequency curves, and high-flow frequency curves are explained.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Portland, OR","doi":"10.3133/70173975","usgsCitation":"Swift, C.H., 1966, Selected flow characteristics of streams in the Willamette River Basin, Oregon: Open-File Report, 177 p., https://doi.org/10.3133/70173975.","productDescription":"177 p.","numberOfPages":"181","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":324025,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70173975.jpg"},{"id":324138,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70173975/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Oregon","otherGeospatial":"Willamette River Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -123.585205078125,\n 43.30919109985686\n ],\n [\n -123.585205078125,\n 45.775186183521036\n ],\n [\n -121.40991210937499,\n 45.775186183521036\n ],\n [\n -121.40991210937499,\n 43.30919109985686\n ],\n [\n -123.585205078125,\n 43.30919109985686\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"576913e7e4b07657d19ff265","contributors":{"authors":[{"text":"Swift, C. H. III","contributorId":43624,"corporation":false,"usgs":true,"family":"Swift","given":"C.","suffix":"III","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":639897,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70095001,"text":"70095001 - 1966 - Flow probability of New Jersey streams","interactions":[],"lastModifiedDate":"2014-03-25T10:32:52","indexId":"70095001","displayToPublicDate":"1966-01-01T13:43:00","publicationYear":"1966","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":149,"text":"New Jersey Division of Water Policy and Supply Water Resources Circular","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"15","title":"Flow probability of New Jersey streams","docAbstract":"This report is one of a series published by the Division of Water \nPolicy and Supply of the New Jersey Department of Conservation and Economic \nDevelopment to make basic water data available in a form that can be readily \nused by all interested persons. The objective of the present report is to \npresent flow-duration information based on past records so that estimates \nof future flows of New Jersey's streams may be made. It is an extension of \nthe flow-duration portions of Water Resources Circular 6 (Miller and McCall, \n1961).","language":"English","publisher":"New Jersey Division of Water Policy and Supply","publisherLocation":"Trenton, NJ","collaboration":"Prepared by the U.S. Geological Survey in cooperation with the State of New Jersey Department of Conservation and Economic Development Division of Water Policy and Supply","usgsCitation":"Miler, E., 1966, Flow probability of New Jersey streams: New Jersey Division of Water Policy and Supply Water Resources Circular 15, 61 p.","productDescription":"61 p.","numberOfPages":"71","costCenters":[],"links":[{"id":282843,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70095001.jpg"},{"id":284830,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70095001/report.pdf"}],"country":"United States","state":"New Jersey","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -75.5634,38.7888 ], [ -75.5634,41.3574 ], [ -73.8851,41.3574 ], [ -73.8851,38.7888 ], [ -75.5634,38.7888 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53559438e4b0120853e8bf88","contributors":{"authors":[{"text":"Miler, E.G.","contributorId":41337,"corporation":false,"usgs":true,"family":"Miler","given":"E.G.","email":"","affiliations":[],"preferred":false,"id":491045,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":38844,"text":"pp542A - 1965 - Effects of the earthquake of March 27, 1964, at Anchorage, Alaska","interactions":[{"subject":{"id":38844,"text":"pp542A - 1965 - Effects of the earthquake of March 27, 1964, at Anchorage, Alaska","indexId":"pp542A","publicationYear":"1965","noYear":false,"chapter":"A","title":"Effects of the earthquake of March 27, 1964, at Anchorage, Alaska"},"predicate":"IS_PART_OF","object":{"id":70048211,"text":"pp542 - 1969 - The Alaska earthquake, March 27, 1964: Effects on communities","indexId":"pp542","publicationYear":"1969","noYear":false,"title":"The Alaska earthquake, March 27, 1964: Effects on communities"},"id":1}],"isPartOf":{"id":70048211,"text":"pp542 - 1969 - The Alaska earthquake, March 27, 1964: Effects on communities","indexId":"pp542","publicationYear":"1969","noYear":false,"title":"The Alaska earthquake, March 27, 1964: Effects on communities"},"lastModifiedDate":"2022-04-28T19:13:46.811205","indexId":"pp542A","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1965","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":"542","chapter":"A","title":"Effects of the earthquake of March 27, 1964, at Anchorage, Alaska","docAbstract":"Anchorage, Alaska’s largest city, is about 80 miles west-northwest of the epicenter of the March 27 earthquake. Because of its size, Anchorage bore the brunt of property damage from the quake; it sustained greater losses than all the rest of Alaska combined. Damage was caused by direct seismic vibration, by ground cracks, and by landslides. Direct seismic vibration affected chiefly multistory buildings and buildings having large floor areas, probably because of the long period and large amplitude of the seismic waves reaching Anchorage. Most small buildings were spared. Ground cracks caused capricious damage throughout the Anchorage Lowland. Cracking was most prevalent near the heads or within landslides but was also widespread elsewhere. Landslides themselves caused the most devastating damage.
Triggering of landslides by the earthquake was related to the physical-engineering properties of the Bootlegger Cove Clay, a glacial estuarine-marine deposit that underlies much of the Anchorage area. The Bootlegger Cove Clay contains zones of low shear strength, high water content, and high sensitivity that failed under the vibratory stress of the earthquake. Shear strength in sensitive zones ranged from less than 0.2 tsf to about 0.5 tsf; sensitivity ranged from about 10 to more than 40. Sensitive zones generally are centered about 10 to 20 feet above sea level, between zones of stiff insensitive clay. Many physical tests by the U.S. Army Corps of Engineers were directed toward analyzing the causes of failure in the Bootlegger Cove Clay and finding possible remedies. Strengths and sensitivities were measured directly in the field by means of vane shear apparatus. A4tterberg limits, natural water contents, triaxial shear, sensitivity, dynamic modulus, consolidation strength, and other properties were measured in the laboratory. Pulsating-load tests simulated earthquake loading.
Most of the destructive landslides in the Anchorage area moved primarily by translation rather than by rotation. Thus, all the highly damaging slides were of a single structural dynamic family despite wide variations in size, appearance, and complexity. They slid on nearly horizontal slip surfaces after loss of strength in the Bootlegger Core Clay. Same failures are attributed to spontaneous liquefaction of sand layers. All translatory slides surmounted flat-topped bluffs bounded marginally by steep slopes facing lower ground. Destructive translatory slides occurred in the downtown area (Fourth Avenue slide and L Street slide), at Government Hill, and at Turnagain Heights. Less destructive slides occurred in many other places-mostly uninhabited or undeveloped areas.
