The Wharton Tract is an area of 150 square miles located in the Mullica River basin in southern New Jersey's Pine Barrens region. The tract is a relatively flat, low-lying, generally sandy area containing shallowly incised streams. The larger streams are commonly bordered by swamps. The tract was purchased by the State primarily as a water-supply preserve, but also for conservation and recreational purposes.
\nMean streamflow at three continuous record gaging stations in the Wharton Tract is: Mullica River near Batsto (46.1-square mile drainage area), 6 mgd (million gallons per day); Batsto River at Batsto (70.5-square mile drainage area), 81 mgd; Oswego River at Harrisville (64.0-square mile drainage area), 55 mgd. Thus mean discharge from this 180.6-sq mi (square mile) area is 202 mgd or 1.12 mgd per sq mi.
\nPrincipal aquifers in the Wharton Tract and Mullic River basin are in the Kirkwood Formation of middle Miocene age, Cohansey Sand of Miocene(?) and Pliocene(?) age, and in overlying hydraulically connected deposits of Quaternary age.
\nThe Kirkwood Formation is composed of sand, silt, and clay. Diverse lithologies represent deposition in different environments such as nearshore marine, barrier bar, lagoonal, estuarine, and tidal marsh. Hydraulic characteristics of the Kirkwood in the Mullica River basin are virtually unknown. Most Kirkwood aquifers in the basin are believed to be hydraulically connected with the overlying Cohansey Sand.
\nThe Cohansey Sand is dominantly a quartz sand containing minor amounts of pebbly sand, silty sand, and interbedded clay. Almost all of the Wharton Tract and most of the Mullica River basin lie within the sandier area of the Cohansey, which contains approximately 75 percent sand beds and 25 percent silt and clay beds. Data from test drilling show that the upper 100 feet of sediments in the Wharton Tract contain about 93 percent sand beds, 3.5 percent clay beds, and 3.5 percent silt beds. The Cohansey in the Tract ranges in thickness from less than 50 feet to about 180 feet; the average thickness is about 125 feet.
\nThe Cohansey Sand is believed to be, in overall aspect, a deltaic deposit. It contains materials that were deposited locally in nearshore-marine, fluvial, estuarine, lagoonal, and beach environments.
\nThe hydraulic conductivity of Cohansey aquifer material ranges from about 90 to 250 feet per day (660 to 1,885 gallons per day per square foot) in southern New Jersey. One aquifer test in the Wharton Tract gives an average value of 130 feet per day (1,000 gallons per day per square foot). The transmissivity of the Cohansey Sand aquifer through most of the Wharton Tract is typically between 10,000 and 20,000 square feet per day (75,000 and 150,000 gallons per day per foot).
\nDeposits of Quaternary age form a discontinuous veneer lying unconformably above the Cohansey Sand. The most important hydrologic function of most of these deposits is to absorb precipitation and transmit the water to the underlying Cohansey Sand. Thicker deposits of estuarine sand and clay of the Cape May Formation fill a channel in the underlying Cohansey Sand along the lower reaches of the Mullica River. This channel deposit is 85 feet thick near Batsto.
\nGround water and surface water in the Mullica River basin are low in dissolved solids, generally less than 50 mg/1 (milligrams per liter). Iron concentrations are generally high, up to 49,000 micrograms per liter (49 mg/1) in ground water and up to 7,100 micrograms per liter (7.1 mg/1) in the streams. The water is acidic as indicated by typical pH values of from 4.5 to 6.5. Color of the surface water is commonly high, ranging from 3 - 150 platinum-cobalt units. After appropriate treatment these waters are acceptable for most uses.
\nThe Wharton Tract is well situated to support the growing water needs of nearby New Jersey communities. Maximum development of water can be achieved by conjunctive use of ground and surface water. During most of the year, some water would be withdrawn either directly from streams or from adjacent wells. During periods of low flow during summer or fall water would be pumped from wells farther from the stream~. From analysis of flow-duration curves it is estimated that 70 mgd of water could be developed with minimal effect upon low flows in the half of the tract above the gaging stations on the Mullica and Batsto Rivers. The quantity available in the entire tract is greater, possibly in the order of 150 mgd. With augmentation of streamflow by pumping from ground water, it is likely that considerably more water could be safely used on a perennial basis.
\nA possibility exists for multiple use of the water resources of the Mullica River through construction of an inexpensive tide barrier at the Garden State Parkway. This would create a fresh water lake in a State forest, park, and recreational area, which would also provide a flexible and economical water supply for much of the Atlantic coastal resort development.
","language":"English","publisher":"State of New Jersey Department of Environmental Protection, Division of Water Resources","collaboration":"Prepared in cooperation with United States Department of the Interior Geological Survey","usgsCitation":"Rhodehamel, E.C., 1973, Geology and water resources of the Wharton Tract and the Mullica River basin in southern New Jersey: Special Report 36, 58 p.","productDescription":"58 p.","numberOfPages":"65","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":287918,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":287917,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70106983/report.pdf"}],"country":"United States","state":"New Jersey","otherGeospatial":"Mullica River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -75.7768,38.8517 ], [ -75.7768,40.7423 ], [ -73.8448,40.7423 ], [ -73.8448,38.8517 ], [ -75.7768,38.8517 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"537b27f4e4b0929ba496ab78","contributors":{"authors":[{"text":"Rhodehamel, Edward C.","contributorId":38135,"corporation":false,"usgs":true,"family":"Rhodehamel","given":"Edward","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":493827,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70047467,"text":"70047467 - 1973 - Lake Okeechobee seepage monitoring network","interactions":[],"lastModifiedDate":"2025-04-10T17:47:21.905845","indexId":"70047467","displayToPublicDate":"1973-01-01T16:11:00","publicationYear":"1973","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}},"seriesNumber":"FL 73-018","displayTitle":"Lake Okeechobee Seepage Monitoring Network","title":"Lake Okeechobee seepage monitoring network","docAbstract":"This report summarizes the data collected at the five original monitoring sites along the south shore of Lake Okeechobee from January 29, 1970 to June 28, 1972. In order to use the hydrographs in this report to full advantage, they should be studied in conjunction with Meyer's graphs and text (1971). During steady-state conditions, water seeps from the lake through the filtercake and through the aquifers beneath the dike. At those sites where the filtercake is missing, or has about the same permeability as the aquifers, the seepage from the lake is about equivalent to the flow through the aquifers. Present data are insufficient to determine whether or not filtercake buildup has reduced seepage. No appreciable change in drainage occurred during the observed period.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Tallahassee, FL","doi":"10.3133/70047467","usgsCitation":"McKenzie, D.J., 1973, Lake Okeechobee seepage monitoring network: Open-File Report FL 73-018, 64 p., https://doi.org/10.3133/70047467.","productDescription":"64 p.","numberOfPages":"64","costCenters":[],"links":[{"id":277873,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70047467/coverthb.jpg"},{"id":276140,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70047467/ofr-fl-73018.pdf","text":"Report","size":"14.6 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR FL 73-018"}],"country":"United States","state":"Florida","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -81.143229,26.624789 ], [ -81.143229,27.207276 ], [ -80.568544,27.207276 ], [ -80.568544,26.624789 ], [ -81.143229,26.624789 ] ] ] } } ] }","contact":"Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
The upper Housatonic River basin report area has an abundant supply of water of generally good quality, which is derived from precipitation on the area and streams entering the area. Annual precipitation has averaged about 46 inches over a 30-year period. Of this, approximately 22 inches of water is returned to the atmosphere each year by evaporation and transpiration; the remainder flows overland to streams or percolates downward to the water table and ultimately flows out of the report area in the Housatonic River or in smaller streams tributary to the Hudson River. During the autumn and winter precipitation normally is sufficient to cause a substantial increase in the amount of water stored in surface reservoirs and in aquifers, whereas in the summer, losses through evaporation and transpiration result in sharply reduced streamflow and lowered ground-water levels. Mean monthly storage of water in November is 2.8 inches more than it is in June.
\nThe amount of water that flows into, through, and out of the report area represents the total amount potentially available for use ignoring reuse. For the 30-year period 1931 through 1960, the annual runoff from precipitation has averaged 24 inches (294 billion gallons). During the same period, inflows from Massachusetts and New York have averaged 220 and 64 billion gallons per year, respectively. A total average annual runoff of 578 billion gallons is therefore available. Although runoff indicates the total amount of water potentially available, it is rarely feasible to use all of it. On the other hand, with increased development, some water may be reused several times.
\nThe water availability may be tapped as it flows through the area or is temporarily stored in streams, lakes, and aquifers. The amounts that can be developed differ from place to place and time to time, depending on the amount of precipitation, on the size of drainage area, on the thickness, transmissivity, and areal extent of aquifers, and on the variations in chemical and physical quality of water.
\nDifferences in precipitation cause differences in the amount of streamflow whereas differences in the proportion of stratified drift affect its timing.
\nWater can be obtained from wells almost anywhere in the area, but the amount obtainable at any particular point depends on the type and water-bearing properties of the aquifers tapped.
\nStratified-drift aquifers are the only ones generally capable of yielding more than 100 gpm (gallons per minute) to individual wells. Drilled, screened wells tapping this unit yield from 17 to 1,400 gpm, with a median yield of 200 gpm.
\nTill and bedrock are widespread but generally provide only small supplies of water. Till is tapped in a few places by dug wells, which can yield small supplies of only a few hundred gallons per day throughout all or most of the year. Bedrock is the chief aquifer for privately owned domestic and rural supplies; it is tapped by drilled wells, about 90 percent of which will supply at least 2 gpm. Only 1 of 10 bedrock wells, however, will supply more than 30 gpm.
\nThe amount of ground water potentially available in the report area depends upon the thickness and hydraulic properties of aquifers, the amount of salvageable natural discharge of ground water, and the quantity of water available by induced infiltration from streams and lakes. From data on transmissivity, thickness, recharge, well performance, and streamflow, preliminary estimates of ground-water availability can be made for most stratified-drift aquifers in the report area. Long-term yields estimated for eight areas of stratified drift especially favorable for development of large ground-water supplies ranged from 0.6 to 5 mgd (million gallons per day). Detailed site studies are needed to verity these estimates and to determine optimum yields, drawdowns, and spacing of individual wells before major ground-water development is undertaken in these or other areas.
\nThe chemical quality of water in the report area is generally good; carbonate-bedrock units exert considerable local influence on water quality. Samples of naturally occurring surface water collected at 24 sites during low flow averaged 90 mg/l (milligrams per liter) dissolved solids and 60 mg/l hardness. Water from wells is generally more highly mineralized than naturally occurring water from streams. About 37 percent of the wells sampled yielded water with more than 200 mg/l dissolved solids and 50 percent yielded water with more than 120 mg/l hardness. These concentrations reflect the high degree of mineralization of ground water in carbonate bedrock and unconsolidated deposits derived from this bedrock. The larger streams, which transport varying amounts of industrial and domestic effluents, averaged about 150 mg/l dissolved solids and 90 mg/l hardness.
\nIron and manganese concentrations in both ground water and surface water at some places exceed recommended limits for domestic and industrial use. Most wells in the report area yield water with little or no iron or manganese. In certain localities however, the probability is high of encountering water with excessive concentrations of these constituents. Schists, especially the unit in the northwestern corner of the basin, are the likely sources of water with excessive iron and manganese.
