A tidal channel in a marsh bordering the Potomac River near Alexandria, Va., was mapped, and current-meter measurements of discharge were made at various locations and at various stages in the tidal cycle. These measurements allowed analysis of the change of width, depth, and velocity with discharge at various cross sections and along the length of the channel.
There is also presented a theoretical development of some, of these same relations based on hydraulic principles and on the assumption of a uniform distribution of energy and a minimum rate of work in the system as a whole.
The change of width, depth, and velocity with discharge downstream developed from the field data checked closely with the theoretically derived values.
The estuarine channel differs from a terrestrial one in that discharge at any section in an estuary varies depending on how the flow shaped the entire length of the channel between the point in question and the main body of tidal water. The result is that a tidal channel changes more rapidly in width and less rapidly in depth as discharge changes downstream than does a terrestrial channel.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp422B","usgsCitation":"Myrick, R.M., and Leopold, L.B., 1963, Hydraulic geometry of a small tidal estuary: U.S. Geological Survey Professional Paper 422, 19 p., https://doi.org/10.3133/pp422B.","productDescription":"19 p.","startPage":"B1","endPage":"B18","numberOfPages":"22","costCenters":[],"links":[{"id":140192,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0422b/report-thumb.jpg"},{"id":94745,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0422b/report.pdf","size":"2291","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Virginia","city":"Alexandria, VA","otherGeospatial":"Potomac River, Wrecked Recorded Creek","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.05480098724365,\n 38.7592035579107\n ],\n [\n -77.04287052154541,\n 38.7592035579107\n ],\n [\n -77.04287052154541,\n 38.77817551784403\n ],\n [\n -77.05480098724365,\n 38.77817551784403\n ],\n [\n -77.05480098724365,\n 38.7592035579107\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db62a200","contributors":{"authors":[{"text":"Myrick, Robert M.","contributorId":24345,"corporation":false,"usgs":true,"family":"Myrick","given":"Robert","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":152320,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Leopold, Luna Bergere","contributorId":93884,"corporation":false,"usgs":true,"family":"Leopold","given":"Luna","email":"","middleInitial":"Bergere","affiliations":[],"preferred":false,"id":152321,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":35360,"text":"b1133C - 1963 - Geology and hydrology of the Elk River, Minnesota, nuclear-reactor site","interactions":[],"lastModifiedDate":"2018-03-19T10:38:39","indexId":"b1133C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1133","chapter":"C","title":"Geology and hydrology of the Elk River, Minnesota, nuclear-reactor site","docAbstract":"The Elk River, Minn., nuclear-reactor site is on the east bluff of the Mississippi River about 35 miles northwest of Minneapolis and St. Paul. The area is underlain by about 70 to 180 feet of glacial drift, including at the top as much as 120 feet of outwash deposits (valley train) of the glacial Mississippi River. The underlying Cambrian bedrock consists of marine sedimentary formations including artesian sandstone aquifers. A hypothetically spilled liquid at the reactor site could follow one or both of two courses, thus: (1) It could flow over the land surface and through an artificial drainage system to the river in a matter of minutes; (2) part or nearly all of it could seep downward to the water table and then move laterally to the river. The time required might range from a few weeks to a year, or perhaps more. The St. Paul and Minneapolis water-supply intakes, 21 and 25 miles downstream, respectively, are the most critical points to be considered in the event of an accidental spill. Based on streamflow and velocity data for the Mississippi River near Anoka, the time required for the maximum concentration of a contaminant to travel from the reactor site to the St. Paul intake was computed to be about 8 hours, at the median annual maximum daily discharge. For this discharge, the maximum concentration at the intake would be about 0.0026 microcurie per cubic foot for the release of 1 curie of activity into the river near the reactor site.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/b1133C","collaboration":"Prepared in cooperation with the U.S. Atomic Energy Commission","usgsCitation":"Norvitch, R.F., Schneider, R., and Godfrey, R.G., 1963, Geology and hydrology of the Elk River, Minnesota, nuclear-reactor site: U.S. Geological Survey Bulletin 1133, Document: iv, 25 p.; 2 Plates: 18 x 16 inches, https://doi.org/10.3133/b1133C.","productDescription":"Document: iv, 25 p.; 2 Plates: 18 x 16 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":63222,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1133c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":63223,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1133c/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":63224,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1133c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109385,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20849.htm","linkFileType":{"id":5,"text":"html"},"description":"20849"},{"id":165594,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1133c/report-thumb.jpg"}],"country":"United States","state":"Minnesota","city":"Elk River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.61209869384766,\n 45.261596972270866\n ],\n [\n -93.61209869384766,\n 45.3297027614069\n ],\n [\n -93.51133346557617,\n 45.3297027614069\n ],\n [\n -93.51133346557617,\n 45.261596972270866\n ],\n [\n -93.61209869384766,\n 45.261596972270866\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b468c","contributors":{"authors":[{"text":"Norvitch, Ralph F.","contributorId":65456,"corporation":false,"usgs":true,"family":"Norvitch","given":"Ralph","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":214511,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schneider, Robert","contributorId":102460,"corporation":false,"usgs":true,"family":"Schneider","given":"Robert","email":"","affiliations":[],"preferred":false,"id":214513,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Godfrey, Richard G.","contributorId":100046,"corporation":false,"usgs":true,"family":"Godfrey","given":"Richard","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":214512,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":38960,"text":"pp417B - 1963 - Some relations between streamflow characteristics and the environment in the Delaware River region","interactions":[],"lastModifiedDate":"2022-09-16T21:44:23.016232","indexId":"pp417B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"417","chapter":"B","title":"Some relations between streamflow characteristics and the environment in the Delaware River region","docAbstract":"Streamflow characteristics are determined by a large number of factors of the meteorological and terrestrial environments. Because of lack of quantitative data to describe some of the factors and complex interrelations among them, complete analysis of the relations between streamflow and the various environmental factors is impossible. However, certain simplifying assumptions and generalizations made possible a partial analysis for the Delaware River region. For relations involving average runoff or low-flow parameters, average annual precipitation was assumed to be the principal meteorological factor, and geology (a complex of many factors) was assumed to be the principal terrestrial influence, except for that of basin size which was largely eliminated by expression of discharge in terms of unit area. As a first approximation, physiographic units were used as a basis for classifying the geology. Relations between flow parameters and precipitation are fairly well defined for some physiographic units, but not for those in which the geology varies markedly or the areal variation in average precipitation is very small. These relations provide a basis for adjusting the flow parameters to reduce or eliminate the effects of areal variations in precipitation and increase their significance in studies of the effects of terrestrial characteristics. An investigation of the residual effect of basin size (the effect remaining when discharge is expressed in terms of unit area) on relations between flow parameters and average precipitation indicates that such effect is negligible, except for very large differences in area. Parameters that are derived from base-flow recession curves and are related to a common discharge per unit area have inherent advantages as indicators of effects of terrestrial characteristics of basins, because the.y are independent of areal variations in average annual precipitation. Winter base-flow parameters are also practically independent of the effects of evapotranspiration from ground water. However, in many parts of the region these advantages are reduced or nullified by the difficulties of defining base-flow recession curves, particularly winter curves, with sufficient accuracy. In the absence of suitable base-flow recession data and a suitable basis for adjusting parameters, the ratio of the discharge equaled or exceeded 90 percent of the time to the average discharge (Qtt/Qa), or a similar duration parameter, probably is the best indicator of the influence of terrestrial characteristics, although the ratio may vary somewhat with average precipitation. In a part of the region where geologic differences are large and areal variations in average precipitation are small, values of Qm/Qa for each major geologic unit were determined from streamflow records. From these values and the percentage of area represented by each unit, a ratio for each gaging station was computed. Comparison of these computed results with the observed results indicates that nearly all of the variation in the ratio is associated with variation in geology. The investigation indicates that the original assumptions are correct; average precipitation is the principal meteorological influence and geology is the principal terrestrial influence. Together these two factors account for a very large proportion of the variation in average runoff and low-flow characteristics.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp417B","usgsCitation":"Hely, A., and Olmsted, F.H., 1963, Some relations between streamflow characteristics and the environment in the Delaware River region: U.S. Geological Survey Professional Paper 417, 25 p., https://doi.org/10.3133/pp417B.","productDescription":"25 p.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":406893,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4409.htm","linkFileType":{"id":5,"text":"html"}},{"id":122039,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0417b/report-thumb.jpg"},{"id":66021,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0417b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66023,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0417b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66022,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0417b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Delaware, New Jersey, Pennsylvania","otherGeospatial":"Delaware River region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.4083,\n 39.5833\n ],\n [\n -74.4417,\n 39.5833\n ],\n [\n -74.4417,\n 41\n ],\n [\n -76.4083,\n 41\n ],\n [\n -76.4083,\n 39.5833\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e8e4b07f02db5e8cd4","contributors":{"authors":[{"text":"Hely, A. G.","contributorId":14401,"corporation":false,"usgs":true,"family":"Hely","given":"A. G.","affiliations":[],"preferred":false,"id":220728,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Olmsted, F. H.","contributorId":24765,"corporation":false,"usgs":true,"family":"Olmsted","given":"F.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":220729,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":23192,"text":"ofr6336 - 1963 - Floods on White Rock Creek above White Rock Lake at Dallas, Texas","interactions":[{"subject":{"id":23192,"text":"ofr6336 - 1963 - Floods on White Rock Creek above White Rock Lake at Dallas, Texas","indexId":"ofr6336","publicationYear":"1963","noYear":false,"title":"Floods on White Rock Creek above White Rock Lake at Dallas, Texas"},"predicate":"SUPERSEDED_BY","object":{"id":68020,"text":"ha238 - 1967 - Floods on White Rock Creek at Dallas, Texas in 1962 and 1964","indexId":"ha238","publicationYear":"1967","noYear":false,"title":"Floods on White Rock Creek at Dallas, Texas in 1962 and 1964"},"id":1}],"supersededBy":{"id":68020,"text":"ha238 - 1967 - Floods on White Rock Creek at Dallas, Texas in 1962 and 1964","indexId":"ha238","publicationYear":"1967","noYear":false,"title":"Floods on White Rock Creek at Dallas, Texas in 1962 and 1964"},"lastModifiedDate":"2016-08-23T14:47:49","indexId":"ofr6336","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"63-36","title":"Floods on White Rock Creek above White Rock Lake at Dallas, Texas","docAbstract":"The White Rock Creek watershed within the city limits of Dallas , Texas, presents problems not unique in the rapid residential and industrial development encountered by many cities throughout the United States. The advantages of full development of the existing area within a city before expanding city boundaries, are related to both economics and civic pride. The expansion of city boundaries usually results in higher per capital costs for the operation of city governments.