In most translatory slides, damage was greatest in graben areas at the head and in pressure-ridge areas at the toe. Many buildings inside the perimeters of slide blocks were little damaged despite horizontal translations of several feet. The large Turnagain Heights slide, however, was characterized by a complete disintegration and drastic lowering of the prequake land surface. Extensive damage back from the slide, moreover, was caused by countless tension cracks.
An approximation of the depth of failure in the Bootlegger Cove Clay in the various slides may be obtained by using a geometric relationship herein called the \"graben rule.\" Because the cross-sectional area of the graben at the head of the slide approximated the cross-sectional area of the space voided behind the slide block as the block moved outward, the depth of failure was equal to the area of the graben divided by the lateral displacement. This approximation supplements and accords with test data obtained from borings. The graben rule should apply to any translatory slide in which flowage of material from the zone of failure has not been excessive.
Geologic evidence indicates that landslides similar to those triggered by the March 27 earthquake have occurred in the Anchorage area at various times in the past.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"The Alaska earthquake, March 27, 1964: Effects on communities (Professional Paper 542)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, DC","doi":"10.3133/pp542A","usgsCitation":"Hansen, W.R., 1965, Effects of the earthquake of March 27, 1964, at Anchorage, Alaska: U.S. Geological Survey Professional Paper 542, Report: iv, 68 p.; 2 Plates: 50.44 x 26.21 inches and 35.05 x 10.13 inches, https://doi.org/10.3133/pp542A.","productDescription":"Report: iv, 68 p.; 2 Plates: 50.44 x 26.21 inches and 35.05 x 10.13 inches","numberOfPages":"77","additionalOnlineFiles":"Y","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":399840,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4583.htm"},{"id":170342,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0542a/report-thumb.jpg"},{"id":113265,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542a/pp542a_plate2.pdf","size":"1792","linkFileType":{"id":1,"text":"pdf"}},{"id":113264,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542a/pp542a_plate1.pdf","size":"7988","linkFileType":{"id":1,"text":"pdf"}},{"id":113263,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0542a/pp542a_text.pdf","size":"19635","linkFileType":{"id":1,"text":"pdf"}},{"id":111457,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0542a/index.html","linkFileType":{"id":5,"text":"html"}}],"scale":"2400","country":"United States","state":"Alaska","city":"Anchorage","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -150.100708,60.999438 ], [ -150.100708,61.301243 ], [ -149.624949,61.301243 ], [ -149.624949,60.999438 ], [ -150.100708,60.999438 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a27e4b07f02db61031d","contributors":{"authors":[{"text":"Hansen, Wallace R.","contributorId":90273,"corporation":false,"usgs":true,"family":"Hansen","given":"Wallace","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":220531,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":52542,"text":"ofr6645 - 1965 - The operation and maintenance of a crest-stage gaging station","interactions":[],"lastModifiedDate":"2016-11-10T16:20:28","indexId":"ofr6645","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"66-45","title":"The operation and maintenance of a crest-stage gaging station","docAbstract":"The purpose of this manual is to familiarize field personnel with the procedures involved in operating crest-stage gaging stations. Crest-stage gages are used to determine the elevation of a peak stage occurring at a specific location in a stream.
\nA crest-stage gage consists of a length of 14-inch diameter pipe installed in a vertical position in the stream channel (figure 1). The pipe is vented and equipped with an intake system that allows water to enter and leave the pipe as the stream rises and recedes. An equal length of aluminum \"T\" channel (staff) is inserted in the pipe and made to rest on a positive stop called a datum pin. When granulated cork is placed in the gage, the cork will float on the rising stage, then adhere to the staff after the stage recedes. The peak stage is then determined by removing the staff and measuring the distance between the cork line and the lower end of the staff.
\nThe primary purpose of a crest-stage gaging station is to collect hydrologic data for flood-frequency analyses. Collection of data for such analyses involves operating a network of stations for a period of years until sufficient peak flow data are obtained to accurately define flood-frequency curves. Because carelessness in collecting data at the gage site might result in the loss of an entire year's flood event, the importance of proper operation and maintenance of these gages can not be overemphasized.
\nPeak discharges are related to the basin characteristics and major changes in these characteristics must be evaluated. For€st fires, timber harvest, or a new road location that alters the natural drainage of the basin, may effect the intensity and timing of the runoff of the basin.
\nRigid datum controls must be maintained at the gage site throughout the period of record. Physical changes of the site resulting from flood flows or manmade alterations must be evaluated. If a drainage structure such as a culvert is part of the site features, free-flow conditions must be maintained or obstructions carefully documented.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Portland, OR","doi":"10.3133/ofr6645","usgsCitation":"Friday, J., 1965, The operation and maintenance of a crest-stage gaging station: U.S. Geological Survey Open-File Report 66-45, vi, 20 p., https://doi.org/10.3133/ofr6645.","productDescription":"vi, 20 p.","numberOfPages":"28","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":173959,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr6645.jpg"},{"id":324122,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1966/0045/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db64935b","contributors":{"authors":[{"text":"Friday, John","contributorId":19160,"corporation":false,"usgs":true,"family":"Friday","given":"John","email":"","affiliations":[],"preferred":false,"id":245520,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":64106,"text":"gp467 - 1965 - Aeromagnetic map of parts of Marquette, Dickinson, Baraga, Alger, and Schoolcraft Counties, Michigan, and its geologic interpretation","interactions":[{"subject":{"id":41753,"text":"ofr647 - 1964 - Aeromagnetic map of parts of Marquette, Dickinson, Baraga, Alger, and Schoolcraft Counties, Michigan","indexId":"ofr647","publicationYear":"1964","noYear":false,"title":"Aeromagnetic map of parts of Marquette, Dickinson, Baraga, Alger, and Schoolcraft Counties, Michigan"},"predicate":"SUPERSEDED_BY","object":{"id":64106,"text":"gp467 - 1965 - Aeromagnetic map of parts of Marquette, Dickinson, Baraga, Alger, and Schoolcraft Counties, Michigan, and its geologic interpretation","indexId":"gp467","publicationYear":"1965","noYear":false,"title":"Aeromagnetic map of parts of Marquette, Dickinson, Baraga, Alger, and Schoolcraft Counties, Michigan, and its geologic interpretation"},"id":1}],"lastModifiedDate":"2016-09-09T15:44:41","indexId":"gp467","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":317,"text":"Geophysical Investigations Map","code":"GP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"467","title":"Aeromagnetic map of parts of Marquette, Dickinson, Baraga, Alger, and Schoolcraft Counties, Michigan, and its geologic interpretation","docAbstract":"The U. S. Geological Survey, in cooperation with the Geological Survey Division of the Michigan Department of Conservation, is conducting a comprehensive restudy of the iron-bearing districts of Michigan. The use of aeromagnetic data is one of the fastest and most reliable methods for outlining the areal distribution of magnetic iron-formation and thus is of material value in assessing the iron resources of the United States. As part of this program of restudy, aeromagnetic surveys of approximately 4,500 square miles of the Northern Peninsula have been made. The results of several of these surveys have been presented by Balsley and others (1949) and by Wier and others (.1953). This report is about a survey made in 1950, over an area of about 1,400 square miles in Marquette County and ad-· joining strips in northern Dickinson and northeastern Baraga Counties, and a later survey flown in 1961, over about 500 square miles in parts of Marquette, Alger, and Schoolcraft Counties. The Marquette iron range extends in an east-west direction across approximately the west-central part of the area, and iron districts of lesser importance are located at Republic, in the southwestern part of the area, and near Gwinn, in the south -central part of the area.