\nIron concentrations in naturally occurring stream water exceed 0.3 mg/l under low-flow conditions at 29 percent of the sites sampled. These excessive concentrations result from discharge of iron-bearing water from aquifers or from swamps where iron is released from decaying vegetation.
\nWater temperature in the larger streams ranges from 0°C (degrees Celsius) to about 28°C. Ground water between 30 feet and 200 feet below the land surface has a relatively constant temperature, usually between 8°C and 11°C.
\nThe quantity of suspended sediment transported by streams under natural conditions is negligible. Even in streams affected by man, turbidity is rarely a problem.
\nThe total amount of water used in the report area for all purposes during 1967 was about 6,360 million gallons, or 140 gpd per person. Public supplies furnished the domestic needs of nearly half the population of the area. All of the 14 public supplies sampled provided water that meets the drinking water standards of the U.S. Public Health Service.
","language":"English","publisher":"Connecticut Department of Environmental Protection","collaboration":"Prepared by the U.S. Geological Survey in cooperation with the Connecticut Department of Environmental Protection","usgsCitation":"Cervione, M.A., Mazzaferro, D.L., and Melvin, R.T., 1972, Water resources inventory of Connecticut Part 6: Upper Housatonic River basin: Connecticut Water Resources Bulletin 21, Report: viii, 82 p.; 6 Plates: 31.73 x 39.58 inches and smaller.","productDescription":"Report: viii, 82 p.; 6 Plates: 31.73 x 39.58 inches and smaller","numberOfPages":"92","costCenters":[],"links":[{"id":258809,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/ctwrb/0021/report.pdf","size":"26735","linkFileType":{"id":1,"text":"pdf"}},{"id":258810,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ctwrb/0021/report-thumb.jpg"},{"id":285991,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038249/plate-b-2.pdf"},{"id":285992,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038249/plate-b-3.pdf"},{"id":285989,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038249/plate-a.pdf"},{"id":285990,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038249/plate-b-1.pdf"},{"id":285993,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038249/plate-c.pdf"},{"id":285994,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038249/plate-d.pdf"}],"scale":"125000","country":"United States","state":"Connecticut","otherGeospatial":"Housatonic River Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -73.566667,41.25 ], [ -73.566667,42.066667 ], [ -73.166667,42.066667 ], [ -73.166667,41.25 ], [ -73.566667,41.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bcb7ce4b08c986b32d699","contributors":{"authors":[{"text":"Cervione, Michael A. Jr.","contributorId":23988,"corporation":false,"usgs":true,"family":"Cervione","given":"Michael","suffix":"Jr.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":463735,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mazzaferro, David L.","contributorId":89539,"corporation":false,"usgs":true,"family":"Mazzaferro","given":"David","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":463736,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Melvin, Robert T.","contributorId":99808,"corporation":false,"usgs":true,"family":"Melvin","given":"Robert","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":463737,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":48036,"text":"ofr72164 - 1972 - Low flows and temperatures of streams in the Seattle-Tacoma urban complex and adjacent areas, Washington","interactions":[],"lastModifiedDate":"2012-07-19T01:01:48","indexId":"ofr72164","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-164","title":"Low flows and temperatures of streams in the Seattle-Tacoma urban complex and adjacent areas, Washington","docAbstract":"Data on the minimum flows of streams and water temperature are necessary for the proper planning and development of the water resources of urban Seattle-Tacoma and adjacent areas. The data on low flows are needed for such purposes as (1) designing and operating municipal and industrial water-supply systems; (2) classifying streams as to their potential for waste disposal; (3) defining the amount of water available for irrigation, for maintaining streamflow as required by law or agreement, and for fish propagation; and (4) designing water-storage facilities. Data on stream temperatures are important to many water users because of the many biological, chemical, and physical properties of water that are dependent on temperature. Agricultural and domestic users as well as municipal, industrial and fishery agencies are concerned with water temperatures. In this report, low-flow data are accompanied by information on seasonal variations in water temperatures at sites selected as representing regional stream-temperature patterns. Because low flows and high water temperatures commonly occur together, they may impose constraints on various uses of the region's streams. The following discussion deals first with low-flow trends in the region, then with stream temperatures, and finally with some of the resulting constraints.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Tacoma, WA","doi":"10.3133/ofr72164","usgsCitation":"Hidaka, F., 1972, Low flows and temperatures of streams in the Seattle-Tacoma urban complex and adjacent areas, Washington: U.S. Geological Survey Open-File Report 72-164, 11 p.; 1 Plate: 58 x 77 cm., https://doi.org/10.3133/ofr72164.","productDescription":"11 p.; 1 Plate: 58 x 77 cm.","costCenters":[],"links":[{"id":170293,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1972/0164/report-thumb.jpg"},{"id":84806,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0164/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84807,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0164/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"250000","country":"United States","state":"Washington","city":"Seattle;Tacoma","otherGeospatial":"Cedar River;Deschutes River;Flett Creek;Green River;Nisqually River;North Creek;Puyallup River;Quilceda Creek;Sammamish River;Skykomish River;Snoqualmie River;Sultan River;Taylor Creek;White River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -123,46.666666666666664 ], [ -123,48.166666666666664 ], [ -121.58333333333333,48.166666666666664 ], [ -121.58333333333333,46.666666666666664 ], [ -123,46.666666666666664 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a74e4b07f02db644921","contributors":{"authors":[{"text":"Hidaka, F.T.","contributorId":48542,"corporation":false,"usgs":true,"family":"Hidaka","given":"F.T.","email":"","affiliations":[],"preferred":false,"id":236709,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2640,"text":"wsp1999L - 1972 - Factors contributing to unusually low runoff during the period 1962-68 in the Concho River Basin, Texas","interactions":[],"lastModifiedDate":"2017-06-14T16:52:05","indexId":"wsp1999L","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1999","chapter":"L","title":"Factors contributing to unusually low runoff during the period 1962-68 in the Concho River Basin, Texas","docAbstract":"To determine the reasons for the unusually low runoff in the Concho River basin during the period 1962-68, the physical developments and climatic changes in the basin were identified and related to changes in the regimen of streamflow.
\nLand use, brush infestation, and land-treatment practices have not caused significant changes in the rainfall-runoff relationship.
\nThe use of surface water for irrigation has increased very little during the past 70 years, and although the use of ground water for irrigation has greatly increased in the past 25 years, springflow has not been significantly diminished. The base flow of the streams is materially reduced by surface-water irrigation diversions. Diversions for municipal and industrial use have increased rapidly, but these diversions affect only the streamflow downstream from San Angelo.
\nStatistical analyses showed the annual rainfall to be highly variable, with little serial correlation. Records of rainfall during the period 1943-68 are significantly different in character from previous long-term records. The frequency of monthly rainfall equal to or greater than 2.0 inches during the period 1943-68, and especially during the period 1962-68, was significantly less than the long-term averages.
\nAnalyses of annual runoff data, adjusted for depletions, show large variations in annual runoff. Coefficients of variation ranged from 0.8 to 1.4, and first-order serial correlations ranged from 0.01 to 0.28. The estimated recurrence interval of the 1962-68 drought is about 200 years.
\nThe analyses of rainfall-intensity and runoff data indicate that the basic cause for the relatively low runoff during the period 1962-68 was the lack of high-intensity, long-duration storms rather than any physical changes or agricultural practices in the watershed
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1999L","collaboration":"Prepared in cooperation with the Texas Water Development Board","usgsCitation":"Sauer, S.P., 1972, Factors contributing to unusually low runoff during the period 1962-68 in the Concho River Basin, Texas: U.S. Geological Survey Water Supply Paper 1999, v, 48 p., https://doi.org/10.3133/wsp1999L.","productDescription":"v, 48 p.","numberOfPages":"61","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":28959,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1999l/report.pdf","text":"Report","size":"924.83 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":138600,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1999l/report-thumb.jpg"}],"country":"United States","state":"Texas","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -101.2335205078125,\n 32.18026188320708\n ],\n [\n -101.3104248046875,\n 32.19885712788488\n ],\n [\n -101.5850830078125,\n 32.16631295696736\n ],\n [\n -101.788330078125,\n 32.10584293285769\n ],\n [\n -101.87072753906249,\n 32.05930026106166\n ],\n [\n -102.337646484375,\n 31.316101383495624\n ],\n [\n -102.3101806640625,\n 31.09998179374943\n ],\n [\n -102.2222900390625,\n 30.798474179567823\n ],\n [\n -102.1234130859375,\n 30.56699087315334\n ],\n [\n -101.700439453125,\n 30.36813582872057\n ],\n [\n -101.3543701171875,\n 30.30176068632071\n ],\n [\n -100.8050537109375,\n 30.315987718557867\n ],\n [\n -100.36560058593749,\n 30.330212685432734\n ],\n [\n -99.986572265625,\n 30.401306519203583\n ],\n [\n -99.7833251953125,\n 30.5717205651999\n ],\n [\n -99.635009765625,\n 30.72294882477251\n ],\n [\n -99.635009765625,\n 30.897511207369128\n ],\n [\n -99.6844482421875,\n 31.147006308556566\n ],\n [\n -99.744873046875,\n 31.283245492650792\n ],\n [\n -99.854736328125,\n 31.587894464070395\n ],\n [\n -99.9700927734375,\n 31.695455797778713\n ],\n [\n -100.1129150390625,\n 31.89621446335144\n ],\n [\n -100.1678466796875,\n 31.91953017247695\n ],\n [\n -101.2335205078125,\n 32.18026188320708\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a04e4b07f02db5f85f8","contributors":{"authors":[{"text":"Sauer, Stanley P.","contributorId":38966,"corporation":false,"usgs":true,"family":"Sauer","given":"Stanley","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":145544,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":14667,"text":"ofr72230 - 1972 - Regional and other general factors bearing on evaluation of earthquake and other geologic hazards to coastal communities of southeastern Alaska","interactions":[],"lastModifiedDate":"2024-02-09T20:07:02.07676","indexId":"ofr72230","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-230","title":"Regional and other general factors bearing on evaluation of earthquake and other geologic hazards to coastal communities of southeastern Alaska","docAbstract":"The great Alaska earthquake of March 27, 1964, brought into sharp focus the need for engineering geologic studies in seismically active regions. As a result, nine communities in southeastern Alaska were selected for reconnaissance investigations as an integral part of an overall program to evaluate earthquake and other geologic hazards in most of the larger Alaska coastal communities. This report gives background information on the regional and other general factors that bear on these evaluations.
Southeastern Alaska, about 525 miles long and averaging about 125 miles in width, consists of a narrow mainland strip and numerous islands. For the most part, it is a region of rugged relief with numerous glaciers capping many of the higher mountainous areas and with long linear fiords forming the inland waterways. A maritime climate prevails with mild winters and cool summers. The southeastern part of the region receives the highest precipitation in the continental United States. Ketchikan, with a population of 6,994 in 1970, is the largest city. Geology and structure of the area are complex. Igneous, metamorphic, and sedimentary rocks crop out and range in age from Paleozoic to Tertiary. Surficial deposits of Pleistocene and Holocene age mantle many areas.