Certainly no responsible city official would oppose reasonable development of watersheds and flood plains and thus sacrifice an increase in tax revenue. Within the words \"reasonable development\" lies the problem faced by these officials. They are aware that the natural function of a stream channel, and its associated flood plain is to carry away excess water in time of flood. They are also aware that failure to recognize this has often led to haphazard development on flood plains with a consequent increase in flood damages. In the absence of factual data defining the risk involved in occupying flood plains, stringent corrective and preventative measures must be taken to regulate man's activities on flood plains to a point beyond normal precaution.
Flood-flow characteristics in the reach of White Rock Creek that lies between the northern city boundary of Dallas and Northwest Highway (Loop 12) at the upper end of White Rock Lake, are presented in this report. Hydrologic data shown include history and magnitude of floods, flood profiles, outlines of areas inundated by three floods, and estimates of mean velocities of flow at selected points.
Approximate areas inundated by floods of April 1942 and July 1962 along White Rock Creek and by the flood of October 1962 along Cottonwood Creek, Floyd Branch, and Jackson Branch, are delineated on maps. Greater floods have undoubtedly occurred in the past but no attempt is made to show their probable overflow limits because basic data on such floods could not be obtained. Depths of inundation can be estimated from the information shown. Elevations shown are in feet above mean sea level, datum of 1929.
The data and computations supporting the results given herein are in the files of the Geological Survey in Austin, Texas.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Austin, TX","doi":"10.3133/ofr6336","issn":"0094-9140","collaboration":"Prepared in cooperation with the City of Dallas","usgsCitation":"Gilbert, C.R., 1963, Floods on White Rock Creek above White Rock Lake at Dallas, Texas: U.S. Geological Survey Open-File Report 63-36, ii, 15 p., https://doi.org/10.3133/ofr6336.","productDescription":"ii, 15 p.","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":113001,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1963/0036/plate-1.pdf","size":"4122","linkFileType":{"id":1,"text":"pdf"}},{"id":113002,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1963/0036/plate-2.pdf","size":"4104","linkFileType":{"id":1,"text":"pdf"}},{"id":155261,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1963/0036/report-thumb.jpg"},{"id":52512,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1963/0036/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Texas","city":"Dallaw","otherGeospatial":"White Rock Creek","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d8e4b07f02db5df7e4","contributors":{"authors":[{"text":"Gilbert, Clarence R.","contributorId":30965,"corporation":false,"usgs":true,"family":"Gilbert","given":"Clarence","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":189612,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":32743,"text":"pp379 - 1963 - Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups","interactions":[],"lastModifiedDate":"2022-03-29T21:42:36.762876","indexId":"pp379","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"379","title":"Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups","docAbstract":"The Elmira-Williamsport region, lying south of the Finger Lakes in central New York and northern Pennsylvania, is part of the Appalachian Plateaus physiographic province. A small segment of the Valley and Ridge province is included near the south border. In 1953 and 1954, the authors, a geologist and a soil scientist, made a reconnaissance of about 5,000 square miles extending southward from the Finger Lakes, N.Y., to Williamsport, Pa., and eastward from Wellsboro, Pa., to Towanda, Pa. Glacial drift of Wisconsin age, covering the central and most of the northern parts of the region, belongs to the Olean substage of MacClintock and Apfel. This drift is thin and patchy, is composed of the relatively soft sandstones, siltstone, shales, and conglomerates of the plateaus, commonly has a low calcium carbonate content, and is deeply leached. Mantling its surface are extensive rubbly colluvial deposits. No conspicuous terminal moraine marks the relatively straight border of Olean drift. The Valley Heads moraine of Fairchild near the south ends of the Finger Lakes is composed of relatively thick drift containing a considerable amount of somewhat resistant sedimentary and crystalline rocks. Commonly this drift has a relatively high carbonate content and is leached to only shallow depths. The Valley Heads drift is younger than Olean, but its precise age is undetermined. The age of the Olean is perhaps between Sangamon and Farmdale, on the basis of, in part, a carbon-14 date from peat at Otto, N.Y. All differences in soil development on these two Wisconsin drifts are clearly related to the lithology of the parent material or the drainage, rather than to weathering differing in kind or in duration. The authors believe that the soils are relatively young, are in equilibrium with the present environment, and contain few, if any, features acquired during past weathering intervals. The effect of tree throw on soil profiles and the presence of soils on slopes clearly indicate that soils form rapidly. Sols Bruns Acides are the most extensive great soil group occurring throughout the region. Podzols and Gray-Brown Podzolic soils are also widespread, and on long, smooth slopes Low Humic-Gley soils are common. Organic soils are of small extent. South of the Wisconsin drift border, the surficial mantle consists chiefly of alluvial, colluvial, or residual deposits of Wisconsin or of Recent age, but there are many small isolated patches of older, strongly weathered materials of pre-Wisconsin age. Although such older materials are commonly overlain or mixed with less weathered mantle, the yellowish-red color, characteristic of the strongly weathered material, is generally not masked. Some of the older material is drift, presumed to be of Illionian age, that was probably strongly weathered to a considerable depth in Sangamon time and has been greatly eroded since the last interglacial period. No clear-cut exposure of Wisconsin drift resting on older drift or other strongly weathered mantle has been found. The old drift and the other strongly weathered materials apparently acquired their present red color in pre-Wisconsin time. Where exposed at the surface, such strongly weathered mantle is the parent material of modern Red-Yellow Podzolic soils. Sols Bruns Acides and Gray-Brown Podzolic soils, developed on slightly weathered parent materials, are found adjacent to these red soils. This suggests that these Red-Yellow Podzolic soils probably developed from strongly weathered parent materials. No buried soils were found nor were any soils recognized as relics from pre-Wisconsin time. Comparison of a map of the great soil groups with a map of the vegetation of the region, prepared by John C. Goodlett, does not reveal a close relation. Laboratory analyses of samples collected furnish data on textural, mineralogical, and chemical changes caused by weathering and soil formation. The results indicate that the amount of chemical weathering which the Wisconsin drift has undergone is slight. The Red-Yellow Podzolic soils on strongly weathered pre-Wisconsin drift have B2 horizons that have a finer texture than the A2 or C horizons. The parent materials of these soils seem to be strongly weathered because of the high chromas, reddish hues, friable condition of most rock fragments, relatively high kaolinite content, and presence of gibbsite in the clay fraction. Measurements at numerous localities show that the depth of leaching increases with decreasing carbonate content and is not a criterion of the age of the drift. Pebble counts of gravels also show that the depth of leaching of gravel is related to its limestone content. The location of the gravel deposits is probably due primarily to the presence of pebbles of resistant rock rather than to ice wastage involving abundant glacial melt water. The region is in the Susquehanna drainage basin except for its north fringe, which drains to Lake Ontario. Most of the region is a dissected plateau ranging in altitude from 700 to 2,500 feet and underlain by gently folded sedimentary rocks of Paleozoic age. Much of the region slopes moderately or steeply; the most extensive areas of gently sloping land are 011 the uplands. In the northern part are several straight and deep valleys the southern extension of the Finger Lakes basins separated by uplands with several low cuestas that face north. Similarly, some streams such as the Canisteo, Cohocton, and Chemung Rivers, and the part of the Susquehanna River that is in New York, trend at right angles to the Finger Lakes, flowing in valleys that parallel the regional strike of the bedrock. The Olean drift border is marked by a change from drift containing very few rounded or striated rock fragments to a mantle containing only angular rock fragments and traces of red, strongly weathered materials. A reconstruction of the surface of the ice sheet, at its maximum extent shows an inferred slope of its distal margin ranging from 100 to 500 feet per mile
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp379","usgsCitation":"Denny, C.S., Lyford, W.H., and Goodlett, J.C., 1963, Surficial geology and soils of the Elmira-Williamsport region, New York and Pennsylvania, with a section on forest regions and great soil groups: U.S. Geological Survey Professional Paper 379, Report: iv, 59 p.; 6 Plates: 41.94 × 24.00 inches or smaller, https://doi.org/10.3133/pp379.","productDescription":"Report: iv, 59 p.; 6 Plates: 41.94 × 24.00 inches or smaller","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":60663,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60662,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60661,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60660,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60659,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60664,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0379/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60665,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0379/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397823,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4377.htm"},{"id":121752,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0379/report-thumb.jpg"}],"scale":"250000","country":"United States","state":"New York, Pennsylvania","otherGeospatial":"Elmira-Williamsport region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.5,\n 41.1667\n ],\n [\n -76.25,\n 41.1667\n ],\n [\n -76.25,\n 42.5\n ],\n [\n -77.5,\n 42.5\n ],\n [\n -77.5,\n 41.1667\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae2e4b07f02db688b83","contributors":{"authors":[{"text":"Denny, Charles Storrow","contributorId":86331,"corporation":false,"usgs":true,"family":"Denny","given":"Charles","email":"","middleInitial":"Storrow","affiliations":[],"preferred":false,"id":209081,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lyford, Walter Henry","contributorId":43824,"corporation":false,"usgs":true,"family":"Lyford","given":"Walter","email":"","middleInitial":"Henry","affiliations":[],"preferred":false,"id":209080,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Goodlett, J. C.","contributorId":98771,"corporation":false,"usgs":true,"family":"Goodlett","given":"J.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":209082,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1686,"text":"1686 - 1963 - Dispersion in natural streams","interactions":[],"lastModifiedDate":"2022-08-17T19:54:23.991124","indexId":"1686","displayToPublicDate":"1963-01-01T10:28:08","publicationYear":"1963","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":"Dispersion in natural streams","docAbstract":"Eleven tests were conducted to study the dispersion patterns of a radiotracer in five natural stream channels and in one canal. The radiotracer was injected as a line source. The patterns of dispersion that were observed in these channels were compared with patterns predicted by the theoretical models for one-dimensional flow developed by Taylor and other investigators. Analysis of the relation between time and concentration of the tracer at several sections in each of the six reaches shows that the available theoretical models are not adequate to describe the dispersion patterns actually observed. Dispersion coefficients determined from the test data are from 2 to 30 times greater than those predicted by the theoretical models. It is apparent that a better understanding of the dispersal phenomenon is needed in order to predict dispersion patterns in natural streams.