Aeromagnetic surveys were flown along north-south lines spaced at intervals of one-quarter mile in the western part of the area and at intervals of from about 1 to 3 miles in the eastern part. Lines were flown at approximately 500 feet above the surface or at elevations of 1,100 to 2,400 feet above sea level. The flight path of the aircraft was recorded by a gyrostabilized continuous-strip camera, and elevation was continuously recorded by a radio altimeter. Magnetic measurements were made by an AN/ASQ-3A fluxgate magnetometer. Compilation of aeromagnetic data was by standard methods, described by Balsley ( 1952 ), under the supervision of John Kirby and Frank Petrafeso. The aeromagnetic contours are relative to an arbitrary datum.
Magnetic properties of rocks were measured by W. E. Huff.
At the time the earlier aeromagnetic survey was flown, the only base maps available were planimetric maps such as the Helena NW quadrangle and county road maps. Small errors, therefore, may exist in the location of flight lines and specific aeromagnetic a nomalies.
The major magnetic anomalies and broad areas that have characteristic magnetic patterns are correlated herein with geology as determined from published reports and from mapping done since 1957 by the U. S. Geological Survey in the eastern part of the Marquette iron range. The geology north of the Marquette iron range and west of the line between R. 25 W. and R. 26 W. is based mainly on a compilation made by Robert Reed of the Geological Survey Division of the Michigan Department of Conservation from data in the files of the State Survey. In addition some aeromagnetic features have been checked by ground magnetometer in selected localities and correlated directly with the rock types. A few oriented samples have been collected for measurement of the magnetic properties of the major rock units, but many hundreds or thousands of samples would be required to obtain a full range of values of the magnetic susceptibility and remanent magnetization of the rocks over such a large area.
Although the geology of much of the area is still imperfectly known, the available aeromagnetic data together with the best obtainable geologic data are presented at this time, rather than awaiting the eventual extension or completion of the present mapping program, because the combined data provide much information on the extent and location of magnetic iron-formation and other major rock units where concealed beneath glacial, vegetative, and alluvial cover.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/gp467","collaboration":"Prepared in cooperation with the Michigan Department of Conservation Geological Survey Division","usgsCitation":"Case, J.E., and Gair, J., 1965, Aeromagnetic map of parts of Marquette, Dickinson, Baraga, Alger, and Schoolcraft Counties, Michigan, and its geologic interpretation: U.S. Geological Survey Geophysical Investigations Map 467, Document: 10 p.; 3 Plates: 48.50 x 43.26 inches or smaller, https://doi.org/10.3133/gp467.","productDescription":"Document: 10 p.; 3 Plates: 48.50 x 43.26 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":250551,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0467/plate-1.pdf","size":"22930","linkFileType":{"id":1,"text":"pdf"}},{"id":250550,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gp/0467/report.pdf","size":"1068","linkFileType":{"id":1,"text":"pdf"}},{"id":250552,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0467/plate-2.pdf","size":"10448","linkFileType":{"id":1,"text":"pdf"}},{"id":250553,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0467/plate-3.pdf","size":"14970","linkFileType":{"id":1,"text":"pdf"}},{"id":253995,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gp/0467/report-thumb.jpg"}],"scale":"62500","country":"United States","state":"Michigan","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -88.166667,\n 46.916667\n ],\n [\n -87.5,\n 46.916667\n ],\n [\n -87.5,\n 46.625\n ],\n [\n -87.375,\n 46.625\n ],\n [\n -87.375,\n 46.666667\n ],\n [\n -86.416667,\n 46.666667\n ],\n [\n -86.416667,\n 46.25\n ],\n [\n -87.375,\n 46.25\n ],\n [\n -87.375,\n 46.125\n ],\n [\n -87.5,\n 46.125\n ],\n [\n -87.5,\n 46.083333\n ],\n [\n -88.166667,\n 46.083333\n ],\n [\n -88.166667,\n 46.916667\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db6976fc","contributors":{"authors":[{"text":"Case, J. E.","contributorId":56625,"corporation":false,"usgs":true,"family":"Case","given":"J.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":269960,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gair, J. E.","contributorId":50891,"corporation":false,"usgs":true,"family":"Gair","given":"J. E.","affiliations":[],"preferred":false,"id":269959,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2639,"text":"wsp1784 - 1965 - Quality of surface waters in the lower Columbia River Basin","interactions":[],"lastModifiedDate":"2017-02-03T13:41:22","indexId":"wsp1784","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1784","title":"Quality of surface waters in the lower Columbia River Basin","docAbstract":"This report, made during 1959-60, provides reconnaissance data on the quality of waters in the lower Columbia River basin ; information on present and future water problems in the basin; and data that can be employed both in water-use studies and in planning future industrial, municipal, and agricultural expansion within this area. \r\n\r\nThe lower Columbia River basin consists of approximately 46,000 square miles downstream from the confluence of the Snake and Columbia Rivers The region can be divided into three geographic areas. The first is the heavily forested, sparsely populated mountain regions in which quality of water in general is related to geologic and climatological factors. The second is a semiarid plateau east of the