All of southeastern Alaska, except probably the highest peaks, was covered by glacier ice advances of late Pleistocene age. Major deglaciation was well advanced by 10,000 years ago--a time which approximately marks the end of the Pleistocene and the beginning of the Holocene. There followed a period of warm climate called the Hypsithermal, which in southeastern Alaska began 7,000-8,000 years ago and ended about 4,800-3,500 years ago. Glaciers in most places receded back of their present positions. The Hypsithermal was followed by an interval (termed Neoglaciation) of cooler climate and resurgence of glacier ice which continues to the present, although most glaciers are now rapidly receding.
During the past 10,000 years worldwide sea level has risen about 100 feet, but during the past 4,000 years it has risen only about 10 feet or about 0.03 inch per year. With sea level used as a datum, the amount of sea-level rise must be added to the apparent uplift of land for the time under consideration to determine the actual amount of land uplift.
The widespread presence of emergent marine deposits, several hundred feet above sea level, demonstrates that the land in southeastern Alaska has been uplifted since the last major deglaciation. The greatest known has been uplifted since the last major deglaciation. The greatest known uplift is in the vicinity of Juneau where glaciomarine deposits are present 750 feet above present sea level. Part of southeastern Alaska is presently undergoing one of the most rapid rates of uplift of any place in the world. The fastest emergence is occurring in the Glacier Bay area where the land is being uplifted relative to sea level approximately 3.9 cm per year. Most or all of the uplift appears to be due to rebound as a result of deglaciation.
Southeastern Alaska lies within the circum-Pacific earthquake belt, one of the world's greatest zones of seismic activity. During historic time, there have been five earthquakes in the region with magnitudes of 8 or greater, three with magnitudes of 7 to 8, eight with magnitudes of 6 to 7, more than 15 with magnitudes of 5 to 6, and about 140 recorded earthquakes with magnitudes smaller than 5 or of unassigned magnitudes. All of the earthquakes with magnitudes 8 or greater, and a large proportion of the others, appear to be related to the active Fairweather- Queen Charlotte Islands fault system or its western extension, the Chugach-St. Elias fault. Earthquake epicenters on the Denali fault system, the other major fault system in southeastern Alaska, are few in comparison. However, because high microearthquake activity has been recorded recently on this system and earthquakes of moderate size have occurred on some of its segments, the Denali fault system probably should not be dismissed as a relict fault system of no current tectonic importance. There are numerous other known faults, as well as lineaments that may be faults of varying degrees of tectonic activity in southeastern Alaska, adjacent Canada, and eastern Alaska. One of these elements is the Totschunda fault system, which connects with the Denali fault system in eastern Alaska; it has been very active during Holocene time but few historical earthquake epicenters appear to be related to it.
Both historical seismicity and geologic conditions, such as frequency and recency of faulting, must be considered together to permit an assessment of the future earthquake probability of an area. Data are too few for both factors for an accurate evaluation to be made of earthquake probability in southeastern Alaska. However, information compiled in the form of strain-release and seismic-zone maps permit some generalizations. Thus, it is tentatively concluded that most, if not all, of southeastern Alaska should be placed in seismic zone 3, a zone in which earthquakes of magnitude greater than 6 will occur from time to time and where there may be major damage to manmade structures.
Inferred effects from future earthquakes in southeastern Alaska include: (1) surface displacement along faults and other tectonic land-level changes, (2) ground shaking, (3) compaction, (4) liquefaction in cohesionless materials, (5) reaction of sensitive and quick clays, (6) water-sediment ejection and associated subsidence and ground fracturing, (7) earthquake-induced sub aerial slides and slumps, (8) earthquake induced subaqueous slides, (9) effects on glaciers and related features, (10) effects on ground water and stream flow, and (11) tsunamis, seiches, and other abnormal water waves. Because of the reconnaissance nature of our studies in the coastal communities and the sparsity of laboratory data on physical properties of geologic units in each area studied, the inferred effects must be largely empirical and generalized. Therefore, the inferences are based in large part upon the effects of past major earthquakes in Alaska and elsewhere, particularly upon the well-documented effects of the Alaska earthquake of March 27, 1964.
Buildings, highways, bridges, tunnels, harbor facilities, pipelines, canals, and other manmade structures may be severely damaged or destroyed by fault displacement or related tectonic land-level changes in southeastern Alaska. Direct damage from fault rupture would be restricted virtually to structures built directly athwart the fault. In California and Nevada, fault rupture almost always accompanies shocks of magnitude 6.5 or greater. The Alaska earthquake of March 27, 1964, and the Chilean earthquake of May 22, 1960, dramatically illustrated the severe adverse effects that can result from uplift or subsidence over a wide area.
The variable most responsible for the degree of shaking at any epicentral distance is the type of ground. Generally, shaking is considerably greater in poorly consolidated deposits than in hard bedrock, particularly if the deposits are water saturated. Severe shaking of alluvial deposits and manmade fill, with resultant heavy damage, is well documented from the records of many past earthquakes.
Damage commonly has been heavy as a result of ground settlement caused by compaction of loose sediments by shaking during an earthquake. This has been especially true where compaction was accompanied by tectonic downdrop of land, such as occurred during the Chilean earthquake of 1960 and the Alaska earthquake of 1964. Loosely emplaced manmade fill, deltaic deposits, beach deposits, and alluvial deposits may be susceptible to compaction in southeastern Alaska during a severe earthquake.
Liquefaction of sand and silt is a fairly common effect of large earthquakes. It was well illustrated at Niigata, Japan, during the earthquake of June 16, 1964, and resulted in extensive damage. When part of a sloping soil mass liquefies, the entire mass can undergo catastrophic failure and can flow as a high-density liquid. In southeastern Alaska, deltaic deposits probably would be most susceptible to liquefaction.
Sensitive and quick clays, which lose a considerable part of their strength when shaken, commonly fail during an earthquake and become rapid earthflows. Extensive studies were made of the sensitivity of the Bootlegger Cove Clay at Anchorage because of the marked loss of shear strength and dramatic failures of the deposits during the Alaska earthquake of 1964. If similar sensitive clays are present in some places in southeastern Alaska, they most likely are in some of the emergent fine-grained marine deposits; supporting data to confirm their presence, however, are largely lacking.
Records of some 50 major earthquakes show that in at least half of the instances water and sediment have been ejected from surficial deposits Water-sediment ejection and associated subsidence and ground fracturing commonly cause extensive damage to the works of man. Ejecta may fill basements and other low-lying parts of buildings. Agricultural land can be covered with a blanket of infertile soils, and small ponds can be filled or made shallow. In southeastern Alaska these phenomena are most likely to occur on valley floors, deltas, tidal flats, alluvial fans, swamps, and lakeshores.
Earthquake-induced sliding on land generally is confined to steep slopes but may take place in fine-grained deposits on moderately to nearly flat surfaces if the deposits are subject to liquefaction. A large rockslide triggered by the Lituya Bay, Alaska, earthquake of July 10, 1958, generated a wave that surged up the opposite wall of the inlet to a record height of 1,740 feet. During the Hebgen Lake, Montana, earthquake of August 17, 1959, a spectacular rockslide plunged into the Madison River canyon, buried 28 people, dammed the river, and created a large lake. Earthquake-records are replete with accounts of sliding of surficial deposits during moderate to large earthquakes. Most or all of the general factors that favor subaerial landsliding are present in southeastern Alaska.
Earthquake-induced subaqueous slides can produce adverse effects both nearshore and some distance offshore. Nearshore sliding may progress shoreward and destroy harbor facilities and other structures, commonly with substantial loss of life. Disastrous large submarine slides occurred along the fronts of deltas in Seward and Valdez during the Alaska earthquake of 1964. In similar fashion, the largest submarine slides in southeastern Alaska likely will be triggered along the larger delta fronts. Sliding farther offshore can constitute a threat to navigation because of changes in water depths. Also underwater sliding can break communication cables.
Glaciers were not greatly affected by the Alaska earthquake of 1964 despite the fact that about 20 percent of the area that underwent strong shaking is covered by ice. In contrast, the cataclysmic avalanche of ice and rock that fell from a high glacier-covered peak in Peru during the earthquake of May 31, 1970, produced devastating effects downvalley on man and his works in the form of mudflows. Most towns in southeastern Alaska are sufficiently distant from glaciers so as not be to directly affected.
Both the Alaska earthquake of 1964 and the Hebgen Lake, Montana, earthquake of 1959 significantly affected ground- and surface-water regimens. Water levels in some wells declined whereas in others flow increased. Some springs discharged at a rate three times as much as normal; flow of others decreased or stopped. Discharge of many streams increased markedly. Most or all of the effects described above could occur in parts of southeastern Alaska during future large earthquakes.
Tsunamis, seiches, and other abnormal water waves associated with large earthquakes commonly cause vast property damage and heavy loss of life. Tsunami effects can be devastating to coastal areas as far as many thousands of miles from their generation source. Seiche effects generally are confined to inland bodies of water or to relatively enclosed coastal bodies of water. Abnormal waves generated by submarine sliding or by subaerial sliding into water generally produce only local effects but may be highly devastating. Tsunami waves resulting from the Chilean earthquake of 1960 inflicted extensive damage and loss of life on coastal communities throughout a large part of southern Chile, and significant runups and damage were recorded in many places throughout the Pacific Ocean area. The tsunami waves generated by the Alaska earthquake of 1964 struck with devastating force along a broad stretch of the Alaska coast and produced heavy property damage and loss of life as far away as Crescent City, Calif. Seiche waves generated by that earthquake reached runup heights of 20-30 feet on some lakes in Alaska, and water-level fluctuations were recorded on streams, reservoirs, lakes, and swimming pools in States bordering the Gulf of Mexico. Waves generated by submarine sliding struck violently at a number of places during or immediately after the quake and were the major cause of loss of life and damage to property. Slide-generated waves probably would have a higher destructive potential in southeastern Alaska than either tsunami waves or seiche waves because of their possibly higher local runups and because they can hit the shores almost without warning during or immediately after an earthquake.
Nonearthquake-related geologic hazards, although generally far less dramatic than those related to earthquakes, tend to occur so much more frequently or persistently that their aggregate effects can be significant. Three kinds of geologic hazards of this type are discussed: (1) nonearthquake-induced landsliding and subaqueous sliding, (2) flooding, and (3) land uplift.
The potential for nonearthquake-triggered landsliding in southeastern Alaska ranges widely from place to place. Past sliding generally furnishes the clue in the prediction of where and in what materials future sliding will occur. Fast-moving rockslides, debris slides, and mudflows can be expected to occur from time to time on steep slopes and be highly destructive to highways, power plants, pipelines, buildings, and other facilities located on a slope or at its base. Present slow downslope movement of talus can be expected to continue at the same general rate unless conditions are changed by man or there are climatic changes. Snow and debris avalanches can be especially hazardous during winter months. Long-inactive landslides may be triggered into renewed activity or new slides may be created by man-induced modifications. Accelerated slope erosion and debris flows may follow large-scale clearing and cutting of timber. Subaqueous sliding can be expected to occur periodically along fronts of deltas and on other oversteepened underwater slopes.
Floods have been common in parts of southeastern Alaska because of heavy precipitation and rapid runoff from steep slopes with resulting heavy damage to roads and other facilities. Continued damage can be expected in the future unless more remedial measures are taken.