","language":"English","publisher":"U.S. Geological Survey,","publisherLocation":"Washington, D.C.","doi":"10.3133/1686","collaboration":"Prepared in cooperation with the United States Atomic Energy Commission","usgsCitation":"Godfrey, R.G., and Frederick, B.J., 1963, Dispersion in natural streams: Open-File Report, viii, 75 p., https://doi.org/10.3133/1686.","productDescription":"viii, 75 p.","numberOfPages":"83","costCenters":[],"links":[{"id":405280,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/1686/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":289868,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/1686/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53c4fc0ce4b0b58d96eeb581","contributors":{"authors":[{"text":"Godfrey, Richard G.","contributorId":100046,"corporation":false,"usgs":true,"family":"Godfrey","given":"Richard","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":143970,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Frederick, Bernard J.","contributorId":106808,"corporation":false,"usgs":true,"family":"Frederick","given":"Bernard","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":143971,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":3197,"text":"wsp1544B - 1962 - An application of thermometry to the study of ground water","interactions":[],"lastModifiedDate":"2018-04-02T10:17:13","indexId":"wsp1544B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"1544","chapter":"B","title":"An application of thermometry to the study of ground water","docAbstract":"Except for studies of temperature data related to ground-water developments that induce infiltration from streams, little attention has been given to the possibility of using temperature fluctuations as a tool for studying the elements of the hydrologic cycle involving ground water.
\nThe temperature of the water discharged from large installations that induce river infiltration through alluvial deposits depends primarily on the following factors: (a) the porosity of the aquifer, (b) the specific heat of the rocks or mineral grains making it up, (c) the temperature of the ground water in storage, (d) the temperature of the river water, and (e) the amount of mixing that occurs as a result of pumping. In six installations of this type, where the annual rivertemperature fluctuations ranged from 44° to 52°F, the average range in groundwater temperature was 22 °F. The cycles of ground-water temperature lagged behind the river-temperature cycles by 1 to 51/2 months. Under the conditions that existed, the lag of the minima of the cycles was much greater than that of the maxima, largely because of variations in pumpage and of the effect of viscosity differences on the rate of flow.
\nAn experimental study was made at Worthington in southwestern Minnesota to determine whether temperature fluctuations could be used to study rates and directions of ground-water movement or to evaluate recharge conditions. Three shallow glacial-outwash aquifers were studied by measuring temperatures at approximately monthly intervals in three municipal-supply wells whose average yields were about 60 to 150 gpm (gallons per minute). Temperatures were read with an accuracy of 0.01° to 0.02°C, and the data were analyzed graphically and correlated in detail with lake levels, lake temperatures, precipitation, and groundwater levels.
\nThermographs for 2 wells, 1 completed in a semiconfined aquifer about 200 feet from Okabena Lake and the other in a water-table aquifer about 850 feet from the lake, indicate that pumping induces water to move from the lake into the aquifers. A larger percentage of cold lake water was mixed with ground water from January to March 1958 than from January to March 1959. On the assumption that the cold or warm lake water was a distinct mass, the average time required for water to move from the lake to the well 200 feet away, under the prevailing hydraulic gradient, was 2 to 4 months; and to the well 850 feet away, 5 to 7 months.
\nThe thermograph for a well 1,800 feet from the lake, completed in an artesian aquifer that is confined by relatively impervious glacial till, indicates that the till acts as an insulating medium. However, despite the apparently low permeability of the till, the thermograph suggests that the lowering of artesian pressure, which results from pumping, induces warmer water to move downward through the till.
\nThe infiltration of relatively warm spring and summer rainfall can be detected on the thermographs of all the wells.
\nThe precise measurement of fluctuations in ground-water temperature, based on monthly readings in shallow glacial-outwash aquifers (up to about 70 feet deep), is useful in the study of ground-water movement and recharge. In addition to the study of natural phenomena in the hydrologic cycle, thermometry may be used as a tool in making detailed studies of (1) the effects of inducing the infiltration of surface water, (2) artificial recharge, (3) the effects of injecting petroleum products or radioactive or other wastes into the ground, and (4) ground-water movement in mines.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1544B","collaboration":"Prepared in cooperation with the Division of Waters, Minnesota Department of Conservation","usgsCitation":"Schneider, R., 1962, An application of thermometry to the study of ground water: U.S. Geological Survey Water Supply Paper 1544, Document: iii, 16 p.; 2 Plates: 16 x 12 inches and 16 x 17 inches, https://doi.org/10.3133/wsp1544B.","productDescription":"Document: iii, 16 p.; 2 Plates: 16 x 12 inches and 16 x 17 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":30184,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1544b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":30182,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1544b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":30183,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1544b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138321,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1544b/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db68571e","contributors":{"authors":[{"text":"Schneider, Robert","contributorId":102460,"corporation":false,"usgs":true,"family":"Schneider","given":"Robert","email":"","affiliations":[],"preferred":false,"id":146417,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1153,"text":"wsp1586B - 1962 - Salinity of the Delaware Estuary","interactions":[{"subject":{"id":22741,"text":"ofr5720 - 1957 - Salinity of water in the Delaware Estuary","indexId":"ofr5720","publicationYear":"1957","noYear":false,"title":"Salinity of water in the Delaware Estuary"},"predicate":"SUPERSEDED_BY","object":{"id":1153,"text":"wsp1586B - 1962 - Salinity of the Delaware Estuary","indexId":"wsp1586B","publicationYear":"1962","noYear":false,"chapter":"B","title":"Salinity of the Delaware Estuary"},"id":1},{"subject":{"id":51727,"text":"ofr54218 - 1954 - Salinity studies on estuaries of the Eastern Shore of Maryland","indexId":"ofr54218","publicationYear":"1954","noYear":false,"title":"Salinity studies on estuaries of the Eastern Shore of Maryland"},"predicate":"SUPERSEDED_BY","object":{"id":1153,"text":"wsp1586B - 1962 - Salinity of the Delaware Estuary","indexId":"wsp1586B","publicationYear":"1962","noYear":false,"chapter":"B","title":"Salinity of the Delaware Estuary"},"id":2},{"subject":{"id":51886,"text":"ofr566 - 1956 - Salinity investigations in the Delaware River estuary","indexId":"ofr566","publicationYear":"1956","noYear":false,"title":"Salinity investigations in the Delaware River estuary"},"predicate":"SUPERSEDED_BY","object":{"id":1153,"text":"wsp1586B - 1962 - Salinity of the Delaware Estuary","indexId":"wsp1586B","publicationYear":"1962","noYear":false,"chapter":"B","title":"Salinity of the Delaware Estuary"},"id":3}],"lastModifiedDate":"2017-07-07T09:19:36","indexId":"wsp1586B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"B","title":"Salinity of the Delaware Estuary","docAbstract":"The purpose of this investigation was to obtain data on and study the factors affecting the salinity of the Delaware River from Philadelphia, Pa., to the Appoquinimink River, Del. The general chemical quality of water in the estuary is described, including changes in salinity in the river cross section and profile, diurnal and seasonal changes, and the effects of rainfall, sea level, and winds on salinity. Relationships are established of the concentrations of chloride and dissolved solids to specific conductance. In addition to chloride profiles and isochlor plots, time series are plotted for salinity or some quantity representing salinity, fresh-water discharge, mean river level, and mean sea level. \r\n\r\n The two major variables which appear to have the greatest effect on the salinity of the estuary are the fresh-water flow of the river and sea level. The most favorable combination of these variables for salt-water encroachment occurs from August to early October and the least favorable combination occurs between December and May.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1586B","usgsCitation":"Cohen, B., and McCarthy, L.T., 1962, Salinity of the Delaware Estuary: U.S. Geological Survey Water Supply Paper 1586, iv, 47 p. :graphs ;24 cm., https://doi.org/10.3133/wsp1586B.","productDescription":"iv, 47 p. :graphs ;24 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":137310,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1586b/report-thumb.jpg"},{"id":25953,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1586b/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5fa30b","contributors":{"authors":[{"text":"Cohen, Bernard","contributorId":45289,"corporation":false,"usgs":true,"family":"Cohen","given":"Bernard","email":"","affiliations":[],"preferred":false,"id":143268,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McCarthy, Leo T. Jr.","contributorId":27029,"corporation":false,"usgs":true,"family":"McCarthy","given":"Leo","suffix":"Jr.