Cascade Mountains; there differences in geology and precipitation, together with more intensive use of available water for irrigation, bring about marked differences in water quality. The third is the Willamette-Puget trough area in which are concentrated most of the industry and population and in which water quality is influenced by sewage and industrial waste disposal. \r\n\r\nThe majority of the streams in the lower Columbia River basin are calcium magnesium bicarbonate waters. In general, the rivers rising in the. Coast Range and on the west slope of the Cascade Range contain less than 100 parts per million of dissolved solids, and hardness of the water is less than 50 parts per million. Headwater reaches of the streams on the east slope of the Cascade Range are similar to those on the west slope; but, downstream, irrigation return flows cause the dissolved-solids content and hardness to increase. Most of the waters, however, remain calcium magnesium bicarbonate in type. \r\n\r\nThe highest observed dissolved-solids concentrations and also some changes in chemical composition occur in the streams draining the more arid parts of the area. In these parts, irrigation is chiefly responsible for increasing the dissolved-solids concentration and altering the chemical composition of the streams. The maximum dissolved-solids concentration and hardness of water observed in major irrigation areas were 507 and 262 parts per million, respectively, for the. Walla Walla River near Touchet, Wash. \r\n\r\nIn terms of the U.S. Salinity Laboratory Staff classification (1954, p. 80), water in most streams in the basin has low salinity and sodium hazards and is suitable for irrigation. A salt-balance problem does exist in the Hermiston-Stanfield, Oreg., area of the Umatilla River basin, and because of poor drainage, improper irrigation practices could cause salt-balance problems in the Willamette River Valley, Oreg., in which irrigation is rapidly increasing.\r\n\r\nPollution by sewage disposal has reached undesirable levels in the Walla Walla River, in the Willamette River from Eugene to Portland, Oreg., and in the Columbia River from Portland to Puget Island. In the lower reaches of the Willamette River, the pollution load from sewage and industrial-waste disposal at times depletes the dissolved oxygen in the water to concentrations below what is considered necessary for aquatic life. \r\n\r\nWater in most of the tributaries to the lower Columbia River is of excellent quality and after some treatment could be used for industrial and municipal supplies. The principal treatment required would be disinfection and turbidity removal.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1784","usgsCitation":"Santos, J.F., 1965, Quality of surface waters in the lower Columbia River Basin: U.S. Geological Survey Water Supply Paper 1784, iv, 78 p. :illus., maps. ;24 cm., https://doi.org/10.3133/wsp1784.","productDescription":"iv, 78 p. :illus., maps. ;24 cm.","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":28958,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1784/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138744,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1784/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a8be4b07f02db651877","contributors":{"authors":[{"text":"Santos, John F.","contributorId":21530,"corporation":false,"usgs":true,"family":"Santos","given":"John","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":145543,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1193,"text":"wsp1759F - 1965 - Water resources in the vicinity of municipalities on the eastern Mesabi Iron Range and the Vermilion Iron Range, northeastern Minnesota","interactions":[{"subject":{"id":52314,"text":"ofr6322 - 1963 - Water resources in the vicinity of municipalities on the Eastern Mesabi Iron Range and the Vermilion Iron Range, northeastern Minnesota","indexId":"ofr6322","publicationYear":"1963","noYear":false,"title":"Water resources in the vicinity of municipalities on the Eastern Mesabi Iron Range and the Vermilion Iron Range, northeastern Minnesota"},"predicate":"SUPERSEDED_BY","object":{"id":1193,"text":"wsp1759F - 1965 - Water resources in the vicinity of municipalities on the eastern Mesabi Iron Range and the Vermilion Iron Range, northeastern Minnesota","indexId":"wsp1759F","publicationYear":"1965","noYear":false,"chapter":"F","title":"Water resources in the vicinity of municipalities on the eastern Mesabi Iron Range and the Vermilion Iron Range, northeastern Minnesota"},"id":1}],"lastModifiedDate":"2021-11-02T21:27:50.468028","indexId":"wsp1759F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1759","chapter":"F","title":"Water resources in the vicinity of municipalities on the eastern Mesabi Iron Range and the Vermilion Iron Range, northeastern Minnesota","docAbstract":"Additional supplies of water are available near the municipalities on the eastern Mesabi Iron Range and the Vermilion Iron Range. On the eastern Mesabi Range the potential for additional development of both ground-water and surface-water supplies are good, and on the Vermilion Range the best potential for development is from surface-water resources.
\nThe most productive aquifers in the area of this report are the Biwabik Iron-Formation and the stratified glacial drift; Bast of Colby Lake the Biwabik Iron-Formation is not an important aquifer, and it is entirely absent on the Vermilion Range. Also, on the Vermilion Range the glacial drift is generally too thin to yield the quantities of water found on the Mesabi Range.
\nSurface-water supplies in the area of this report are good. An extensive network of river systems and many lakes form a large untapped potential supply. Records of flow from eight gaging stations are presented as are data from many wells and test holes.