Current uplift of land in southeastern Alaska, although probably not affecting man significantly in a short period of time, may have some adverse long-term effects. These long-term effects should be borne in mind when facilities such as docks and boat harbors are constructed on or near the shore, where there is a critical relation between height of land and water.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr72230","usgsCitation":"Lemke, R.W., and Yehle, L.A., 1972, Regional and other general factors bearing on evaluation of earthquake and other geologic hazards to coastal communities of southeastern Alaska: U.S. Geological Survey Open-File Report 72-230, ii, 99 p., https://doi.org/10.3133/ofr72230.","productDescription":"ii, 99 p.","costCenters":[],"links":[{"id":425551,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0230/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":147832,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1972/0230/report-thumb.jpg"}],"country":"United 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Richard Walter","contributorId":105280,"corporation":false,"usgs":true,"family":"Lemke","given":"Richard","email":"","middleInitial":"Walter","affiliations":[],"preferred":false,"id":169813,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Yehle, Lynn A. yehle@usgs.gov","contributorId":3794,"corporation":false,"usgs":true,"family":"Yehle","given":"Lynn","email":"yehle@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":169812,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1946,"text":"wsp1873E - 1972 - Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina","interactions":[{"subject":{"id":55881,"text":"ofr68327 - 1968 - Interim report on sea-water encroachment into the Cape Fear River Estuary, North Carolina","indexId":"ofr68327","publicationYear":"1968","noYear":false,"title":"Interim report on sea-water encroachment into the Cape Fear River Estuary, North Carolina"},"predicate":"SUPERSEDED_BY","object":{"id":1946,"text":"wsp1873E - 1972 - Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina","indexId":"wsp1873E","publicationYear":"1972","noYear":false,"chapter":"E","title":"Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina"},"id":1}],"lastModifiedDate":"2019-12-30T10:14:20","indexId":"wsp1873E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1873","chapter":"E","title":"Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina","docAbstract":"This report presents the results of a fluorescent-dye-tracing study to determine the concentrations of a pollutant that would be present in the Northeast Cape Fear Estuary at various rates of continuous waste injection and freshwater inflow. Rhodamine WT dye was introduced into the estuary at a constant rate over a 24.8-hour period (two tidal cycles) at a point 6.4 miles upstream from the mouth in Wilmington, N.C., and concentrations were monitored at several selected sections in the tide-affected part of the river for 17 days. The range between high and low tide in this reach of the estuary averages at-rut 3.5 feet, and there is usually strong flow in both directions. \r\n\r\nResults of the dye study indicate that if a pollutant were injected at a rate of 100 pounds per day under the conditions of relatively low inflow existing' at the time, concentrations would ultimately build up to 20 micrograms of dye per liter of water 1,000 feet downstream. The flushing time during the study is estimated to be 17 days. These results are extrapolated to include periods of lower or higher inflow. For example, at average intervals of 10 years, it is estimated that inflow is so low that 100 days are required for a pollutant to travel the 6.4 miles from the point of waste release to the mouth of the river. Under these conditions it is expected that 1,000 feet downstream from the point of waste discharge, daily maximum concentrations will average about 130 micrograms per liter for each 100 pounds of pollutant injected per day. \r\n\r\nResults of a continuous discharge measurement of flow made by current meter during a complete tidal cycle are presented as a part of this report. Data from this measurement and other evidence indicate that net upstream flow in the estuary is possible over a period of several days.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1873E","usgsCitation":"Hubbard, E., and Stamper, W.G., 1972, Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina: U.S. Geological Survey Water Supply Paper 1873, v, 31 p. , https://doi.org/10.3133/wsp1873E.","productDescription":"v, 31 p. ","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":138417,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1873e/report-thumb.jpg"},{"id":27277,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1873e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"North Carolina","otherGeospatial":"Cape Fear Estuary","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -78.3599853515625,\n 33.77458136371689\n ],\n [\n -77.7227783203125,\n 33.77458136371689\n ],\n [\n -77.7227783203125,\n 34.5020297944346\n ],\n [\n -78.3599853515625,\n 34.5020297944346\n ],\n [\n -78.3599853515625,\n 33.77458136371689\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b47ea","contributors":{"authors":[{"text":"Hubbard, E. F.","contributorId":66666,"corporation":false,"usgs":true,"family":"Hubbard","given":"E. F.","affiliations":[],"preferred":false,"id":144416,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stamper, William G.","contributorId":58259,"corporation":false,"usgs":true,"family":"Stamper","given":"William","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":144415,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":56755,"text":"wdrMS711 - 1972 - Water resources data for Mississippi, water year 1971","interactions":[],"lastModifiedDate":"2025-08-28T14:25:18.228863","indexId":"wdrMS711","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":340,"text":"Water Data Report","code":"WDR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"MS-71-1","title":"Water resources data for Mississippi, water year 1971","docAbstract":"Water resources data for the 1971 water year for Mississippi including records of streamflow or reservoir storage at gaging stations, partial-record stations, and miscellaneous sites, and records of water-quality data on the chemical and physical characteristics of surface water, are given in this report. In Part 1, records are included for 71 gaging stations of which 67 are streamflow discharge stations, and 4 are reservoir or lake stations; also are included records for 27 low-flow partial-record stations, 143 crest-stage partial-record stations, and 91 miscellaneous sites. Locations of gaging stations are shown in Figure 1. In Part 2, data on the quality of surface water (chemical and temperature) were collected from designated sampling sites at pre-determined intervals such as monthly, or less frequently, and at one site data were recorded on punched paper tape at 60-minute intervals. Records are given for 55 sampling stations of which 5 are continuous record stations, 26 are partial-record stations, and 3 are miscellaneous sites. Locations of water-quality stations are shown in Figure 1. A few pertinent stations (not included above) in bordering States are also included in this report. The records were collected and computed by the Water Resources Division of the U.S. Geological Survey under the direction of L. E. Carroon, district chief. These data represent that portion of the National Water Data System collected by the U.S. Geological Survey and cooperating State and Federal agencies in Mississippi.
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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f9e4b07f02db5f3bb8","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":532871,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2352,"text":"wsp1608N - 1972 - Electric analog studies of flow to wells in the Punjab aquifer of West Pakistan","interactions":[],"lastModifiedDate":"2012-02-02T00:05:20","indexId":"wsp1608N","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1608","chapter":"N","title":"Electric analog studies of flow to wells in the Punjab aquifer of West Pakistan","docAbstract":"A series of experiments was performed with a steady-state electric analog simulating a cylindrical segment of the aquifer underlying the plains of the Punjab region of West Pakistan. In most of the experiments recharge was assumed to be from the surface, within a specified radius of influence, and distributed uniformly over the area within this radius. Experiments were made with different anisotropies (ratios of lateral to vertical resistance) so that various possible combinations of aquifer thickness and effective radius or radius of influence and combinations .of lateral and vertical permeability could be included in the models. Flow nets were constructed to show distribution of potential in the vertical section and intersections of stream surfaces with the vertical plane. \r\n\r\nThe series of experiments in which the screened interval is in the upper part of the aquifer shows that flow decreases and stream tubes shift progressively toward the upper part of the aquifer as anisotropy increases. \r\n\r\nAnother series illustrates that total yield increases and yield per foot of screen decreases as screen length increases. \r\n\r\nThe experiments indicate that, under conditions prevalent in the Punjab, the Distance-drawdown method for determining permeability gives results with an error of 10 percent or less provided that at least one piezometer or observation well is within a few feet of the pumped well and that no observation well or piezometer used is more than 100 feet from the pumped well. \r\n\r\nRelative traveltime for each of 10 stream tubes is given for three models. Relative traveltimes for one-fourth and one-half the effective radius are given for selected stream tubes. By substituting values for the aquifer parameters, actual traveltimes are computed from the relative-traveltime data.","language":"ENGLISH","publisher":"United States Govt. Print. Off.,","doi":"10.3133/wsp1608N","usgsCitation":"Mundorff, M.J., Bennett, G., and Ahmad, M., 1972, Electric analog studies of flow to wells in the Punjab aquifer of West Pakistan: U.S. Geological Survey Water Supply Paper 1608, iv, 28 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1608N.","productDescription":"iv, 28 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":137770,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1608n/report-thumb.jpg"},{"id":28277,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608n/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28278,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1608n/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a25e4b07f02db60eee0","contributors":{"authors":[{"text":"Mundorff, Maurice John","contributorId":41404,"corporation":false,"usgs":true,"family":"Mundorff","given":"Maurice","email":"","middleInitial":"John","affiliations":[],"preferred":false,"id":145063,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bennett, G.D.","contributorId":81073,"corporation":false,"usgs":true,"family":"Bennett","given":"G.D.","email":"","affiliations":[],"preferred":false,"id":145065,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ahmad, Masood","contributorId":57438,"corporation":false,"usgs":true,"family":"Ahmad","given":"Masood","email":"","affiliations":[],"preferred":false,"id":145064,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":14599,"text":"ofr72218 - 1972 - Clay deposits of the Connecticut River Valley, Connecticut: a special problem in land management","interactions":[],"lastModifiedDate":"2018-05-08T11:08:04","indexId":"ofr72218","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-218","title":"Clay deposits of the Connecticut River Valley, Connecticut: a special problem in land management","docAbstract":"When man first settled the United States, two natural features favored settlement; flat land that was easy to build on and to farm, and a nearby river that could act as a source of water, transportation, and power. The Connecticut River Valley from Middletown, Ct. north past the Connecticut-Massachusetts state line satisfied these two needs, and was favored by many early Americans in New England. This area remains an area of rapid urbanization, partly because of the broad flat lowlands.
The subdued topography of this area is due in large part to deposition of fine-grained materials into glacial Lake Hitchcock. This lake was formed during the Wisconsinan age when southward drainage in the Triassic valley of Connecticut was dammed by glacial drift in the area of Rocky Hill, Connecticut. Lake Hitchcock grew to and beyond St. Johnsbury, Vt. with much of the lake being filled with cyclical lake-bottom deposits during the 2,290 to 2,350 years of its life.
Aside from the relative flatness inherent in the deposition of fine-grained lake-bottom deposits, these deposits present very few characteristics that are favorable for urbanization. Favorable characteristics are possible sources of clay for manufacturing and possible sources for waste storage sites. Unfavorable characteristics include low water yields resulting in poor urban water-supply sources, and very low flows in streams during dry periods; low percolation rates resulting In drainage and septic problems; and low or uneven bearing strength which create problems in construction.
Fine-grained lake-bottom deposits have been mapped for six quadrangles in the Connecticut Valley lowlands; the quadrangles of Windsor Locks, Broad Brook, Hartford North, Manchester, Hartford South, and Glastonbury (all located in Connecticut). All the maps were prepared from existing information including well and test hole data on file at the Water Resources Division in Hartford, surficial geologic quadrangle maps, and bedrock contour maps. The maps also reflect geologic interpretations of the history of glacial Lake Hitchcock.
The Hartford North maps were prepared as test maps to determine if the project was feasible. They were prepared using the previously described information plus additional subsurface data obtained from engineering firms and the State Highway Department.
During preparation of the maps, an arcuate-shaped, ice-contact deposit composed of coarse sand and gravel was delineated in the Broad Brook and Windsor Locks quadrangles. This feature marks the location of a zone of stagnant ice In front of and marginal to active ice to the north.