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":143267,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1015,"text":"wsp1536G - 1962 - Constant-head pumping test of a multiaquifer well to determine characteristics of individual aquifers","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1536G","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"1536","chapter":"G","title":"Constant-head pumping test of a multiaquifer well to determine characteristics of individual aquifers","docAbstract":"This report describes the theory and field procedures for determining the transmissibility and storage coefficients and the original hydrostatic head of each aquifer penetrated by a multiaquifer well. The procedure involves pumping the well in such a manner that the drawdown of water level is constant while the discharges of the different aquifers are measured by means of borehole flowmeters. \r\n\r\nThe theory is developed by analogy to the heat-flow problem solved by Smith. The internal discharge between aquifers after the well is completed is analyzed as the first step. Pumping at constant, drawdown constitutes the second step. Transmissibility and storage coefficients are determined by a method described by Jacob and Lohman, after the original internal discharge to or from the aquifer has been compensated for in the calculations. The original hydrostatic head of each aquifer is then determined by resubstituting the transmissibility and storage coefficients into the first step of the analysis. \r\n\r\nThe method was tested on a well in Chester County, Pa., but the results were not entirely satisfactory, owing to the lack of sufficiently accurate methods of flow measurement and, probably, to the effects of entrance losses in the well. The determinations of the transmissibility coefficient and static head can be accepted as having order-of-magnitude significance, but the determinations of the storage coefficient, which is highly sensitive to experimental error, must be rejected. It is felt that better results may be achieved in the future, as more reliable devices for metering the flow become available and as more is learned concerning the nature of entrance losses. If accurate data can be obtained, recently developed techniques of digital or analog computation may permit determination of the response of each aquifer in the well to any form of pumping.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1536G","usgsCitation":"Bennett, G.D., and Patten, E., 1962, Constant-head pumping test of a multiaquifer well to determine characteristics of individual aquifers: U.S. Geological Survey Water Supply Paper 1536, iii, p. 181-203 :ill. ;23 cm., https://doi.org/10.3133/wsp1536G.","productDescription":"iii, p. 181-203 :ill. ;23 cm.","costCenters":[],"links":[{"id":137906,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1536g/report-thumb.jpg"},{"id":25627,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1536g/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db6972a1","contributors":{"authors":[{"text":"Bennett, Gordon D.","contributorId":18740,"corporation":false,"usgs":true,"family":"Bennett","given":"Gordon","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":143030,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Patten, E.P.","contributorId":21524,"corporation":false,"usgs":true,"family":"Patten","given":"E.P.","affiliations":[],"preferred":false,"id":143031,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1370,"text":"wsp1598 - 1962 - Geology and ground-water resources of the Ahtanum Valley, Yakima County, Washington","interactions":[{"subject":{"id":43527,"text":"ofr5744 - 1957 - Geologic sections of the Ahtanum Valley, Yakima County, Washington","indexId":"ofr5744","publicationYear":"1957","noYear":false,"title":"Geologic sections of the Ahtanum Valley, Yakima County, Washington"},"predicate":"SUPERSEDED_BY","object":{"id":1370,"text":"wsp1598 - 1962 - Geology and ground-water resources of the Ahtanum Valley, Yakima County, Washington","indexId":"wsp1598","publicationYear":"1962","noYear":false,"title":"Geology and ground-water resources of the Ahtanum Valley, Yakima County, Washington"},"id":1}],"lastModifiedDate":"2022-03-22T18:43:07.929619","indexId":"wsp1598","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"1598","title":"Geology and ground-water resources of the Ahtanum Valley, Yakima County, Washington","docAbstract":"The Ahtanum Valley covers an area of about 100 square miles in an important agricultural district in central Yakima County, Wash. Because the area is semiarid, virtually all crops require irrigation. Surface-water supplies are inadequate in most of the area, and ground water is being used increasingly for irrigation. The purpose of this investigation was the collection and interpretation of data, pertaining to ground water in the area as an aid in the proper development and management of the water resources. \r\n\r\nThe occurrence and movement of ground water in the Ahtanum Valley are directly related to the geology. The valley occupies part of a structural trough (Ahtanum-Moxee subbasin) that is underlain by strongly folded flow layers of a thick sequence of the Yakima basalt. The upper part of the basalt sequence interfingers with, and is conformably overlying by, sedimentary rocks of the Ellensburg formation which are as much as 1,000 feet thick. These rocks are in turn overlying unconformably by cemented basalt gravel as much as 400 feet thick. Unconsolidated alluvial sand and gravel, as much as 30 feet thick, form the valley floor. \r\n\r\nAlthough ground water occurs in each of the rock units within the area, the Yakima basalt and the unconsolidated alluvium yield about three-fourths of the ground water currently used. Wells in the area range in depth from a few feet to more than 1,200 feet and yield from less than 1 to more than 1,030 gallons per minute. \r\n\r\nAlthough water levels in water-table wells usually are shallow--often less than 5 feet below the land surface--levels in deeper wells tapping confined water range from somewhat above the land surface (in flowing wells) to about 200 feet below. Wells drilled into aquifers in the Yakima basalt, the Ellensburg formation, and the cemented gravel usually tap confined water, and at least 12 wells in the area flow or have flowed in the past. Ground-water levels fluctuate principally in response to changes in stream levels, variations in the flow of irrigation ditches and in rates of water application, variations in local precipitation, and seasonal differences in withdrawals from wells. Annual fluctuations of levels generally are less than 10 feet except in localities of heavy pumping. Periodic measurements of water levels in two observation wells in the area indicate, locally at least, a persistent decline in artesian pressures in confined basalt aquifers, although the record is too short to show whether withdrawal by pumping has \r\nreached, or is nearing, an optimum balance with recharge. \r\n\r\nThe aquifers are recharged by precipitation, by infiltration from streams, and by ground-water underflow into the area. Ground water is discharged by seepage to streams, by evapotranspiration, by springs and seeps at the land surface, and, artificially, by withdrawal from wells. It is estimated that the seepage discharge to the Yakima River from the area studied may range from about 20,000 to 25,000 acre-feet per year. The consumptive waste of ground water by phreatophytes probably exceeds 4,000 acre-feet per year and may represent a large reclaimable source of water in the area. The annual withdrawal of ground water from wells in the area for domestic, industrial, irrigation, public, and stock supplies is estimated to be 6,300 acre-feet. The chemical quality of the ground water generally is satisfactory for most purposes, although the water from many wells is harder than is desirable for domestic use.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1598","usgsCitation":"Foxworthy, B., 1962, Geology and ground-water resources of the Ahtanum Valley, Yakima County, Washington: U.S. Geological Survey Water Supply Paper 1598, Report: v, 100 p.; 3 Plates: 28.00 × 25.00 inches or smaller, https://doi.org/10.3133/wsp1598.","productDescription":"Report: v, 100 p.; 3 Plates: 28.00 × 25.00 inches or smaller","costCenters":[],"links":[{"id":397412,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24787.htm"},{"id":26461,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1598/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26460,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1598/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26459,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1598/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26458,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1598/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137263,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1598/report-thumb.jpg"}],"scale":"62500","country":"United States","state":"Washington","county":"Yakima County","otherGeospatial":"Ahtanum Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -120.924,\n 46.493\n ],\n [\n -120.457,\n 46.493\n ],\n [\n -120.457,\n 46.575\n ],\n [\n -120.924,\n 46.575\n ],\n [\n -120.924,\n 46.493\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db68571f","contributors":{"authors":[{"text":"Foxworthy, B. L.","contributorId":45686,"corporation":false,"usgs":true,"family":"Foxworthy","given":"B. L.","affiliations":[],"preferred":false,"id":143650,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":4149,"text":"cir457 - 1962 - Floods in Utah, magnitude and frequency","interactions":[],"lastModifiedDate":"2017-02-21T16:28:11","indexId":"cir457","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"457","title":"Floods in Utah, magnitude and frequency","docAbstract":"This report presents a procedure for estimating the magnitude and frequency of floods, within the range of the base data, for any site, gaged or ungaged. From the relation of annual floods to the mean annual flood, a composite frequency curve was derived for recurrence intervals of 1.1 to 50 years. For regions of similar hydrologic characteristics, curves were developed by multiple correlation to express the relation of mean annual flood to drainage area and mean altitude. The records of gaging stations having 5 or more years of record were used as base data when the natural conditions of streamflow are not affected by works of man. For major rivers where the flow is affected by diversion or regulation, separate analyses were made for each stream. The results may be applied to any area in Utah, except the Great Salt Lake Desert and a small area of the State in the Snake River basin.