\nGround water commonly has a high concentration of iron and manganese and is hard. Surface water generally has a high concentration of iron and is colored. Analyses of water from many sources are included.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Water resources of the Mesabi and Vermilion Iron Ranges","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1759F","usgsCitation":"Cotter, R.D., Young, H.L., Petri, L.R., and Prior, C.H., 1965, Water resources in the vicinity of municipalities on the eastern Mesabi Iron Range and the Vermilion Iron Range, northeastern Minnesota: U.S. Geological Survey Water Supply Paper 1759, Report: iv, 27 p.; 1 Plate: 31.18 x 23.60 inches, https://doi.org/10.3133/wsp1759F.","productDescription":"Report: iv, 27 p.; 1 Plate: 31.18 x 23.60 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":137952,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1759f/report-thumb.jpg"},{"id":26061,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1759f/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":278838,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1759f/plate-1.pdf"},{"id":391292,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24938.htm"}],"country":"United States","state":"Minnesota","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.62548828125,\n 47.09630525444073\n ],\n [\n -91.99676513671875,\n 47.09630525444073\n ],\n [\n -91.99676513671875,\n 47.945786463687185\n ],\n [\n -93.62548828125,\n 47.945786463687185\n ],\n [\n -93.62548828125,\n 47.09630525444073\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f4e4b07f02db5f08d4","contributors":{"authors":[{"text":"Cotter, R. D.","contributorId":89874,"corporation":false,"usgs":true,"family":"Cotter","given":"R.","email":"","middleInitial":"D.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":143334,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Young, H. L.","contributorId":23922,"corporation":false,"usgs":true,"family":"Young","given":"H.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":143331,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Petri, L. R.","contributorId":48944,"corporation":false,"usgs":true,"family":"Petri","given":"L.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143332,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Prior, C. H.","contributorId":57827,"corporation":false,"usgs":true,"family":"Prior","given":"C.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143333,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":2000,"text":"wsp1802 - 1965 - Fluvial sediment of the Mississippi River at St. Louis, Missouri","interactions":[],"lastModifiedDate":"2012-02-02T00:05:22","indexId":"wsp1802","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1802","title":"Fluvial sediment of the Mississippi River at St. Louis, Missouri","docAbstract":"An investigation of the fluvial sediment of the Mississippi River at St. Louis, Mo., was begun in 1948. Most data have been obtained only to determine the daily suspended-sediment discharge and the particle-size distribution of suspended sediment and bed material, but a few data have been obtained to study the flow resistance, the vertical distribution of sediment and velocity, and the bed-material discharge. \r\n\r\nThe flow of the Mississippi River at St. Louis is made up of the flows from the Missouri River, which had an average flow of 79,860 cubic feet per second for 1897-1958 at Hermann, Mo., and from the upper Mississippi River, which had an average flow of 91,890 cubic feet per second for 1928-58 at Alton, Il. The Missouri River is partly controlled by reservoirs that had a total capacity of 90,300,000 acre-feet in 1956, and the upper Mississippi River is partly controlled by lakes and reservoirs that had a total capacity of 4,890,000 acre-feet in 1956. The flows of the Missouri and upper Mississippi Rivers have not become mixed at St. Louis; so the river has a lateral gradient of suspended-sediment concentration. The concentration near the west bank has been as much as 2,400 parts per million greater than the concentration near the east bank. \r\n\r\nSuspended-sediment discharges from April 1948 to September 1958 ranged from 4,250 to 7,010,000 tons per day and averaged 496,000 tons per day. Mean concentrations for water years decreased steadily from 1,690 parts per million in 1949 to 403 parts per million in 1956, but they increased to 756 parts per million in 1958. Effects of new reservoirs in the Missouri River basin on the concentration have been obscured by the close relation of concentration to streamflow. Measured suspended-sediment discharge through September 1958 averaged 47 percent clay, 38 percent silt, and 15 percent sand. Variations of particle size were due mainly to differences in the source areas of the sediment. Most of the bed material in the main flow was between 0.125 and 1.000 millimeter in diameter. The average of median diameters was related to the discharge for periods of 1 year and longer. Geometric quartile deviations of the bed material ranged from 1.1 to 2.5 and averaged 1.5. \r\n\r\nThe mean elevation of the bed had a range of almost 10 feet and was related to the median diameter of bed material by the regression equation hb=363.0 - 7.8 d50 for which the standard error of estimate was 0.91 foot. \r\n\r\nThe resistance to flow as measured by Manning's n ranged from 0.024 to 0.041 and was related to the discharge and mean velocity but not to the shear velocity. Normal dune height is 2-8 feet, and average dune length is about 250 feet. When the resistance to flow was low, much of the bed was fairly fiat; a few dunes were present, but they were much longer than the average. For a given discharge during individual rises in stage, the gage height was lower for increasing discharge than for decreasing discharge even though the bed elevation was higher. The changes in gage height were not caused by changes in energy gradient due to changing discharge, by channel storage between the gage and the measuring section, nor by return of overbank flow; but they were probably caused by a combination of changes in roughness due to changing bed configuration and of changes in turbulence constant due to changing sediment concentration. Turbulence constants (Von Karman's k) computed from velocity measurements at 5-10 points in the vertical and from routine velocity measurements at 2 points in the vertical averaged 0.35 and 0.33, respectively. \r\n\r\nThe exponent z1 of the vertical distribution of concentration for different size ranges varied with about the 0.77 power of the fall velocity. Except for the difference between the theoretical variation and the actual variation of z1 with changing fall velocity, the theoretical equation for the vertical distribution of sediment concentration seems to apply reasonably well for the Miss","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1802","usgsCitation":"Jordan, P.R., 1965, Fluvial sediment of the Mississippi River at St. Louis, Missouri: U.S. Geological Survey Water Supply Paper 1802, viii, 89 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1802.","productDescription":"viii, 89 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":138367,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1802/report-thumb.jpg"},{"id":27444,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1802/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6aea9e","contributors":{"authors":[{"text":"Jordan, Paul Robert","contributorId":57819,"corporation":false,"usgs":true,"family":"Jordan","given":"Paul","email":"","middleInitial":"Robert","affiliations":[],"preferred":false,"id":144507,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1194,"text":"wsp1759C - 1965 - Water resources in the vicinity of municipalities on the west-central Mesabi Iron Range, northeastern Minnesota","interactions":[{"subject":{"id":52315,"text":"ofr6323 - 1963 - Water resources in the vicinity of municipalities on the West-Central Mesabi Iron Range, northeastern Minnesota","indexId":"ofr6323","publicationYear":"1963","noYear":false,"title":"Water resources in the vicinity of municipalities on the West-Central Mesabi Iron Range, northeastern Minnesota"},"predicate":"SUPERSEDED_BY","object":{"id":1194,"text":"wsp1759C - 1965 - Water resources in the vicinity of municipalities on the west-central Mesabi Iron Range, northeastern Minnesota","indexId":"wsp1759C","publicationYear":"1965","noYear":false,"chapter":"C","title":"Water resources in the vicinity of municipalities on the west-central Mesabi Iron Range, northeastern Minnesota"},"id":1}],"lastModifiedDate":"2019-12-30T10:07:58","indexId":"wsp1759C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1759","chapter":"C","title":"Water resources in the vicinity of municipalities on the west-central Mesabi Iron Range, northeastern Minnesota","docAbstract":"Additional supplies of water are available near the municipalities or the west-central Mesabi Iron Range. The largest sources are the ground-water aquifers in the Biwabik Iron-Formation and the stratified glacial drift. Areas of stratified drift that probably have good water potential have been outlined. Surface-water supplies are negligible in the eastern part of this area but increase toward the west. Flow records from one gaging station, results of discharge measurements at two miscellaneous sites, and data from many wells and test holes are presented.