Two types of maps were prepared for the area in study; Thickness of the Principal Clay Deposit, and Thickness of Material Overlying the Principal Clay Deposit. The term \"principal clay deposit\" refers to the fine-grained lake-bottom deposits of Glacial Lake Hitchcock. These maps define the distribution of the deposit, and show the thickness of the deposit in 50 foot intervals and the thickness of the material overlying the deposit In 20 foot intervals. The maps indicate that much of the area is underlain with substantial thicknesses of finegrained lake-bottom deposits (50 feet thick or greater), and that much of the deposit is within 20 feet of the surface.
The maps included in this report can be used for land-use planning. Uses include location of favorable sites for specific uses such as landfills, utility corridors, heavy construction, etc; location of problem areas for specific land uses; identification of possible problems for specific areas; design and construction cost estimates; and prospecting for exploitable clay deposits. It Is suggested that, for effective planning, these maps be used together or in conjunction with other maps such as maps showing surface materials, depth to bedrock, depth to water table, and flood prone areas.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr72218","usgsCitation":"Langer, W.H., 1972, Clay deposits of the Connecticut River Valley, Connecticut: a special problem in land management: U.S. Geological Survey Open-File Report 72-218, Report: vii, 39 leaves; 13 Plates: 22.43 x 30.27 inches or smaller, https://doi.org/10.3133/ofr72218.","productDescription":"Report: vii, 39 leaves; 13 Plates: 22.43 x 30.27 inches or smaller","costCenters":[],"links":[{"id":354002,"rank":15,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":354001,"rank":14,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353997,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353989,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0218/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353995,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353998,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-9.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353990,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353991,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353992,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353993,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353994,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353996,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":353999,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":354000,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0218/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":148239,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1972/0218/report-thumb.jpg"}],"scale":"24000","country":"United States","state":"Connecticut","otherGeospatial":"Connecticut River Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -72.75,\n 41.625\n ],\n [\n -72.5,\n 41.625\n ],\n [\n -72.5,\n 42\n ],\n [\n -72.75,\n 42\n ],\n [\n -72.75,\n 41.625\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abbe4b07f02db672b5f","contributors":{"authors":[{"text":"Langer, William H. blanger@usgs.gov","contributorId":1241,"corporation":false,"usgs":true,"family":"Langer","given":"William","email":"blanger@usgs.gov","middleInitial":"H.","affiliations":[{"id":387,"text":"Mineral Resources Program","active":true,"usgs":true}],"preferred":false,"id":169716,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1350,"text":"wsp1798K - 1972 - Fluvial sediment in Salem Fork watershed, West Virginia","interactions":[],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1798K","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"K","title":"Fluvial sediment in Salem Fork watershed, West Virginia","docAbstract":"Suspended sediment discharged from the 8.32-square-mile Salem Fork study area in Harrison County, W. Va., averaged 3,500 tons per year during the first 4-year period of investigation and 1,770 tons per year during the second 4-year period. The difference \r\nas attributed to increased flow control, effected by the completion of detention structures and other conservation measures, the absence of appreciable sediment-producing construction activities, and a reduction of the amounts of rainfall and runoff during the second 4-year period. Particle-size distribution of the suspended sediment discharged from the watershed remained unchanged during the two 4-year periods. Although sand and some silt were deposited in upstream reservoirs, sands and other sediments were evidently entrained in the flow below the reservoirs. \r\n\r\nDuring the 7.75-year period, reservoir 11A had a trap efficiency of 88 percent. The average annual sediment yield of subwatershed 11A was 1.31 tons per acre, or 837 tons per square mile. Outflow from reservoir 11A occurred during 81 percent of the investigation 'period, October 1954 to June 1962, and 78 percent of the sediment discharge from the reservoir occurred during less than 6 percent of the investigation period. A comparison of particle-size distribution of inflow sediment with that of outflow sediment revealed that practically all sands and some silts entering reservoir 11A were deposited in the reservoir. Chemical analyses of inflow water and the particle-size analyses suggested that flocculation of fine sediments occurred in the reservoir. Analysis of the sediment data collected at the outflow of reservoir 9 during 1956-62 revealed that the average annual sediment discharge was 128,000 pounds per year. Limited particle-size data suggested that practically no sand was discharged from reservoir 9, even though the inflow contained sand. Average annual inflow to reservoirs 11A and 9 compared favorably with average annual runoff for the entire watershed-study area.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1798K","usgsCitation":"Flint, R., 1972, Fluvial sediment in Salem Fork watershed, West Virginia: U.S. Geological Survey Water Supply Paper 1798, iv, K1-K29 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1798K.","productDescription":"iv, K1-K29 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":137541,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1798k/report-thumb.jpg"},{"id":26425,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1798k/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4883e4b07f02db517721","contributors":{"authors":[{"text":"Flint, R.F.","contributorId":39761,"corporation":false,"usgs":true,"family":"Flint","given":"R.F.","email":"","affiliations":[],"preferred":false,"id":143608,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":12786,"text":"ofr7251 - 1972 - Geological and geophysical investigations of an Apollo 9 photo anomaly near Point of Pines, Arizona","interactions":[],"lastModifiedDate":"2025-04-30T15:22:01.296707","indexId":"ofr7251","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-51","title":"Geological and geophysical investigations of an Apollo 9 photo anomaly near Point of Pines, Arizona","docAbstract":"An infrared photograph of southeastern Arizona, taken during the Apollo 9 multispectral terrain photography experiment in 1969, reveals a ringlike feature, some 3-4 miles (5-6 kin) in diameter, on the Natanes Plateau, 35 miles (56 kin) north of the town of Safford. Because the feature occurs in an area of nearly flat lying Tertiary volcanic rocks, the possibilities of its being a small collapse caldera or an exposed circular intrusive body were considered. Geological and geophysical studies of the area were made to test these hypotheses. \r\n\r\nThe local stratigraphic section consists of approximately 1,500 feet (457 m) of Oligocene and perhaps older volcanic rocks, resting on a moderately irregular basement surface carved from nearly flat lying trending Basin-and-Range faults define a broad horst within which two arcuate cross faults, with 300-600 feet (91-183 m) of displacement, bound a downdropped area. Deep erosion along these faults has created a polygonal network of canyons which constitutes the 'ring' seen on the photograph. A mild arching of the volcanic rocks within the ring is suggested by structure contours on the base of the youngest flows. \r\n\r\nA sharp 350-gamma positive aeromagnetic anomaly is centered within the ring. In its southwest quadrant the anomaly has an elongate extension that trends northwest along an adjoining Basin-and-Range fault. Associated with both is a subtle gravity low. The geophysical data thus suggest the presence of a small blind silicic pluton, possibly of middle Tertiary or younger age. Although it can be argued that the arcuate faults and mild arching of the volcanic pile are related to this postulated pluton, no evidence of hydrothermal alteration or thermal metamorphism of the country rocks was seen. Thus if a pluton is present and of postvolcanic age, it must have been emplaced as a relatively cool dry body; or alternatively, it is older than the surface volcanic rocks. In either instance, its magnetic expression contrasts with that of the known mineralized Laramide porphyry intrusive bodies of the region.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr7251","usgsCitation":"Bromfield, C., Eaton, G.P., Peterson, D.L., and Ratte, J., 1972, Geological and geophysical investigations of an Apollo 9 photo anomaly near Point of Pines, Arizona: U.S. Geological Survey Open-File Report 72-51, Report: ii, 19 p.; 11 Plates: 45.00 × 42.92 inches or smaller, https://doi.org/10.3133/ofr7251.","productDescription":"Report: ii, 19 p.; 11 Plates: 45.00 × 42.92 inches or smaller","costCenters":[],"links":[{"id":144797,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1972/0051/report-thumb.jpg"},{"id":41191,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41190,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41189,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41188,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41187,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41186,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41197,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0051/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":106541,"rank":14,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8739.htm","linkFileType":{"id":5,"text":"html"},"description":"8739"},{"id":41196,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41195,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41194,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41193,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41192,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0051/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Arizona","otherGeospatial":"Point of Pines","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -109.875,\n 33.25\n ],\n [\n -109.6250,\n 33.25\n ],\n [\n -109.6250,\n 33.375\n ],\n [\n -109.875,\n 33.375\n ],\n [\n -109.875,\n 33.25\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adee4b07f02db687646","contributors":{"authors":[{"text":"Bromfield, Calvin S.","contributorId":98690,"corporation":false,"usgs":true,"family":"Bromfield","given":"Calvin S.","affiliations":[],"preferred":false,"id":166707,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Eaton, G. P.","contributorId":86334,"corporation":false,"usgs":true,"family":"Eaton","given":"G.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":166706,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Peterson, D. L.","contributorId":36484,"corporation":false,"usgs":true,"family":"Peterson","given":"D.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":166705,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Ratte, J.C.","contributorId":10416,"corporation":false,"usgs":true,"family":"Ratte","given":"J.C.","affiliations":[],"preferred":false,"id":166704,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":48169,"text":"ofr73166 - 1972 - Shallow ground water in the Zamin Dawar area, Helmand Province, Afghanistan","interactions":[],"lastModifiedDate":"2012-02-02T00:10:07","indexId":"ofr73166","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"73-166","title":"Shallow ground water in the Zamin Dawar area, Helmand Province, Afghanistan","docAbstract":"The Zamin Dawar area lies between Kajakai Reservoir and Musa Qala Rud (river) in southcentral Afghanistan, about 90 km (kilometers) northeast of Lashkar Gab. The area comprises two main stream drainage areas: that of Gulmesh Mandeh (ephemeral stream) to the east which includes mostly plains with low hills on the east and north slopes and a high limestone scarp on the west slope; and Baghni Rud to the west which drains a mountainous area to the north and spreads onto a large alluvial fan with distributaries leading both to Helmand Rud to the southeast and Musa Qala Rud to the west. Most of the cultivated lands in the Zamin Dawar area lie in the southern part of the Gulmesh plains and in the Baghni alluvial fan, as well as a ribbon of cultivation on the flood plain of Baghni Rud in the mountains. The southern end of the Zamin Dawar area with high terraces and sharply incised ephemeral stream valleys is uninhabited. \r\n\r\nKarezes provide the chief source of water in the plains. Some 80 were examined and inventoried during the course of the present investigation. Several springs and one large-yield well also contribute to the water supply on the plains. In Baghni valley, developed springs provide the main source of water supply. \r\n\r\nDuring the present investigation, conducted in 1971,. it was found that the karezes yield a total of about 20,000 ac-ft (acre-feet) (25 million cu m (cubic meters)) of water The springs on the plains yield about 3,000 ac-ft (4 million cu m) per year, and the wells yield about 300 ac-ft (375,000 cu m) per year. The inventoried springs in Baghni valley yield about 6,500 ac-ft (8 million cu m) per year, and probably supply about 70 percent of the total water used in the valley. Therefore,the total amount of water used in the Zamin Dawar area in 1971 was about 32,000 ac-ft (40 million cu m). This amount of water was used to irrigate about i0,000 jiribs (approximately 5,000 acres or 2,000 hectares) of cultivated land and served a population of about 40,000 people. \r\n\r\nTwenty years ago the water supply was more than double the 1971 flow from karezes and springs, and the population of the area was probably 60,000 to 70,000 people. During the past 10 years and particularly during the last 3 years, the water table has been declining as a direct result of a dry-weather cycle which has affected much of Afghanistan. Concurrently, the population of the area has declined. Rainfall, based on data from the Kajakai Camp weather station, has declined from a 27-year annual average of about 200 mm (millimeters) to about 160 mm per year, which is the annual average for the last 5 years and equivalent to a reduction of approximately 70,000 ac-ft (88 million cu m) of precipitation per year over the entire area. To compensate for the declining water levels many karezes have been deepened or lengthened at great financial cost to the people.