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/cir457","usgsCitation":"Berwick, V., 1962, Floods in Utah, magnitude and frequency: U.S. Geological Survey Circular 457, iii, 24 p., https://doi.org/10.3133/cir457.","productDescription":"iii, 24 p.","numberOfPages":"28","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":124558,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1962/0457/report-thumb.jpg"},{"id":31255,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1962/0457/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Utah","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dbe4b07f02db5e0a37","contributors":{"authors":[{"text":"Berwick, Vernon K.","contributorId":100373,"corporation":false,"usgs":true,"family":"Berwick","given":"Vernon K.","affiliations":[],"preferred":false,"id":148294,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2879,"text":"wsp1609 - 1962 - Ground-water resources of Camas Prairie, Camas and Elmore Counties, Idaho","interactions":[],"lastModifiedDate":"2012-02-02T00:05:35","indexId":"wsp1609","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"1609","title":"Ground-water resources of Camas Prairie, Camas and Elmore Counties, Idaho","docAbstract":"Camas Prairie is an eastward-trending intermontane basin along the north flank of the Snake River Plain in southern Idaho. The basin is about 40 miles long and averages about 8 miles wide. It was formed as a structural depression in which a considerable thickness of alluvial and lake deposits accumulated behind basalt flows, which at times blocked the outlet to the east. Intrusive and extrusive rocks of Cretaceous to Quarternary age enclose the basin on the north, west, and east. The enclosing rocks yield small amounts of water to springs and wells from the weathered mantle and fractures. \r\n\r\nThe principal aquifers are sand and gravel in the alluvial fill, and basalt. Water in the shallow deposits is not confined, and the water table generally is less than 10 feet below the surface at most places. Ground water in the deeper deposits occurs chiefly in two horizons that comprise the upper and lower artesian aquifers. Throughout much of the prairie, the pressure is sufficient that water will flow from wells in these aquifers. \r\n\r\nRecharge to the basin is from direct precipitation and percolation of stream runoff from the bordering mountains. Ground water moves from the higher areas at the base of the encircling mountains toward the center of the basin and the eastern outlet. The artesian aquifers leak by upward percolation through the imperfectly confining beds and help maintain the shallow water table. Basalt, which interfingers with the alluvial deposits, is an important aquifer near the southeast margin of the prairie and at the east end. Annual recharge to the artesian aquifers is estimated to be about 40,000 acre-feet. Discharge from the artesian aquifers is about equally divided between upward leakage to the shallow aquifers and underflow out of the prairie. Most of the underflow discharges into Camas Creek or Magic Reservoir east of the prairie; little of the underflow reaches the Snake River Plain. \r\n\r\nWells drilled for irrigation generally yield 500 to 1,200 gallons per minute from the artesian aquifers. Better construction and development methods would result in considerably better yields. Wells drilled in the basalt will yield 2,000 to 3,000 gallons per minute with moderate drawdowns. \r\n\r\nComputations made using aquifer coefficients, estimated on the basis of data collected during the investigation, suggest that 12,000 acre-feet of ground water might be withdrawn annually. However, the aquifers are limited in areal extent, and productivity of the alluvial aquifers is not great. Consequently heavy development would result in large drawdowns in wells, and there would be much interference between wells. The postulated large withdrawals from wells on the prairie would be supplied in part by a reduction in underflow from the prairie and in part by a decrease in leakage from the artesian aquifers, which in turn would cause a decline in the shallow water table.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1609","usgsCitation":"Walton, W.C., 1962, Ground-water resources of Camas Prairie, Camas and Elmore Counties, Idaho: U.S. Geological Survey Water Supply Paper 1609, iv, 57 p. :maps (1 fold. col. in pocket) diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1609.","productDescription":"iv, 57 p. :maps (1 fold. col. in pocket) diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":138988,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1609/report-thumb.jpg"},{"id":29515,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1609/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29516,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1609/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d925","contributors":{"authors":[{"text":"Walton, William Clarence","contributorId":89511,"corporation":false,"usgs":true,"family":"Walton","given":"William","email":"","middleInitial":"Clarence","affiliations":[],"preferred":false,"id":145948,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":67936,"text":"ha59 - 1962 - Floods at Mount Clemens, Michigan","interactions":[],"lastModifiedDate":"2017-02-06T16:09:17","indexId":"ha59","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"59","title":"Floods at Mount Clemens, Michigan","docAbstract":"The approximate areas inundated during the flood of April 5-6, 1947, by Clinton River, North Branch and Middle Branch of Clinton River, and Harrington Drain, in Clinton Township, Macomb County, Mich., are shown on a topographic map base to record the flood hazard in graphical form. The flood of April 1947 is the highest known since 1934 and probably since 1902. Greater floods are possible, but no attempt was made to define their probable overflow limits.
The Clinton River Cut-Off Canal, a flood-relief channel which diverts flow directly into Lake St. Clair from a point about 1500 feet downstream from Gratiot Avenue (about 9 miles upstream from the mouth) has been in operation since October 1951. The approximate limits of overflow that would results from a flood equivalent in discharge to that of April 1947, and occurring with the Cut-Off Canal in operation, are also shown. Although the Cut-Off Canal may reduce the frequency and depth of flooding it will not necessarily eliminate future flooding in the area. Improvements and additions to the drainage systems in the basin, expanding urbanization, new highways, and other cultural changes may influence the inundation pattern of future floods.
The preparation of this flood inundation map was financed through a cooperative agreement between Clinton Township, Macomb County, Mich., and the U.S. Geological Survey.
Backwater curves used to define the profile for a hypothetical flood on the Clinton River downstream from Moravian Drive, equivalent in discharge to the 1947 flood, but occurring with the present Cut-Off Canal in operation; flood stage established at the gaging station on Clinton River at Mount Clemens; and supplementary floodmark elevations were furnished by the Corps of Engineers.
Bench-mark elevations and field survey data, used in the analysis of floods on Harrington Drain, were furnished by the Macomb County Drain Commission.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ha59","collaboration":"Prepared in cooperation with Clinton Township, Macomb County, Michigan","usgsCitation":"Wiitala, S., and Ash, A.D., 1962, Floods at Mount Clemens, Michigan: U.S. Geological Survey Hydrologic Atlas 59, Plate: 35.5 x 31.0 inches, https://doi.org/10.3133/ha59.","productDescription":"Plate: 35.5 x 31.0 inches","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":188156,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":89137,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/059/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"8000","country":"United States","state":"Michigan","city":"Mount Clemens","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -82.973611,\n 42.626389\n ],\n [\n -82.858333,\n 42.626389\n ],\n [\n -82.858333,\n 42.622222\n ],\n [\n -82.861667,\n 42.622222\n ],\n [\n -82.865278,\n 42.541111\n ],\n [\n -82.973611,\n 42.541111\n ],\n [\n -82.973611,\n 42.626389\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e71ab","contributors":{"authors":[{"text":"Wiitala, S.W.","contributorId":41806,"corporation":false,"usgs":true,"family":"Wiitala","given":"S.W.","email":"","affiliations":[],"preferred":false,"id":277352,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ash, Arlington D.","contributorId":65546,"corporation":false,"usgs":true,"family":"Ash","given":"Arlington","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":277353,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":52246,"text":"ofr6258 - 1962 - Gravity survey of the Nevada Test Site and vicinity, Nye, Lincoln, and Clark Counties, Nevada--interim report","interactions":[],"lastModifiedDate":"2017-08-29T15:59:33","indexId":"ofr6258","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1962","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":"62-58","title":"Gravity survey of the Nevada Test Site and vicinity, Nye, Lincoln, and Clark Counties, Nevada--interim report","docAbstract":"The gravity survey of the Nevada Test Site and contiguous areas of southern Nevada and southeastern California (fig. 1) has been made by the U.S. Geological Survey on behalf of the U.S. Atomic Energy Commission.
The objective of this study is to delineate and interpret gravity anomalies and regional trends so that the configuration and depth of the buried erosional surface of the Paleozoic rocks may be determined. This buried surface is of utmost importance in understanding the geologic history of the Nevada Test Site region, the thickness and distribution of the overlying volcanic rocks and alluvium, and the movement of ground water. The Paleozoic rocks cause positive gravity anomalies where they outcrop or occur near the surface and negative anomalies where they are buried in valleys or capped by low-density Tertiary volcanic rocks.
Gravity trends which extend over the entire area provide a basis for computing the regional gravity gradient. The regional gravity gradient must be removed from the data for geologic interpretation of the paleotopographic surface in any limited area.
Knowledge of the thickness of low-density material overlying the paleotopographic surface is useful in several ways. Proposed underground test sites, such as drill holes and tunnels, may be evaluated in terms of rock unit thickness and alluvial cover requirements. Recent work by the Water Resources Division of the U.S. Geological Survey has demonstrated ground-water movement through the Paleozoic rocks in the vicinity of the Nevada Test Site. Therefore, knowledge of the position of buried Paleozoic rocks is important in evaluating (a) the rate and direction of flow of the ground water, (b) ground-water supplies for domestic and industrial uses, and (c) the possibility of radioactive contamination of ground water. Finally, regional gravity trends and paleotopography are useful in working out the structural history of the area in connection with geologic studies now in progress.
The purpose of this interim report is to present the major part of the gravity data obtained as of December 31, 1961. The data are presented as a complete Bouguer gravity anomaly map. Although the gravity contours are somewhat generalized because the map has a scale of 1:250,000 and a contour interval of 5 milligals, the largest anomalies are adequately delineated.