\nMost of the ground water is hard and has a high concentration of iron and manganese. The surface water generally has a high concentration of. iron and is colored. Analyses of water from many sources are .shown.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1759C","collaboration":"Prepared in cooperation with the Minnesota Department of Iron Range Resources and Rehabilitation","usgsCitation":"Cotter, R.D., Young, H.L., Petri, L.R., and Prior, C.H., 1965, Water resources in the vicinity of municipalities on the west-central Mesabi Iron Range, northeastern Minnesota: U.S. Geological Survey Water Supply Paper 1759, Report: iv, 21 p.; 1 Plate: 24.50 x 28.50 inches, https://doi.org/10.3133/wsp1759C.","productDescription":"Report: iv, 21 p.; 1 Plate: 24.50 x 28.50 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":137953,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1759c/report-thumb.jpg"},{"id":26062,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1759c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26063,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1759c/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Minnesota","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.27667236328125,\n 47.338822694822\n ],\n [\n -93.19839477539062,\n 47.31741394628156\n ],\n [\n -93.043212890625,\n 47.31741394628156\n ],\n [\n -92.86056518554688,\n 47.40764414848437\n ],\n [\n -92.779541015625,\n 47.48287279099342\n ],\n [\n -92.82073974609375,\n 47.51349065484327\n ],\n [\n -92.88803100585938,\n 47.52832925298343\n ],\n [\n -92.9608154296875,\n 47.53852835471765\n ],\n [\n -93.043212890625,\n 47.511635534978225\n ],\n [\n -93.1585693359375,\n 47.447593738482304\n ],\n [\n -93.2464599609375,\n 47.37975438400816\n ],\n [\n -93.27667236328125,\n 47.338822694822\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7ee4b07f02db648595","contributors":{"authors":[{"text":"Cotter, R. D.","contributorId":89874,"corporation":false,"usgs":true,"family":"Cotter","given":"R.","email":"","middleInitial":"D.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":143338,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Young, H. L.","contributorId":23922,"corporation":false,"usgs":true,"family":"Young","given":"H.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":143335,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Petri, L. R.","contributorId":48944,"corporation":false,"usgs":true,"family":"Petri","given":"L.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143336,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Prior, C. H.","contributorId":57827,"corporation":false,"usgs":true,"family":"Prior","given":"C.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143337,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1192,"text":"wsp1759A - 1965 - Ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota","interactions":[{"subject":{"id":52311,"text":"ofr6319 - 1963 - The occurrence and quality of ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota","indexId":"ofr6319","publicationYear":"1963","noYear":false,"title":"The occurrence and quality of ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota"},"predicate":"SUPERSEDED_BY","object":{"id":1192,"text":"wsp1759A - 1965 - Ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota","indexId":"wsp1759A","publicationYear":"1965","noYear":false,"chapter":"A","title":"Ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota"},"id":1}],"lastModifiedDate":"2022-05-17T21:57:43.798429","indexId":"wsp1759A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1759","chapter":"A","title":"Ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota","docAbstract":"Within the Mesabi-Vermilion Iron Range area, water of good quality is available from the Biwabik Iron-Formation, from stratified drift, and from lakes and streams. About 700 bgy (billion gallons a year) leaves the area as surface water, of which about one-third comes from ground water.
\nLeached, oxidized, and fractured parts of the Biwabik Iron-Formation yield as much as 1,000 gpm (gallons per minute) to wells. Much of the permeable stratified drift within the area underlies the Ice-Contact region and the Horainal and Ice-Contact region, and several wells drilled in drift have been pumped at rates of more than 1,000 gpm.
\nParts of three major drainage basins lie within the area, and lakes compose about 5 percent of the area. Low-flow and flood-frequency data have been compiled for many of the streams. Large quantities of surface water are available from the Border-Lakes region and the Morainal and Ice-Contact region.
\nThe quality of ground water from the Biwabik Iron-Formation and from the drift is similar. The water is generally moderately siliceous, hard or very hard, and contains much iron and manganese. Surface water is generally soft, contains much iron, and is highly colored.
\nLarge uses of water in the area include: taconite processing (50 bgy), wash-ore processing (19 bgy), power plants (63 bgy), municipal water supplies (3 bgy) and paper processing (1 bgy). Optimum development of the water resources might be achieved by using streamflow in the spring and stunner and ground-water and surface-water storage in the fall and winter.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, DC","doi":"10.3133/wsp1759A","collaboration":"Prepared in cooperation with the Minnesota Department of Iron Range Resources and Rehabilitation","usgsCitation":"Cotter, R.D., Young, H.L., Petri, L.R., and Prior, C.H., 1965, Ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota: U.S. Geological Survey Water Supply Paper 1759, Document: iv, 35 p.; 1 Plate: 23.00 x 17.00 inches, https://doi.org/10.3133/wsp1759A.","productDescription":"Document: iv, 35 p.; 1 Plate: 23.00 x 17.00 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":400746,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24933.htm"},{"id":26060,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1759a/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26059,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1759a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137940,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1759a/report-thumb.jpg"}],"scale":"303000","country":"United States","state":"Minnesota","otherGeospatial":"Mesabi and Vermilion Iron Range area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.75,\n 48\n ],\n [\n -93.75,\n 47.089\n ],\n [\n -91.582,\n 47.089\n ],\n [\n -91.582,\n 48\n ],\n [\n -93.75,\n 48\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab1e4b07f02db66eaed","contributors":{"authors":[{"text":"Cotter, R. D.","contributorId":89874,"corporation":false,"usgs":true,"family":"Cotter","given":"R.","email":"","middleInitial":"D.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":143330,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Young, H. L.","contributorId":23922,"corporation":false,"usgs":true,"family":"Young","given":"H.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":143327,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Petri, L. R.","contributorId":48944,"corporation":false,"usgs":true,"family":"Petri","given":"L.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143328,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Prior, C. H.","contributorId":57827,"corporation":false,"usgs":true,"family":"Prior","given":"C.