\r\n\r\nThis report evaluates present ground-water conditions in the area and suggests ways-and means by which more water can be obtained for local requirements.","language":"ENGLISH","doi":"10.3133/ofr73166","usgsCitation":"McClymonds, N.E., 1972, Shallow ground water in the Zamin Dawar area, Helmand Province, Afghanistan: U.S. Geological Survey Open-File Report 73-166, 112 p. ill., maps (2 fold. col. in pocket) ; 27 cm., https://doi.org/10.3133/ofr73166.","productDescription":"112 p. ill., maps (2 fold. col. in pocket) ; 27 cm.","costCenters":[],"links":[{"id":162307,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1973/0166/report-thumb.jpg"},{"id":84903,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0166/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84904,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0166/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84905,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1973/0166/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d6e4b07f02db5ddf05","contributors":{"authors":[{"text":"McClymonds, N. E.","contributorId":94653,"corporation":false,"usgs":true,"family":"McClymonds","given":"N.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":236907,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2027,"text":"wsp1586J - 1972 - Tracer simulation study of potential solute movement in Port Royal Sound, South Carolina","interactions":[],"lastModifiedDate":"2019-12-30T09:39:10","indexId":"wsp1586J","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1586","chapter":"J","title":"Tracer simulation study of potential solute movement in Port Royal Sound, South Carolina","docAbstract":"A tracer study was conducted in Port Royal Sound to simulate the movement and ultimate pattern of concentration of a solute continuously injected into the flow. A total of 750 pounds of Rhodamine WT dye was injected by boat during a period of 24.8 hours in a line across the Colleton River. During the following 43 days, samples of water were taken at selected points in the sound, and the concentration of dye in the samples was determined by fluorometric analysis. \r\n\r\nThe data obtained in the field study were used with theoretical models to compute the ultimate pattern of concentration of nonconservative and conservative solutes for a hypothetical continuous injection at the site on the Colleton River.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1586J","usgsCitation":"Kilpatrick, F.A., and Cummings, T.R., 1972, Tracer simulation study of potential solute movement in Port Royal Sound, South Carolina: U.S. Geological Survey Water Supply Paper 1586, iv, 27 p. , https://doi.org/10.3133/wsp1586J.","productDescription":"iv, 27 p. ","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":27500,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1586j/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137629,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1586j/report-thumb.jpg"}],"country":"United States","state":"South Carolina","otherGeospatial":"Port Royal Sound","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -80.9637451171875,\n 32.16166284018013\n ],\n [\n -80.321044921875,\n 32.16166284018013\n ],\n [\n -80.321044921875,\n 32.648625783736726\n ],\n [\n -80.9637451171875,\n 32.648625783736726\n ],\n [\n -80.9637451171875,\n 32.16166284018013\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4de4b07f02db6271d5","contributors":{"authors":[{"text":"Kilpatrick, F. A.","contributorId":22319,"corporation":false,"usgs":true,"family":"Kilpatrick","given":"F.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":144550,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cummings, T. Ray","contributorId":20722,"corporation":false,"usgs":true,"family":"Cummings","given":"T.","email":"","middleInitial":"Ray","affiliations":[],"preferred":false,"id":144549,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":48019,"text":"ofr7280 - 1972 - The ground-water system in southeastern Laramie County, Wyoming","interactions":[],"lastModifiedDate":"2017-09-20T16:34:25","indexId":"ofr7280","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-80","title":"The ground-water system in southeastern Laramie County, Wyoming","docAbstract":"Increased development of irrigation wells in southeastern Laramie County, Wyo., has caused concern about the quantity of water available. Ground water from approximately 230 large-capacity wells is used to irrigate most of the 18,165 acres under irrigation. \r\n\r\nThe purpose of this study is to provide more knowledge about the character of the aquifers, quantity of water in storage, rate of withdrawal, and the effect of withdrawals on streamflow. The area studied consists of about 400 square miles in southeastern Laramie County in the extreme southeast corner of Wyoming. \r\n\r\nThe White River Formation of Oligocene age and alluvium of Quaternary age are the principal aquifers. The White River Formation is made up primarily of clay, silt, and fine sand. Secondary permeability in the White River Formation accounts for it being an important aquifer. The alluvium, which Includes terrace and flood-plain deposits, consists of sand and gravel that contain some lenses of silt and clay.\r\n\r\nExistence of secondary permeability in the White River Formation has been accepted for some time although the nature of the secondary permeability has been disputed. Examination of downhole conditions with a television camera during this study revealed openings in the formation that appeared to be similar to tubes or caverns. The openings were of various sizes and shapes but only a few appeared to be associated with fracturing. Solution activity in the formation probably is an important factor in the development of secondary permeability. \r\n\r\nThe study area was divided into the Pine Bluffs-Egbert area and the Carpenter area. Ground-water movement in the Pine Bluffs-Egbert area is generally eastward into Nebraska; in the Carpenter area, movement is generally southward into Colorado. \r\n\r\nPumpage from large-capacity wells in the Pine Bluffs-Egbert area was estimated to be about 21,790 acre-feet in 1971. Water levels exhibited a declining trend annually in some areas during the period of record. Data indicate that pumpage in the Pine Bluffs-Egbert area probably is the cause of decreased base flow in Lodgepole Creek since approximately 1961. Increased pumpage, above that in 1971, will result in further reduction of discharge of Lodgepole Creek into Nebraska. \r\n\r\nIn the Carpenter area, it was estimated that the terrace deposit contained about 1 million acre-feet of saturated sediments in March 1971. The amount of ground water in storage in the White River Formation in this area is unknown.\r\n\r\nPumpage from large-capacity wells in the Carpenter area was estimated to be about 7,090 acre-feet in 1971. Recharge to the area was not estimated but there was no indication of a net decline in water levels between September 1970 and September 1971.","language":"ENGLISH","doi":"10.3133/ofr7280","usgsCitation":"Crist, M.A., and Borchert, W.B., 1972, The ground-water system in southeastern Laramie County, Wyoming: U.S. Geological Survey Open-File Report 72-80, 51 p. ill., maps ; 28 cm., https://doi.org/10.3133/ofr7280.","productDescription":"51 p. ill., maps ; 28 cm.","costCenters":[{"id":5050,"text":"WY-MT Water Science Center","active":true,"usgs":true}],"links":[{"id":84790,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0080/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84791,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0080/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84794,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0080/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":161748,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1972/0080/report-thumb.jpg"},{"id":84792,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0080/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84793,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0080/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84787,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0080/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84788,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0080/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84789,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0080/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a90e4b07f02db655e6e","contributors":{"authors":[{"text":"Crist, Marvin A.","contributorId":63376,"corporation":false,"usgs":true,"family":"Crist","given":"Marvin","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":236681,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Borchert, William B.","contributorId":16879,"corporation":false,"usgs":true,"family":"Borchert","given":"William","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":236680,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":56676,"text":"wdrWV711 - 1972 - Water resources data for West Virginia, water year 1971; Part 1. Surface water records; Part 2. Water quality records","interactions":[],"lastModifiedDate":"2023-03-10T21:03:59.256814","indexId":"wdrWV711","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":340,"text":"Water Data Report","code":"WDR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"WV-71-1","title":"Water resources data for West Virginia, water year 1971; Part 1. Surface water records; Part 2. Water quality records","docAbstract":"Water resources data for the 1971 water year for West Virginia including records of streamflow or reservoir storage at gaging stations, partial-record stations, and miscellaneous sites, and records of water-quality data on the chemical and physical characteristics of surface water, are given in this report. In Part 1, records are included for 111 gaging stations of which 105 are streamflow discharge stations, 1 is stage only streamflow station, and 5 are reservoir or lake stations; also included are records for 5 low-flow partial-record stations, 44 crest-stage partial-record stations, and 6 miscellaneous sites. Locations of gaging stations are shown in Figure 1. In Part 2, data on the quality of surface water (chemical, temperature, and sediment) were collected from designated sampling sites at predetermined intervals such as once daily, weekly, monthly, or less frequently, and at some sites data were recorder on punched paper tape at 15-, 30-, or 60-minute intervals. Records are given for 23 sampling stations of which 10 are continuous record stations, 11 are partial-record stations, and 2 are miscellaneous sites. Locations of water-quality stations are shown in Figure 1. A few pertinent stations (not included above) in bordering States are also included in this report. The records were collected and computed by the Water Resources Division of the U.S. Geological Survey under the direction of Edwin E. Harris, district chief. These data represent that portion of the National Water Data System collected by the U.S. Geological Survey and cooperating State and Federal agencies in West Virginia.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wdrWV711","collaboration":"Prepared in cooperation with the State of West Virginia and with other agencies","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1972, Water resources data for West Virginia, water year 1971; Part 1. Surface water records; Part 2. Water quality records: U.S. Geological Survey Water Data Report WV-71-1, viii, 179 p., https://doi.org/10.3133/wdrWV711.","productDescription":"viii, 179 p.","costCenters":[],"links":[{"id":184744,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wdr/1971/wv-71-1/report-thumb.jpg"},{"id":413969,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wdr/1971/wv-71-1/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"West 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Virginia\",\"nation\":\"USA \"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f6e4b07f02db5f1775","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":532792,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":48084,"text":"ofr72382 - 1972 - Hydrograph simulation models of the Hillsborough and Alafia Rivers, Florida: a preliminary report","interactions":[],"lastModifiedDate":"2014-05-29T07:19:12","indexId":"ofr72382","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-382","title":"Hydrograph simulation models of the Hillsborough and Alafia Rivers, Florida: a preliminary report","docAbstract":"Mathematical (digital) models that simulate flood hydrographs from rainfall records have been developed for the following gaging stations in the Hillsborough and Alafia River basins of west-central Florida: Hillsborough River near Tampa, Alafia River at Lithia, and north Prong Alafia River near Keysville. These models, which were developed from historical streamflow and and rainfall records, are based on rainfall-runoff and unit-hydrograph procedures involving an arbitrary separation of the flood hydrograph. These models assume the flood hydrograph to be composed of only two flow components, direct (storm) runoff, and base flow. Expressions describing these two flow components are derived from streamflow and rainfall records and are combined analytically to form algorithms (models), which are programmed for processing on a digital computing system.
\nMost Hillsborough and Alafia River flood discharges can be simulated with expected relative errors less than or equal to 30 percent and flood peaks can be simulated with average relative errors less than 15 percent.
\nBecause of the inadequate rainfall network that is used in obtaining input data for the North Prong Alafia River model, simulated peaks are frequently in error by more than 40 percent, particularly for storms having highly variable areal rainfall distribution.
\nSimulation errors are the result of rainfall sample errors and, to a lesser extent, model inadequacy. Data errors associated with the determination of mean basin precipitation are the result of the small number and poor areal distribution of rainfall stations available for use in the study. Model inadequacy, however, is attributed to the basic underlying theory, particularly the rainfall-runoff relation.