Preliminary results of this gravity survey have been reported by Wilmarth and others, 1960, and by Diment and others, 1959 and 1960.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6258","collaboration":"Prepared on behalf of the U.S. Atomic Energy Commission,","usgsCitation":"Healy, D.L., and Miller, C., 1962, Gravity survey of the Nevada Test Site and vicinity, Nye, Lincoln, and Clark Counties, Nevada--interim report: U.S. Geological Survey Open-File Report 62-58, Report: 34 p.; 3 Figures: 19.52 x 25.07 inches or smaller, https://doi.org/10.3133/ofr6258.","productDescription":"Report: 34 p.; 3 Figures: 19.52 x 25.07 inches or smaller","costCenters":[],"links":[{"id":86763,"rank":401,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1962/0058/plate-2.pdf","text":"Figure 3","size":"2.28 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Figure 3"},{"id":86764,"rank":402,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1962/0058/plate-3.pdf","text":"Figure 5","size":"1.60 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Figure 5"},{"id":86765,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0058/report.pdf","text":"Report","size":"514.56 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":175257,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0058/report-thumb.jpg"},{"id":86762,"rank":400,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1962/0058/plate-1.pdf","text":"Figure 2","size":"3.27 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Figure 2"}],"country":"United States","state":"Nevada","county":"Clark County, Lincoln County, Nye County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.191162109375,\n 36.20882309283712\n ],\n [\n -114.06005859375,\n 36.20882309283712\n ],\n [\n -114.06005859375,\n 38.71123253895224\n ],\n [\n -117.191162109375,\n 38.71123253895224\n ],\n [\n -117.191162109375,\n 36.20882309283712\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abae4b07f02db671fd1","contributors":{"authors":[{"text":"Healy, D. L.","contributorId":99204,"corporation":false,"usgs":true,"family":"Healy","given":"D.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":245035,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, C.H.","contributorId":19148,"corporation":false,"usgs":true,"family":"Miller","given":"C.H.","email":"","affiliations":[],"preferred":false,"id":245034,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":3411,"text":"cir439 - 1961 - Time of travel of water in the Ohio River, Pittsburgh to Cincinnati","interactions":[],"lastModifiedDate":"2017-06-09T08:32:55","indexId":"cir439","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"439","title":"Time of travel of water in the Ohio River, Pittsburgh to Cincinnati","docAbstract":"This report presents a procedure for estimating the time of travel of water in the Ohio River from Pittsburgh, Pa., to Cincinnati, Ohio, under various river stage conditions. This information is primarily for use by civil defense officials and by others concerned with problems involving travel time of river water. \r\n\r\nTables and charts are presented to show, for a particular stage or discharge at Cincinnati, the average time it would take for water to travel through the entire reach from Pittsburgh, or through successive intermediate segments of the reach. For example, when the discharge at Cincinnati is 200,000 cfs, travel time from Pittsburgh to Cincinnati, a distance of 470 miles, averages about 7 days; and for discharges of more than 200,000 cfs, the travel time decreases very slowly with increasing discharge. When the discharge is 30,000 cfs, travel time is about 28 days; and for discharges of less than 30,000 cfs, the travel time increases very rapidly with decreasing discharge. Estimates of travel time at low discharge are subject to large errors. Statistical analysis of the possible variations of upstream discharge for a given discharge at Cincinnati indicates that the shortest probable travel time from Pittsburgh to Cincinnati ranges from 56 percent of that under average conditions when the discharge at Cincinnati is 15,000 cfs to 93 percent of that under average conditions when the discharge at Cincinnati is 894,000 cfs. \r\n\r\nA chart showing the time distribution of flow at Cincinnati is presented so that the probable travel time of Ohio River water can be determined for any time of the year. This chart provides information which, when applied to the time-of-travel chart, shows that the most probable travel time of water from Pittsburgh to Cincinnati ranges from 160 hours in February to 1,250 hours in September. Also presented is a flow-duration curve that can be used to predict future discharges and, subsequently, times of travel, for use in long-range planning. The procedure used to compute time of travel is described in sufficient detail to make it usable as a guide for similar studies of other rivers that have deans and pools in the reach being studied. \r\n\r\nThe computations for the time-of-travel charts were made as follows: (a) by dividing the reach between Pittsburgh and Cincinnati into four subreaches with a full-range streamgaging station at or near the ends of each; (b) by computing for each subreach mean velocities corresponding to various discharges at Cincinnati, using data obtained from river survey maps and data available from gaging station operations; (c) by assuming that any mass of contaminated water would travel at a rate equal to that of the mean velocity of the river water.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir439","usgsCitation":"Steacy, R.E., 1961, Time of travel of water in the Ohio River, Pittsburgh to Cincinnati: U.S. Geological Survey Circular 439, iii, 14 p. :map, diagrs., tables. ;27cm., https://doi.org/10.3133/cir439.","productDescription":"iii, 14 p. :map, diagrs., tables. ;27cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":30428,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1961/0439/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124727,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1961/0439/report-thumb.jpg"}],"country":"United States","otherGeospatial":"Ohio River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -84.957275390625,\n 38.272688535980976\n ],\n [\n -79.8046875,\n 38.272688535980976\n ],\n [\n -79.8046875,\n 40.73893324113601\n ],\n [\n -84.957275390625,\n 40.73893324113601\n ],\n [\n -84.957275390625,\n 38.272688535980976\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48b6e4b07f02db533c35","contributors":{"authors":[{"text":"Steacy, Robert E.","contributorId":71162,"corporation":false,"usgs":true,"family":"Steacy","given":"Robert","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":146848,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":24284,"text":"ofr61123 - 1961 - Flow of springs and small streams in the Tecolote Tunnel area of Santa Barbara County, California","interactions":[],"lastModifiedDate":"2016-09-06T13:13:06","indexId":"ofr61123","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"61-123","title":"Flow of springs and small streams in the Tecolote Tunnel area of Santa Barbara County, California","docAbstract":"This report presents the results of an investigation to determine the effect of the construction of Tecolote Tunnel in southern Santa Barbara County, California, on the flow of springs and spring-fed streams in the tunnel area. A program of monthly measurement of discharge for this purpose began in late 1948 at 125 springs and streams; tunnel construction started in March 1950 and was completed in January 1956. By late 1951 appreciable seepage was entering the tunnel.
Incidental to the primary objective of this study, but a necessary part of the investigation, were a study of the discharge pattern of the springs and streams of the region, and an evaluation of the effect on flow of both the Arvin-Tehachapi earthquake of July 21, 1952 and the Refugio brush fire of early September 1955. The most striking characteristic of the regimen of flow in the area is the rapid response of discharge to precipitation. An interesting effect was observed in July 1952 when the Arvin-Tehachapi earthquake abruptly increased the flow at 18 measuring sites. At 15 of these sites this effect was felt for only several months, but at three of the sites the effect remained for several years. As for the Refugio fire, there is some reason to believe that the summer flow of many springs and streams may have increased in the years that followed as a result of decreased evapotranspiration losses, but the evidence is inconclusive.
The many complex and interrelated factors that influence the discharge of springs and spring-fed streams make it exceedingly difficult to isolate the effect of Tecolote Tunnel on the flow Another major difficulty in evaluating the effect of the tunnel stems from the fact that the calibration period for this study was only three years long, lasting from late 1948 to late 1951, and was uniformly deficient in precipitation, Furthermore, these inadequacies of the calibration period in regard to short length of record and limited range in precipitation, cannot be overcome by the collection of additional discharge information in the years to come. From the data available, however, the following conclusions were reached concerning the effect of Tecolote Tunnel:
Artesian aquifers underlie most of South Dakota and large areas in adjacent States. About 15,000 wells have been completed since 1881 in these aquifers within South Dakota. Many wells that originally flowed have ceased to flow and have been abandoned, and others have been equipped with pumps. Many thousands, however, continue to flow. This report presents data collected through June 1958 and includes records of 1,045 flowing and nonflowing artesian wells
\nSufficient information is not available at present (1958) to permit a detailed description of the geologic and hydrologic properties of artesian aquifers or their correlation in South Dakota. The description of the various aquifers given in this report is, therefore, necessarily a general one.
","language":"English","publisher":"U.S. Government Print Office","doi":"10.3133/wsp1534","usgsCitation":"Davis, R.W., Dyer, C., and Powell, J., 1961, Progress report on wells penetrating artesian aquifers in South Dakota: U.S. Geological Survey Water Supply Paper 1534, Report: iv, 100 p.; 3 Plates: 26.00 x 17.50 inches or smaller, https://doi.org/10.3133/wsp1534.","productDescription":"Report: iv, 100 p.; 3 Plates: 26.00 x 17.50 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":137430,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1534/report-thumb.jpg"},{"id":26208,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1534/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26209,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1534/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26210,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1534/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26211,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1534/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"South Dakota","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -104.029541015625,\n 45.935870621190546\n ],\n [\n -104.08447265624999,\n 43.004647127794435\n ],\n [\n -98.536376953125,\n 42.99661231842139\n ],\n [\n -98.031005859375,\n 42.74701217318067\n ],\n [\n -97.811279296875,\n 42.85180609584705\n ],\n [\n -97.23999023437499,\n 42.85180609584705\n ],\n [\n -96.976318359375,\n 42.73894375124379\n ],\n [\n -96.624755859375,\n 42.569264372193864\n ],\n [\n -96.40502929687499,\n 42.21224516288584\n ],\n [\n -96.317138671875,\n 42.25291778330197\n ],\n [\n -96.40502929687499,\n 42.39912215986002\n ],\n [\n -96.45996093749999,\n 42.553080288955826\n ],\n [\n -96.64672851562499,\n 42.73087427928485\n ],\n [\n -96.5478515625,\n 42.84375132629021\n ],\n [\n -96.492919921875,\n 43.03677585761058\n ],\n [\n -96.427001953125,\n 43.15710884095329\n ],\n [\n -96.51489257812499,\n 43.29320031385282\n ],\n [\n -96.51489257812499,\n 43.381097587278596\n ],\n [\n -96.602783203125,\n 43.50872101129684\n ],\n [\n -96.448974609375,\n 43.492782808225\n ],\n [\n -96.43798828125,\n 45.24395342262324\n ],\n [\n -96.51489257812499,\n 45.38301927899065\n ],\n [\n -96.64672851562499,\n 45.40616374516014\n ],\n [\n -96.778564453125,\n 45.51404592560424\n ],\n [\n -96.866455078125,\n 45.63708709571876\n ],\n [\n -96.624755859375,\n 45.767522962149904\n ],\n [\n -96.56982421875,\n 45.94351068030587\n ],\n [\n -104.029541015625,\n 45.935870621190546\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d9f3","contributors":{"authors":[{"text":"Davis, R. W.","contributorId":93459,"corporation":false,"usgs":true,"family":"Davis","given":"R.