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143329,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1062,"text":"wsp1790A - 1965 - Floods of March-April 1960 in Eastern Nebraska and adjacent states","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1790A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1790","chapter":"A","title":"Floods of March-April 1960 in Eastern Nebraska and adjacent states","docAbstract":"Snowmelt floods, record breaking on many streams and outstanding in terms of total area affected and runoff volumes generated, occurred in late March and early April 1960 on Missouri River tributaries in adjacent parts of six states. In order of area affected, the States are Nebraska, South Dakota, Iowa, Kansas, Minnesota, and Missouri. \r\n\r\nFive lives were lost, and the estimated damage was $14 million. Main-stem reservoirs kept Missouri River stages substantially below potential unregulated levels. Without regulation by reservoirs, the stage at Sioux City and Omaha would have been about 9 feet higher than it was and the damage would have been many millions of dollars more than actually occurred. \r\n\r\nThe floods were caused by rapid melting of an extensive snow cover of unusual depth and water equivalent, augmented by light to moderate rains. Temperatures almost continuously below normal, beginning in late December and culminating in record lows at many places during the first half of March, resulted in the retention of record snow accumulations, much later and much farther south than normal. The snowfall in eastern Nebraska from December 27 to March 26 was about twice the annual average. The excessive snowfall and below-normal temperatures produced a record-breaking 75-day period of continuous snow cover at Omaha. \r\n\r\nA rapidly rising, eastward-moving temperature pattern late in March, in combination with an easterly orientation of many Nebraska streams, tended to magnify flood peaks. The rapid temperature rise started about March 18 in western Nebraska but not until March 26 in the eastern part of the State. As a consequence, flood discharges from the headwaters, often bearing heavy ice floes, arrived in the lower reaches simultaneously with or even ahead of the breakup of the unusually heavy ice cover and caused serious jamming. Comparisons of the peak discharges of the 1960 snowmelt floods with those of previous floods reveal several interesting facts. Peak discharges on the Missouri main stem were appreciably less than those in several other years, largely because of effective reservoir control of upstream runoff, but, many tributaries throughout the report area had maximum discharges for their periods of record. Particularly significant are comparisons at some stations for which historical flood data were available. For example, the peak discharge of the Platte River at Louisville, Nebr., was the greatest since at least 1881, and the peak on the Elkhorn River at Waterloo, Nebr., was the greatest snowmelt flood since at least 1912, although it was less than half of the rain peak of June 12, 1944. \r\n\r\nFollowing a characteristic pattern for snowmelt floods, the peaks on the smaller streams generally were not unusual, but the cumulative effect of widespread high runoff throughout the stream systems caused higher and more outstanding peaks in the larger basins. Peaks due to local rains of high intensity often are more significant for small areas. \r\n\r\nSnowmelt floods occur less frequently than rainfall floods in most basins of this flood area.. Studies made for this report show that an average of only about one out of every four maximum annual flood discharges in the report area results primarily from snowmelt. But for streams flowing from north to south in South Dakota and Iowa, the ratio of snowmelt peaks to rainfall peaks is higher. \r\n\r\nComparisons of 1960 flood volumes with those for previous floods are even more striking than peak-discharge comparisons. Flood volumes at eight selected stations for the maximum 20-day period during March and April 1960 exceeded all previous 20-day volumes with only one exception; the ratios ranged from 3.11 for Vermillion River near Wakonda, S. Dak., to 0.93 for Elkhorn River at Waterloo, Nebr. The ratio of the 20-day volume to the 1960 annual runoff for the same group of stations ranged from 20 percent at Niobrara River near Spencer, Nebr., to 74 percent on the Vermillion River. For the lat","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey ;","doi":"10.3133/wsp1790A","usgsCitation":"Brice, H., and West, R., 1965, Floods of March-April 1960 in Eastern Nebraska and adjacent states: U.S. Geological Survey Water Supply Paper 1790, v, 144 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1790A.","productDescription":"v, 144 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138100,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1790a/report-thumb.jpg"},{"id":25740,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1790a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25741,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1790a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d9e4b07f02db5df9c2","contributors":{"authors":[{"text":"Brice, H.D.","contributorId":41406,"corporation":false,"usgs":true,"family":"Brice","given":"H.D.","email":"","affiliations":[],"preferred":false,"id":143112,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"West, R.E.","contributorId":27031,"corporation":false,"usgs":true,"family":"West","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":143111,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2017,"text":"wsp1809O - 1965 - Delaware River water quality Bristol to Marcus Hook, Pennsylvania, August 1949 to December 1963","interactions":[],"lastModifiedDate":"2017-06-26T08:23:46","indexId":"wsp1809O","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1809","chapter":"O","title":"Delaware River water quality Bristol to Marcus Hook, Pennsylvania, August 1949 to December 1963","docAbstract":"During the 14-year period from August 1949 to July 1963, the U.S. Geological Survey, in cooperation with the city of Philadelphia, collected samples of river water once each month in the 43-mile reach of the Delaware River from Bristol to Marcus Hook, Pa., and daily at Trenton, 10 miles upstream from Bristol. This part of the Delaware is an estuary into which salt water is brought by tides; fresh water flows into the estuary at Trenton, NJ, and farther downstream from the Schuylkill River and other tributaries of the Delaware.\r\n\r\n In March, April, and May, when fresh-water flow is high, the average concentration of dissolved solids in the water at Bristol was 76 ppm (parts per million), and at Marcus Hook 112 PPM In August and September, streamflow is lower, and the average concentration of dissolved solids increased to 117 PPM at Bristol and 804 PPM at Marcus Hook. Major salinity invasions of the Delaware River occurred in 1949, 1953, 1954, 1957, and 1963. In each of these years the fresh-water flow into the tidal river at Trenton was low during the period from July to October. The greatest dissolved-solids concentrations in these monthly samples were 160 PPM at Bristol and 4,000 PPM at Marcus Hook.\r\n\r\n At times the dissolved-oxygen concentration of the river water has become dangerously low, especially in that reach of the river between Wharton Street and League Island. At the Benjamin Franklin Bridge, one-third of the samples of river water were less than 30 percent saturated with oxygen; however, no trend, either for better or for worse, was apparent during the 14-year period.