\nThese models broaden and enhance existing water-management capabilities within these basins by allowing the establishment and implementation of programs providing for continued development in these areas. Specifically, the models serve not only as a basis for forecasting floods, but also for simulating hydrologic information needed in flood-plain mapping and delineating and evaluating alternative flood control and abatement plans.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Tampa, FL","doi":"10.3133/ofr72382","collaboration":"Prepared by the United States Geological Survey in cooperation with Southwest Florida Water Management District","usgsCitation":"Turner, J.F., 1972, Hydrograph simulation models of the Hillsborough and Alafia Rivers, Florida: a preliminary report: U.S. Geological Survey Open-File Report 72-382, 107 p., https://doi.org/10.3133/ofr72382.","productDescription":"107 p.","numberOfPages":"107","costCenters":[],"links":[{"id":287744,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287743,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0382/report.pdf"}],"country":"United States","state":"Florida","otherGeospatial":"Alafia River;Hillsborough River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -82.5,27.75 ], [ -82.5,28.5 ], [ -82.0,28.5 ], [ -82.0,27.75 ], [ -82.5,27.75 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a2de4b07f02db61475b","contributors":{"authors":[{"text":"Turner, James F. Jr.","contributorId":16275,"corporation":false,"usgs":true,"family":"Turner","given":"James","suffix":"Jr.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":236785,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":48022,"text":"ofr7297 - 1972 - Ground-water outflow, San Timoteo-Smiley Heights area, upper Santa Ana Valley, southern California, 1927 through 1968","interactions":[],"lastModifiedDate":"2022-09-16T19:31:03.070135","indexId":"ofr7297","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-97","title":"Ground-water outflow, San Timoteo-Smiley Heights area, upper Santa Ana Valley, southern California, 1927 through 1968","docAbstract":"The San Timoteo-Smiley Heights area is in the upper Santa Ana Valley, San Bernardino and Riverside Counties, Calif., where the Yucaipa and San Timoteo-Beaumont ground-water basins border Bunker .Hill basin on the south between the San Jacinto and San Andreas faults. The area is broken by numerous faults, the topography is rough, and in a large part of the area few wells had been drilled prior to 196S. \r\n\r\nThe alluvial deposits, which constitute the aquifers in the area, range in thickness from 0 where they lap onto exposed bedrock hills to about 1,000 feet. Beneath the southern part of the area near the San Jacinto fault the total thickness of alluvial and lacustrine deposits may be as much as 6,000 feet. \r\n\r\nThe purpose of this study was to estimate ground-water outflow by an indirect method not involving balancing of the hydrologic budget. For this purpose it was necessary to estimate the permeability of the aquifer materials, the average annual hydraulic gradient, and the cross-sectional area through which the flow occurs; these values were estimated for five segments along a line of section between the San Jacinto fault and Crafton Hills. \r\n\r\nTo provide data for the outflow estimates, several miles of reflection and refraction seismic traverses were made along and across the outflow section. Nineteen deep and shallow test holes were drilled; one of the deep test holes and several existing wells were pumped to obtain data on aquifer permeability.\r\n\r\nThe estimated average permeabilities of the aquifer materials range from 5 gallons per day per square foot for the lower part of the San Timoteo beds of Frick (1921) and 40 gallons per day per square foot for the older alluvium to 220 gallons per day per square foot for the upper part of the San Timoteo beds. \r\n\r\nThe estimated outflow in 1927 was 8,150 acre-feet. By 1967 the estimated total outflow was 5,350 acre-feet, a reduction of approximately 34 percent. During the 12-year period 1956 through 1967, however, the annual outflow decline has been considerably less than the average for the 41-year period 1927 through 1967, and the decline as of 1968 was probably about 30-35 acre-feet per year.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr7297","usgsCitation":"Dutcher, L., and Fenzel, F., 1972, Ground-water outflow, San Timoteo-Smiley Heights area, upper Santa Ana Valley, southern California, 1927 through 1968: U.S. Geological Survey Open-File Report 72-97, Report: ii, 30 p.; 2 Plates: 35.22 × 22.43 inches and 33.72 × 22.76 inches, https://doi.org/10.3133/ofr7297.","productDescription":"Report: ii, 30 p.; 2 Plates: 35.22 × 22.43 inches and 33.72 × 22.76 inches","costCenters":[],"links":[{"id":110340,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_52161.htm","linkFileType":{"id":5,"text":"html"},"description":"52161"},{"id":84797,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0097/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84796,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0097/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":84795,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0097/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":161751,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1972/0097/report-thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"San Timoteo-Smiley Heights area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.2431,\n 33.9756\n ],\n [\n -117.0681,\n 33.9756\n ],\n [\n -117.0681,\n 34.0778\n ],\n [\n -117.2431,\n 34.0778\n ],\n [\n -117.2431,\n 33.9756\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa8e4b07f02db66741d","contributors":{"authors":[{"text":"Dutcher, L.C.","contributorId":42191,"corporation":false,"usgs":true,"family":"Dutcher","given":"L.C.","email":"","affiliations":[],"preferred":false,"id":236685,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fenzel, F. W.","contributorId":94742,"corporation":false,"usgs":true,"family":"Fenzel","given":"F. W.","affiliations":[],"preferred":false,"id":236686,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":22987,"text":"ofr72108 - 1972 - The hydraulic geometry of some Alaskan streams south of the Yukon River","interactions":[],"lastModifiedDate":"2024-02-14T22:23:45.085047","indexId":"ofr72108","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-108","title":"The hydraulic geometry of some Alaskan streams south of the Yukon River","docAbstract":"Channel geometry surveys were conducted to determine bankfull stage, discharge, and other hydraulic parameters at 22 locations along the proposed route of the trans-Alaska pipeline corridor south of the Yukon River. Combined with the records from gaging stations located at some of the sites, the data are sufficient to describe some of the channel and flow characteristics typical of each of two major hydrologic areas, the Yukon River Region and the South-Central Region. Although each region follows general hydrologic trends, least squares relations indicate each exhibits its own particular deviations.
Average values of the hydraulic and geometric properties of rivers were used to illustrate their application to practical engineering problems, namely the computation of depth of channel scour and of bedload discharge. For design purposes, caution is recommended when making computations based on average values. In the absence of other data, however, the average data become useful predictive tools.
In general, long freeze-free periods occur at low elevations, and short freeze-free periods occur at high elevations. But some valley floors have shorter freeze-free seasons than the glancing foothills because air cooled at high elevations flows downward and is trapped in the valleys. This temperature pattern occurs in the western part of the quadrangle in Rabbit Valley, Grass Valley, and the Sevier River Valley near Salina.
Because year-round weather stations are sparse in Utah, a special technique for estimating length of freeze-free season was developed by Dr. Gaylen L. Ashcroft, Assistant Professor of Climatology, Utah State University, and E. Arlo Richardson, State Climatologist, U.S. Weather Bureau, based on average annual temperature, average annual temperature range, average daily temperature range, and average july maximum temperature. This technique was used in preparation of the map showing “Length of 32°F freeze-free season for Utah,” figure 23 in Hydrologic Atlas of Utah (Utah State University and Utah Division of Water Resources, 1968), from which the data for this map were taken.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/i591E","usgsCitation":"1972, Map showing length of freeze-free season in the Salina quadrangle, Utah: U.S. Geological Survey IMAP 591, 1 Plate: 39.94 x 27.87 inches; Cover: 9.13 x 11.87 inches, https://doi.org/10.3133/i591E.","productDescription":"1 Plate: 39.94 x 27.87 inches; Cover: 9.13 x 11.87 inches","costCenters":[],"links":[{"id":254841,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/imap/0591e/plate-1.pdf","text":"Map 591-E","size":"8.48 MB","linkFileType":{"id":1,"text":"pdf"}},{"id":254842,"rank":2,"type":{"id":8,"text":"Cover"},"url":"https://pubs.usgs.gov/imap/0591e/report.pdf","text":"Folio Cover","size":"38 KB","linkFileType":{"id":1,"text":"pdf"}},{"id":254843,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/imap/0591e/report-thumb.jpg"},{"id":493508,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_9378.htm","linkFileType":{"id":5,"text":"html"}}],"scale":"250000","country":"United States","state":"Utah","otherGeospatial":"Salina quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112,38 ], [ -112,39 ], [ -110,39 ], [ -110,38 ], [ -112,38 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b15e4b07f02db6a4c3b","contributors":{"compilers":[{"text":"Covington, Harry R.","contributorId":101309,"corporation":false,"usgs":true,"family":"Covington","given":"Harry R.","affiliations":[],"preferred":false,"id":669782,"contributorType":{"id":3,"text":"Compilers"},"rank":1}]}} ,{"id":64986,"text":"i591G - 1972 - Map showing springs in the Salina quadrangle, Utah","interactions":[],"lastModifiedDate":"2025-08-04T21:15:19.964823","indexId":"i591G","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":320,"text":"IMAP","code":"I","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"591","chapter":"G","title":"Map showing springs in the Salina quadrangle, Utah","docAbstract":"A spring is “a place where, without the agency of man, water flows from a rock or soil upon the land or into a body of surface water” (Meinzer, 1923, p. 48).
About 450 springs are located on this map. Locations and names are from the U.S. Forest Service maps (1963, 1964) and from topographic maps of the U.S. Geological Survey, both published and in preparation. There is considerable variation in geological occurrence of the springs and in quantity and chemical quality of the water that issues from them. Springs in the Salina quadrangle are more abundant where annual precipitation is 16 inches or more, although there are many springs in arid parts of the quadrangle as well.
In the Salina quadrangle, springs are used most commonly for watering livestock. They are used also for irrigation and for domestic and municipal water supply. Several communities in Rabbit Valley, Grass Valley, and Sevier Valley depend on springs for all or part of their water supply.