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":143456,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dyer, C.F.","contributorId":23917,"corporation":false,"usgs":true,"family":"Dyer","given":"C.F.","email":"","affiliations":[],"preferred":false,"id":143454,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Powell, J.E.","contributorId":27030,"corporation":false,"usgs":true,"family":"Powell","given":"J.E.","email":"","affiliations":[],"preferred":false,"id":143455,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2662,"text":"wsp1602 - 1961 - Effect of reforestation on streamflow in central New York","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"wsp1602","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"1602","title":"Effect of reforestation on streamflow in central New York","docAbstract":"Hydrologic data have been collected since 1932 in central New York State to determine the effect of reforestation on streamflow. Data are available for three small partly reforested areas and for one nonreforested control area. From 35 to 58 percent of the 3 areas were reforested, mostly with species of pine and spruce. The trees were allowed to grow without thinning or cutting, and by 1958 these reforested areas had developed into dense coniferous woodlots. \r\n\r\nIntensive statistical analyses of the data from the four study areas were made in 1958. Analyses were made for three hydrologic periods: the dormant season represented by the 6-month period ending April 30, the growing season represented by the 6-month period ending October 31, and the year represented by the 12-month period ending April 30. Analyses of the hydrologic data using multiple correlation with time as a variable and analyses of covariance between early and late periods of record indicated that several significant changes had occurred in the streamflow from the partly reforested study areas. Based on correlation with precipitation, total runoff for the dormant season from the 3 study areas was reduced by annual rates of 0.17 to 0.29 inches per year. Based on correlations with streamflow from a control area, total runoff from the partly reforested Shackham Brook area was reduced by average rates of 0.14 inches per growing season, 0.23 inches per dormant season, and 0.36 inches per hydrologic year. Peak discharges on Shackham Brook during the dormant season were reduced by 1958 by an average of 41 percent for the season, with reductions ranging from an average of 66 percent for November to an average of 16 percent for April. No significant changes were found in the peak discharges for the growing season, rates of base-flow recession, volumes of direct runoff, or annual low flows of streams in the three partly reforested areas. \r\n\r\nThe significant reductions in total runoff are attributed to increases in interception and transpiration in the reforested areas. The reductions in peak discharges during the dormant period are attributed largely to increased interception and sublimation of snowfall, and a gradual desynchronization of snowmelt runoff from the wooded and open areas of partly reforested watersheds. The changes in streamflow occurred gradually over the years; it could not be determined from the data whether changes in streamflow were still occurring in 1958, or whether they had reached a maximum.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1602","usgsCitation":"Schneider, W.J., and Ayer, G.R., 1961, Effect of reforestation on streamflow in central New York: U.S. Geological Survey Water Supply Paper 1602, v, 61 p. :maps, diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1602.","productDescription":"v, 61 p. :maps, diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":138228,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1602/report-thumb.jpg"},{"id":28999,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1602/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a05e4b07f02db5f8680","contributors":{"authors":[{"text":"Schneider, William Joseph","contributorId":104466,"corporation":false,"usgs":true,"family":"Schneider","given":"William","email":"","middleInitial":"Joseph","affiliations":[],"preferred":false,"id":145573,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ayer, Gordon Roundy","contributorId":52950,"corporation":false,"usgs":true,"family":"Ayer","given":"Gordon","email":"","middleInitial":"Roundy","affiliations":[],"preferred":false,"id":145572,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":39144,"text":"pp282F - 1961 - Drainage basins, channels, and flow characteristics of selected streams in central Pennsylvania","interactions":[],"lastModifiedDate":"2025-05-16T19:56:16.98169","indexId":"pp282F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"282","chapter":"F","title":"Drainage basins, channels, and flow characteristics of selected streams in central Pennsylvania","docAbstract":"The hydraulic, basin, and geologic characteristics of 16 selected streams in central Pennsylvania were measured for the purpose of studying the relations among these general characteristics and their process of development. The basic parameters which were measured include bankfull width and depth, channel slope, bed material size and shape, length of stream from drainage divide, and size of drainage area. The kinds of bedrock over which the streams flow were noted. In these streams the bankfull channel is filled by flows approximating the 2.3-year flood. By measuring the breadth and mean depth of the channel, it was possible to compute the bankfull mean velocity for each of the 119 sampling stations. These data were then used to compute the downstream changes in hydraulic geometry of the streams studied. This method has been called an indirect computation of the hydraulic geometry. The results obtained by the indirect method are similar to those of the direct method of other workers. The basins were studied by examining the relations of drainage area, discharge, and length of stream from drainage divide. For the streams investigated, excellent correlations were found to exist between drainage area and the 2.3-year flood, as well as between length of stream from the basin divide and drainage area. From these correlations it is possible to predict the discharge for the 2.3-year flood at any arbitrary point along the length of the stream. The long, intermediate, and short axes of pebbles sampled from the bed of the stream were recorded to study both size and sphericity changes along individual streams and among the streams studied. No systematic downstream changes in sphericity were found. Particle size changes are erratic and show no consistent relation to channel slope. Particle size decreases downstream in many streams but remains constant or increases in others. Addition of material by tributaries is one factor affecting particle size and another is the parent material. Wear does not appear to account for some of the changes noted in particle size in a downstream direction. Comparison with laboratory studies indicates that at least in some streams the downstream decrease in size is much greater than would be expected from wear alone. The type of bedrock underlying the channels included in this study appears to affect both channel slope and particle size. For a given length of stream, a stream channel underlain by sandstone tends to have a steeper slope and larger bed material than channels underlain by shale or limestone. Hence, a stream which heads in sandstone and ends in limestone tends to have a more rapid decrease in slope and particle size than a stream heading in limestone and ending in sandstone. The association of steep slopes and small particles for limestone channels implies that slope and particle size may show a vague correlation between lithologic groups although no correlation may exist within a given lithologic type. In addition to the effect of bedrock on slope and particle size, there is some evidence that channels in limestone or dolomite have a slightly smaller cross section at bankfull stage than channels in shale or sandstone. Near the headwaters of many of these streams, a deposit of periglacial rubble affects the slope and bed material size. Some of the debris contains residual boulders which are too large to be moved by ordinary floods and, therefore, impose larger particle sizes in the bed of the stream. The addition of this very coarse debris to the bed material is another example of the influence of geologic factors on stream channels even though the channel consists of unconsolidated debris instead of bedrock. The influence of geologic factors noted in selected streams in central Pennsylvania may not be directly applicable to areas other than the Appalachian Mountains, but the general process is no doubt similar in most areas. In large alluvial valleys bedrock cannot be much of an influencing factor; yet large, thick alluvial deposits and terraces are in a sense \"bedrock\" materials upon which the stream works to form the landscape.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp282F","usgsCitation":"Brush, L.M., 1961, Drainage basins, channels, and flow characteristics of selected streams in central Pennsylvania: U.S. Geological Survey Professional Paper 282, Report: 37 p.; 3 Plates: 10.00 x 24.00 inches or smaller, https://doi.org/10.3133/pp282F.","productDescription":"Report: 37 p.; 3 Plates: 10.00 x 24.00 inches or smaller","startPage":"145","endPage":"181","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":66643,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0282f/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66644,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0282f/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66645,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0282f/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":66646,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0282f/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":119375,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0282f/report-thumb.jpg"},{"id":486127,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4258.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Pennsylvania","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -78.5,\n 41.2139\n ],\n [\n -78.5,\n 40.5\n ],\n [\n -77.1372,\n 40.5\n ],\n [\n -77.1372,\n 41.2139\n ],\n [\n -78.5,\n 41.2139\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a61e4b07f02db635dfb","contributors":{"authors":[{"text":"Brush, Lucien M. Jr.","contributorId":107343,"corporation":false,"usgs":true,"family":"Brush","given":"Lucien","suffix":"Jr.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":221035,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":45982,"text":"ofr6047 - 1960 - Low-flow frequency data in Tennessee","interactions":[{"subject":{"id":45982,"text":"ofr6047 - 1960 - Low-flow frequency data in Tennessee","indexId":"ofr6047","publicationYear":"1960","noYear":false,"title":"Low-flow frequency data in Tennessee"},"predicate":"SUPERSEDED_BY","object":{"id":9181,"text":"ofr78807 - 1978 - Low-flow and flow duration of Tennessee streams","indexId":"ofr78807","publicationYear":"1978","noYear":false,"title":"Low-flow and flow duration of Tennessee streams"},"id":1}],"supersededBy":{"id":9181,"text":"ofr78807 - 1978 - Low-flow and flow duration of Tennessee streams","indexId":"ofr78807","publicationYear":"1978","noYear":false,"title":"Low-flow and flow duration of Tennessee streams"},"lastModifiedDate":"2012-02-02T00:10:10","indexId":"ofr6047","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"60-47","title":"Low-flow frequency data in Tennessee","language":"ENGLISH","doi":"10.3133/ofr6047","usgsCitation":"Eaton, W.R., 1960, Low-flow frequency data in Tennessee: U.S. Geological Survey Open-File Report 60-47, 1 map., https://doi.org/10.3133/ofr6047.","productDescription":"1 map.","costCenters":[],"links":[{"id":162324,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db648754","contributors":{"authors":[{"text":"Eaton, W. Robert","contributorId":92716,"corporation":false,"usgs":true,"family":"Eaton","given":"W.","email":"","middleInitial":"Robert","affiliations":[],"preferred":false,"id":232399,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":52107,"text":"ofr6077 - 1960 - Progress report number 2: investigations of some sedimentation characteristics of sand-bed streams","interactions":[],"lastModifiedDate":"2012-06-27T01:01:44","indexId":"ofr6077","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"60-77","title":"Progress report number 2: investigations of some sedimentation characteristics of sand-bed streams","docAbstract":"Hydraulic and sediment characteristics at six river sections upstream and downstream from the confluence of the Middle Loup and Dismal Rivers were measured and studied to determine some of the interrelationships between variables and the differences that exist between common variables when two flows unite. The two streams, which flow through the Sandhills region of Nebraska, have about the same water discharge, sediment concentration, and particle-size distribution of suspended sediment and bed material. Sediment discharges and flow resistances varied widely, although water discharges remained almost constant. The factor affecting the variations was water temperature, which ranged from 32° to 80° F. The bed form, which also varied with the water temperature, seemed to have a dominating influence on the sediment discharge, flow resistance, and possibly the vertical distribution of velocity and suspended sediment. Multiple regression with parameters derived from dimensional analysis yielded an expression for predicting the flow resistance and the widths and depths of individual channel sections. Contrary to those near many other confluences, slopes were steeper and channels were wider downstream from the junction of the two rivers than they were upstream. An investigation of specific sediment-transport phenomena and field procedures was made during 1956 and 1957 in cooperation with the U.S. Bureau of Reclamation. The purposes of this investigation were to provide information on the regime of rivers and to improve the procedures related to the collection of sediment data. The basic data and results of the studies made in 1956 were presented in progress report number 1, \"Investigations of Some Sedimentation Characteristics of a Sand-Bed Stream.