\r\n\r\n It is useful now to summarize these monthly analyses for the period 1949-63 even though a much more detailed description of water quality in this reach of the estuary will soon become available through the use of recording instrumental conditions. This compendium of water-quality data is useful as an explicit statement of water quality during the 14-year study period and is valuable for directing attention to water-quality problems for selecting instrument sites, and for making comparative studies with the more detailed information which is already being obtained with the aid of recording instruments.","language":"English","publisher":"United States Government Printing Office","doi":"10.3133/wsp1809O","usgsCitation":"Keighton, W.B., 1965, Delaware River water quality Bristol to Marcus Hook, Pennsylvania, August 1949 to December 1963: U.S. Geological Survey Water Supply Paper 1809, iv, 57 p. :ill. ;23 cm., https://doi.org/10.3133/wsp1809O.","productDescription":"iv, 57 p. :ill. ;23 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":137596,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1809o/report-thumb.jpg"},{"id":27484,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1809o/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fee4b07f02db5f753a","contributors":{"authors":[{"text":"Keighton, Walter B.","contributorId":81877,"corporation":false,"usgs":true,"family":"Keighton","given":"Walter","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":144535,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1197,"text":"wsp1759E - 1965 - Water resources in the vicinity of municipalities on the east-central Mesabi Iron Range, northeastern Minnesota","interactions":[{"subject":{"id":52313,"text":"ofr6321 - 1963 - Water resources in the vicinity of muncipalities on the East-Central Mesabi Iron Range, northeastern Minnesota","indexId":"ofr6321","publicationYear":"1963","noYear":false,"title":"Water resources in the vicinity of muncipalities on the East-Central Mesabi Iron Range, northeastern Minnesota"},"predicate":"SUPERSEDED_BY","object":{"id":1197,"text":"wsp1759E - 1965 - Water resources in the vicinity of municipalities on the east-central Mesabi Iron Range, northeastern Minnesota","indexId":"wsp1759E","publicationYear":"1965","noYear":false,"chapter":"E","title":"Water resources in the vicinity of municipalities on the east-central Mesabi Iron Range, northeastern Minnesota"},"id":1}],"lastModifiedDate":"2018-03-05T12:34:53","indexId":"wsp1759E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1759","chapter":"E","title":"Water resources in the vicinity of municipalities on the east-central Mesabi Iron Range, northeastern Minnesota","docAbstract":"Additional supplies of water are available near the municipalities on the east-central Mesabi Iron Range. Both ground water and surface water offer good potential supplies. For the ground-water supplies, the most productive aquifers are the Biwabik Iron Formation and the stratified glacial drift. Surface-water supplies are variable. Streams in the western part of the report area are too small to yield supplies of importance, but lakes are a good potential supply. Eveleth and Gilbert are the only towns presently utilizing this source. In the eastern part of the area of this report, the Pike and Embarrass Rivers offer good potential supplies. Flow records from two gaging stations are presented as are data from many wells and test holes. Surface water generally has a high concentration of iron and is colored. Most ground water has a high concentration of iron and manganese and is hard. Analyses of water from many sources are presented.
","language":"English","publisher":"U.S. Government Publishing Office","publisherLocation":"Washington, DC","doi":"10.3133/wsp1759E","collaboration":"Prepared in cooperation with the Minnesota Department of Iron Range Resources and Rehabilitation","usgsCitation":"Cotter, R.D., Young, H.L., Petri, L.R., and Prior, C.H., 1965, Water resources in the vicinity of municipalities on the east-central Mesabi Iron Range, northeastern Minnesota: U.S. Geological Survey Water Supply Paper 1759, Document: iv, 23 p.; Plate: 28.00 x 27.25 inches, https://doi.org/10.3133/wsp1759E.","productDescription":"Document: iv, 23 p.; Plate: 28.00 x 27.25 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":137956,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1759e/report-thumb.jpg"},{"id":26068,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1759e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26069,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1759e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Minnesota","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -92.6,\n 47.583333\n ],\n [\n -92.6,\n 47.491667\n ],\n [\n -92.583333,\n 47.491667\n ],\n [\n -92.583333,\n 47.391667\n ],\n [\n -92.491667,\n 47.391667\n ],\n [\n -92.491667,\n 47.441667\n ],\n [\n -92.375,\n 47.441667\n ],\n [\n -92.375,\n 47.5\n ],\n [\n -92.3,\n 47.5\n ],\n [\n -92.3,\n 47.558333\n ],\n [\n -92.458333,\n 47.558333\n ],\n [\n -92.458333,\n 47.5\n ],\n [\n -92.491667,\n 47.5\n ],\n [\n -92.491667,\n 47.491667\n ],\n [\n -92.508333,\n 47.491667\n ],\n [\n -92.508333,\n 47.583333\n ],\n [\n -92.6,\n 47.583333\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f4e4b07f02db5f08db","contributors":{"authors":[{"text":"Cotter, R. D.","contributorId":89874,"corporation":false,"usgs":true,"family":"Cotter","given":"R.","email":"","middleInitial":"D.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":143350,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Young, H. L.","contributorId":23922,"corporation":false,"usgs":true,"family":"Young","given":"H.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":143347,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Petri, L. R.","contributorId":48944,"corporation":false,"usgs":true,"family":"Petri","given":"L.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143348,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Prior, C. H.","contributorId":57827,"corporation":false,"usgs":true,"family":"Prior","given":"C.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143349,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1195,"text":"wsp1759B - 1965 - Water resources in the vicinity of municipalities on the western Mesabi Iron Range, northeastern Minnesota","interactions":[{"subject":{"id":52316,"text":"ofr6324 - 1963 - Water resources in the vicinity of municipalities on the Western Mesabi Iron Range, northeastern Minnesota","indexId":"ofr6324","publicationYear":"1963","noYear":false,"title":"Water resources in the vicinity of municipalities on the Western Mesabi Iron Range, northeastern Minnesota"},"predicate":"SUPERSEDED_BY","object":{"id":1195,"text":"wsp1759B - 1965 - Water resources in the vicinity of municipalities on the western Mesabi Iron Range, northeastern Minnesota","indexId":"wsp1759B","publicationYear":"1965","noYear":false,"chapter":"B","title":"Water resources in the vicinity of municipalities on the western Mesabi Iron Range, northeastern Minnesota"},"id":1}],"lastModifiedDate":"2016-05-06T10:48:02","indexId":"wsp1759B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1759","chapter":"B","title":"Water resources in the vicinity of municipalities on the western Mesabi Iron Range, northeastern Minnesota","docAbstract":"Additional supplies of water are available near the municipalities on the western Mesabi Iron Range. Potential yields from both ground-water and surface-water sources are good. The most productive aquifers for ground-water supplies are the Biwabik Iron-Formation and the stratified glacial drift. Areas of stratified drift believed to have good water potential have been outlined. The most abundant surface-water supplies in the area of this report are from the Mississippi River and its tributaries.
\nThe ground water is generally hard and has a high concentration of iron and manganese. The surface water is generally high in iron and is colored. Analyses of water from many sources are included.
\nData from many wells and test holes are given as are flow data for two discharge stations.
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