Quantity and quality of water are shown for those few springs for which data are available (Mundorff, 1971). Caution must be used in drinking from springs, especially in arid areas; the water commonly tastes bad and may cause illness.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/i591G","usgsCitation":"1972, Map showing springs in the Salina quadrangle, Utah: U.S. Geological Survey IMAP 591, 1 Plate: 39.96 x 27.76 inches; Cover: 9.24 x 11.74 inches, https://doi.org/10.3133/i591G.","productDescription":"1 Plate: 39.96 x 27.76 inches; Cover: 9.24 x 11.74 inches","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":254853,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/imap/0591g/plate-1.pdf","text":"Map I-591-G","size":"7.96 MB","linkFileType":{"id":1,"text":"pdf"}},{"id":254854,"rank":2,"type":{"id":8,"text":"Cover"},"url":"https://pubs.usgs.gov/imap/0591g/report.pdf","text":"Folio Cover","size":"32 KB","linkFileType":{"id":1,"text":"pdf"}},{"id":493510,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_9380.htm","linkFileType":{"id":5,"text":"html"}},{"id":254855,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/imap/0591g/report-thumb.jpg"}],"scale":"250000","country":"United States","state":"Utah","otherGeospatial":"Salina quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112,38 ], [ -112,39 ], [ -110,39 ], [ -110,38 ], [ -112,38 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7ee4b07f02db648640","contributors":{"compilers":[{"text":"Covington, Harry R.","contributorId":101309,"corporation":false,"usgs":true,"family":"Covington","given":"Harry R.","affiliations":[],"preferred":false,"id":669242,"contributorType":{"id":3,"text":"Compilers"},"rank":1}]}} ,{"id":4711,"text":"twri04B1 - 1972 - Low-flow investigations","interactions":[],"lastModifiedDate":"2012-02-02T00:05:31","indexId":"twri04B1","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":336,"text":"Techniques of Water-Resources Investigations","code":"TWRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"04-B1","title":"Low-flow investigations","docAbstract":"This manual describes methods of defining the low-flow characteristics of streams, shows how certain basin characteristics influence the mean and variability of annual low flows, and recommends procedures for data collection, analysis, and reporting.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/twri04B1","issn":"0565-596X","usgsCitation":"Riggs, H.C., 1972, Low-flow investigations: U.S. Geological Survey Techniques of Water-Resources Investigations 04-B1, vi, 18 p. :ill., maps ;26 cm. Reprinted in 1982, 1989., https://doi.org/10.3133/twri04B1.","productDescription":"vi, 18 p. :ill., maps ;26 cm. Reprinted in 1982, 1989.","costCenters":[],"links":[{"id":139157,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":300,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/twri/twri4b1/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db648796","contributors":{"authors":[{"text":"Riggs, H. C.","contributorId":17210,"corporation":false,"usgs":true,"family":"Riggs","given":"H.","email":"","middleInitial":"C.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":149660,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":48102,"text":"ofr72463 - 1972 - Ground-water levels in observation wells in Oklahoma, 1969-70","interactions":[],"lastModifiedDate":"2014-05-29T07:40:16","indexId":"ofr72463","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-463","title":"Ground-water levels in observation wells in Oklahoma, 1969-70","docAbstract":"The investigation of the ground-water resources of Oklahoma by the U.S. Geological Survey in cooperation with the Oklahoma Water Resources Board includes a continuing program to collect records of water levels in selected observation wells on a systematic basis. These water-level records: (1) provide an index to available ground-water supplies; (2) facilitate the prediction of trends in water levels that will indicate likely changes in storage; (3) aid in the prediction of the base flow of streams; (4) provide information for use in basic research; (5) provide long-time continuous records of fluctuations of water levels in representative wells; and (6) serve as a framework to which other types of hydrologic data my be related.
\nPrior to 1956, measurements of water levels in observation wells in Oklahoma were included in water-supply papers published annually by the U.S. Geological Survey. Beginning with the 1956 calendar year, however, Geological Survey water-level reports will contain only records of a selected network of observation wells, and will be published at 5-year intervals. The first of this series, for the 1956-59 period was published in 1962.
\nIn addition to the water-supply papers, the U.S. Geological Survey, cooperation with the Oklahoma Water Resources Board, has published the following informal reports on water levels in Oklahoma.
\nGround-water levels in observations wells in Oklahoma, 1956-60
\nGround-water levels in observations wells in Oklahoma, 1961-62
\nGround-water levels in observations wells in Oklahoma, 1963-64
\nGround-water levels in observations wells in Oklahoma, 1965-66
\nGround-water levels in observations wells in Oklahoma, 1967-68
\nRecords of water-level measurements in wells in the Oklahoma Panhandle, 1966-70
\nRecords of water-level measurements in wells in the Oklahoma Panhandle, 1971-72
\nThe basic observation-well network in Oklahoma during the period 1969-70 included the following counties: Alfalfa, Beaver, Beckham, Caddo, Cimarron, Cleveland, Garfield, Garvin, Grady, Greer, Harmon, Jackson, Kingfisher, LeFlore, Major, Muskogee, Oklahoma, Payne, Pontotoc, Rogers, Sequoyah, Texas, Tillman, Wagoner, Washita, and Woodward. Table 2 includes the basic observation-well network and other wells measured by the U.S. Geological Survey.
\nThe data in this report were compiled and prepared for publication under the cooperative agreement for ground-water investigations in Oklahoma between the Oklahoma Water Resources Board, the U.S. Army Corps of Engineers, the Oklahoma Geological Survey, and the U.S. Geological Survey.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr72463","collaboration":"Prepared in cooperation with the Oklahoma Water Resources Board","usgsCitation":"Moore, R., 1972, Ground-water levels in observation wells in Oklahoma, 1969-70: U.S. Geological Survey Open-File Report 72-463, 86 p., https://doi.org/10.3133/ofr72463.","productDescription":"86 p.","numberOfPages":"91","costCenters":[],"links":[{"id":287756,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287755,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0463/report.pdf"}],"country":"United States","state":"Oklahoma","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.0,34.0 ], [ -103.0,37.0 ], [ -95.0,37.0 ], [ -95.0,34.0 ], [ -103.0,34.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66dd44","contributors":{"authors":[{"text":"Moore, R.L.","contributorId":95930,"corporation":false,"usgs":true,"family":"Moore","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":236815,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39023,"text":"pp387B - 1972 - Recent activity of glaciers of Mount Rainier, Washington","interactions":[],"lastModifiedDate":"2025-05-20T13:43:37.038244","indexId":"pp387B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"387","chapter":"B","title":"Recent activity of glaciers of Mount Rainier, Washington","docAbstract":"Knowing the ages of trees growing on recent moraines at Mount Rainier, Wash., permits the moraines to be dated. Moraines which are ridges of boulders, gravel, sand, and dust deposited at the margins of a glacier, mark former limits of a receding glacier. Knowing past glacial activity aids our understanding of past climatic variations.\r\n\r\nThe report documents the ages of moraines deposited by eight glaciers. Aerial photographs and planimetric maps show areas where detailed field studies were made below seven glaciers. Moraines, past ice positions, and sample areas are plotted on the photographs and maps, along with trails, roads, streams, and landforms, to permit critical areas to be identified in the future. Ground photographs are included so that sample sites and easily accessible moraines can be found along trails. Tables present data about trees sampled in areas near the glaciers of Mount Rainier, Wash.\r\n\r\nThe data in the tables show there are modern moraines of different age around the mountain; some valleys contain only one modern moraiine; others contain as many as nine. The evidence indicates a sequence of modern glacial advances terminating at about the following A.D. dates: 1525, 1550, 1625-60, 1715, 1730-65, 1820-60, 1875, and 1910. Nisqually River valley near Nisqually Glacier contains one moraine formed before A.D. 1842; Tahoma Creek valley near South Tahoma Glacier contains three moraines formed before A.D. 1528; 1843, and 1864; South Puyallup River valley near Tahoma Glacier, six moraines A.D. 1544, 1761, 1841, 1851, 1863, 1898; Puyallup Glacier, one moraine, A.D. 1846; Carbon Glacier, four moraines, 1519, 1763, 1847, 1876; Winthrop Glacier, four moraines, 1655, 1716, 1760, amid 1822; Emmons Glacier, nine moraines, 1596, 1613, 1661, 1738, 1825, 1850, 1865, 1870, 1901; and Ohanapecosh Glacier, three moraines, 1741, 1846, and 1878.\r\n\r\nAbandoned melt-water and flood channels were identified within moraine complexes below three glaciers, and their time of abandonment was dated. Outwash in three areas was deposited by melt-water of Tahoma Glacier before A.D. 1862, 1873, and 1910, respectively. Flood channels or melt-water channels on either side of Carbon River near Carbon Glacier dated from about 1901 to 1907. Melt-water channels of three different ages cut through Emmons Glacier moraines were dated as being abandoned before 1865, 1871, and 1917, respectively.\r\n\r\nAlthough the evidence at Mount Rainier indicates a sequence of glacial advance and retreat and of melt-water flow through different channels at different times, their climatic and hydrologic significance is not yet known.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp387B","usgsCitation":"Sigafoos, R.S., and Hendricks, E.L., 1972, Recent activity of glaciers of Mount Rainier, Washington: U.S. Geological Survey Professional Paper 387, Report: vi, 24 p.; 7 Plates: 35.00 x 33.00 inches or smaller, https://doi.org/10.3133/pp387B.","productDescription":"Report: vi, 24 p.; 7 Plates: 35.00 x 33.00 inches or smaller","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":66160,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0387b/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124857,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0387b/report-thumb.jpg"},{"id":66155,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0387b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66157,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0387b/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66158,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0387b/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66161,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0387b/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":486132,"rank":10,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4385.htm","linkFileType":{"id":5,"text":"html"}},{"id":66162,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0387b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66156,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0387b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66159,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0387b/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Washington","otherGeospatial":"Mount Rainier","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.9659158058002,\n 47.00544610953378\n ],\n [\n -121.9659158058002,\n 46.74731525709666\n ],\n [\n -121.55292944619455,\n 46.74731525709666\n ],\n [\n -121.55292944619455,\n 47.00544610953378\n ],\n [\n -121.9659158058002,\n 47.00544610953378\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a73e4b07f02db643aac","contributors":{"authors":[{"text":"Sigafoos, Robert S.","contributorId":82379,"corporation":false,"usgs":true,"family":"Sigafoos","given":"Robert","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":220820,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hendricks, E. L.","contributorId":50126,"corporation":false,"usgs":true,"family":"Hendricks","given":"E.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":220819,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70173978,"text":"70173978 - 1972 - Falling-stream turbidimeter as a means of measuring sediment concentrations in streams","interactions":[],"lastModifiedDate":"2016-06-22T08:10:31","indexId":"70173978","displayToPublicDate":"1973-01-01T00:00:00","publicationYear":"1972","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":"Falling-stream turbidimeter as a means of measuring sediment concentrations in streams","docAbstract":"An optical (photocell) sensing device was used to measure the relative transparency characteristics of sediment suspensions with a view toward improving our ability to measure the temporal variations of suspended-sediment concentration moving in streams. The instrument used was a commercial \"falling stream\" turbidimeter that measured the relative transparency of a gravity induced smooth flat sample stream formed as the flow drops vertically from an orifice.
\nOutput results were recorded on a strip-chart recorder as a function of concentration, up to about 100,000 mg/2, for a range of particle sizes and for three kinds of sediment--a fine sand, a silty alluvial soil, and a clayey residual soil. The sensitivity range was improved by use of both the 1/8- and 1/16-inch thick orifices. The use of the two orifice or nozzle sizes provided data useful in evaluation of the effect of particle size and type of sediment at different concentrations. The unique relative transparency-concentration relationships were more linear for coarse than for fine sediments of a given kind. It was concluded that curvature in this relationship resulted from light reflections from the surface of the particles and (or) the fact that some particles moved through the system while in the \"shadow\" of other particles closer to the light source.
\nThe ratio of suspended-sediment concentration to the square root of the median particle size of sand-sized sediments was found to be a useful parameter for elimination of the effect of particle size in the relative transparency-concentration relationships. Thus it was possible to evaluate the effect of the different type of sediment on the relative transparency independent of particle size. The use of this parameter to eliminate the effect of particle size was unsuccessful for finer sediments. -
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/70173978","usgsCitation":"Guy, H., and Olson, R., 1972, Falling-stream turbidimeter as a means of measuring sediment concentrations in streams: Open-File Report, 58 p., https://doi.org/10.3133/70173978.","productDescription":"58 p.","numberOfPages":"62","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":324035,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70173978.jpg"},{"id":324183,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70173978/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"576913bae4b07657d19ff052","contributors":{"authors":[{"text":"Guy, Harold P.","contributorId":6434,"corporation":false,"usgs":true,"family":"Guy","given":"Harold P.","affiliations":[],"preferred":false,"id":639911,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Olson, Richard C.","contributorId":172202,"corporation":false,"usgs":false,"family":"Olson","given":"Richard C.","affiliations":[],"preferred":false,"id":639912,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}