\" Some of the basic data and results of the studies made in 1957 are given in this report.","language":"ENGLISH","doi":"10.3133/ofr6077","collaboration":"Prepared as part of a program of the Department of the Interior for development of the Missouri River basin","usgsCitation":"Hubbell, D.W., 1960, Progress report number 2: investigations of some sedimentation characteristics of sand-bed streams: U.S. Geological Survey Open-File Report 60-77, 53 p.; Tables: pgs. 54-78, https://doi.org/10.3133/ofr6077.","productDescription":"53 p.; Tables: pgs. 54-78","startPage":"1","endPage":"78","numberOfPages":"78","costCenters":[],"links":[{"id":178264,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_60_77.jpg"},{"id":257892,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1960/hubbell/Hubbell_et_al_1960.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6495d3","contributors":{"authors":[{"text":"Hubbell, D. W.","contributorId":15997,"corporation":false,"usgs":true,"family":"Hubbell","given":"D.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":244810,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":52133,"text":"ofr60129 - 1960 - Lowest mean discharge and flow duration data by years at selected gaging stations in the Mississippi Embayment area","interactions":[{"subject":{"id":52133,"text":"ofr60129 - 1960 - Lowest mean discharge and flow duration data by years at selected gaging stations in the Mississippi Embayment area","indexId":"ofr60129","publicationYear":"1960","noYear":false,"title":"Lowest mean discharge and flow duration data by years at selected gaging stations in the Mississippi Embayment area"},"predicate":"SUPERSEDED_BY","object":{"id":32717,"text":"pp448G - 1966 - Low-flow characteristics of streams in the Mississippi embayment in southern Arkansas, northern Louisiana and northeastern Texas with a section on quality of the water","indexId":"pp448G","publicationYear":"1966","noYear":false,"chapter":"G","title":"Low-flow characteristics of streams in the Mississippi embayment in southern Arkansas, northern Louisiana and northeastern Texas with a section on quality of the water"},"id":1}],"supersededBy":{"id":32717,"text":"pp448G - 1966 - Low-flow characteristics of streams in the Mississippi embayment in southern Arkansas, northern Louisiana and northeastern Texas with a section on quality of the water","indexId":"pp448G","publicationYear":"1966","noYear":false,"title":"Low-flow characteristics of streams in the Mississippi embayment in southern Arkansas, northern Louisiana and northeastern Texas with a section on quality of the water"},"lastModifiedDate":"2012-02-02T00:11:28","indexId":"ofr60129","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"60-129","title":"Lowest mean discharge and flow duration data by years at selected gaging stations in the Mississippi Embayment area","language":"ENGLISH","doi":"10.3133/ofr60129","usgsCitation":"Speer, P.R., 1960, Lowest mean discharge and flow duration data by years at selected gaging stations in the Mississippi Embayment area: U.S. Geological Survey Open-File Report 60-129, 666 p., https://doi.org/10.3133/ofr60129.","productDescription":"666 p.","costCenters":[],"links":[{"id":178977,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db6489cc","contributors":{"authors":[{"text":"Speer, P. R.","contributorId":104948,"corporation":false,"usgs":true,"family":"Speer","given":"P.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":244853,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":52138,"text":"ofr60135 - 1960 - Floods of May 1959 in the Au Gres and Rifle River basins, Michigan","interactions":[],"lastModifiedDate":"2017-07-12T10:36:22","indexId":"ofr60135","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"60-135","title":"Floods of May 1959 in the Au Gres and Rifle River basins, Michigan","docAbstract":"The floods of May 1959 in the Au Gres and Rifle River basins, Michigan, resulted from heavy rainfall during the night of May 19-20. Peak unit discharges for small drainage areas (less than about 15 square miles) were the highest ever measured in the Lower Peninsula of Michigan, and for very small areas (about one square mile) were of the same order of magnitude as those for the record Ontonagon River flood of August 1942 in the Upper Peninsula.
Because the flood area is sparsely populated, damages were largely confined to farm lands and facilities and to secondary roads and their appurtenant drainage structures.
The U. S. Geological Survey, through the district office in Lansing, Michigan, operates a network of streamgaging stations and crest-stage stations in the area affected by this flood. Six recording rain gages are operated in the upper Rifle River basin. Most of the gaging stations have been in operation for 7 to 9 years giving systematic records of stage, discharge, and volume of flow covering the range from drought to flood. This report contains records of
-stage and discharge at 9 gaging stations for the flood
period, peak discharges at 7 crest-stage stations
and 2 miscellaneous sites within the flood area, and
other data pertinent to the flood.
Forty-two east-west aeromagnetic lines were flown across the Cook Inlet-Susitna Lowland between Chelatna Lake and Seldovia at a flight altitude of approximately 2,500 feet. The lines traverse all or part of five Mesozoic tectonic elements that dominate the structure of the Cook Inlet area. Each of these tectonic elements, the Alaska Range geosyncline, the Talkeetna geanticline, the Matanuska geosyncline, the Seldovia geanticline, and the Chugach Mountains geosyncline, has a characteristic magnetic pattern.
The aeromagnetic data, compiled as total intensity aeromagnetic profiles, show several significant features which are consistent with the structural grain of the area. A two-dimensional anomaly was observed near the east edge of the area on all but the southernmost profiles, where it becomes obscure. Geologic evidence suggests that this feature, the Knik Arm anomaly, is produced by plutonic rocks that have been intruded along the Seldovia geanticline. Southeast of this anomaly the profiles are almost flat. This flatness indicates that magnetic rocks are deeply buried in this area, which is underlain by slate and graywacke deposited in the Chugach Mountains geosyncline.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6059","usgsCitation":"Grantz, A., Zietz, I., and Andreasen, G., 1960, An aeromagnetic reconnaissance of the Cook Inlet area, Alaska: U.S. Geological Survey Open-File Report 60-59, Report: 58 p.; 9 Plates: 27.85 x 35.82 inches or smaller, https://doi.org/10.3133/ofr6059.","productDescription":"Report: 58 p.; 9 Plates: 27.85 x 35.82 inches or smaller","costCenters":[],"links":[{"id":421784,"rank":11,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421783,"rank":10,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-3explanation.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421782,"rank":9,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421781,"rank":8,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421780,"rank":7,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421779,"rank":6,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421778,"rank":5,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421777,"rank":4,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421776,"rank":3,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-9.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421775,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1960/0059/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":144657,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1960/0059/report-thumb.jpg"}],"scale":"500000","country":"United States","state":"Alaska","otherGeospatial":"Cook Inlet area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -154.86692834754194,\n 58.461367338468136\n ],\n [\n -148.58541629436866,\n 58.461367338468136\n ],\n [\n -148.58541629436866,\n 61.78410578839723\n ],\n [\n -154.86692834754194,\n 61.78410578839723\n ],\n [\n -154.86692834754194,\n 58.461367338468136\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685c25","contributors":{"authors":[{"text":"Grantz, Arthur agrantz@usgs.gov","contributorId":2585,"corporation":false,"usgs":true,"family":"Grantz","given":"Arthur","email":"agrantz@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":168548,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":168549,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Andreasen, Gordon E.","contributorId":94272,"corporation":false,"usgs":true,"family":"Andreasen","given":"Gordon E.","affiliations":[],"preferred":false,"id":168550,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1948,"text":"wsp1476 - 1959 - Investigations of Sediment Transportation, Middle Loup River at Dunning, Nebraska: With Application of Data from Turbulence Flume","interactions":[],"lastModifiedDate":"2012-02-02T00:05:22","indexId":"wsp1476","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"1476","title":"Investigations of Sediment Transportation, Middle Loup River at Dunning, Nebraska: With Application of Data from Turbulence Flume","docAbstract":"An investigation of fluvial sediments of the Middle Loup River at Dunning, Nebr., was begun in 1946 and expanded in 1949 to provide information on sediment transportation. Construction of an artificial turbulence flume at which the total sediment discharge of the Middle Loup River at Dunning, Nebr., could be measured with suspended-sediment sampling equipment was completed in 1949. Since that time. measurements have been made at the turbulence flume and at several selected sections in a reach upstream and downstream from the flume. The Middle Loup River upstream from Dunning traverses the sandhills region of north-central Nebraska and has a drainage area of approximately 1,760 square miles. The sandhills are underlain by the Ogallala formation of Tertiary age and are mantled by loess and dune sand. The topography is characterized by northwest-trending sand dunes, which are stabilized by grass cover. The valley floor upstream from Dunning is generally about half a mile wide, is about 80 feet lower than the uplands, and is composed of sand that was mostly stream deposited. The channel is defined by low banks. Bank erosion is prevalent and is the source of most of the sediment load. The flow originates mostly from ground-water accretion and varies between about 200 and 600 cfs (cubic feet per second). Measured suspended-sediment loads vary from about 200 to 2,000 tons per day, of which about 20 percent is finer than 0.062 millimeter and 100 percent is finer than 0.50 millimeter. Total sediment discharges vary from about 500 to 3,500 tons per day, of which about 10 percent is finer than 0.062 millimeter, about 90 percent is finer than 0.50 millimeter, and about 98 percent is finer than 2.0 millimeters. The measured suspended-sediment discharge in the reach near Dunning averages about one-half of the total sediment discharge as measured at the turbulence flume. \r\n\r\nThis report contains information collected during the period October 1, 1948, to September 30, 1952. The information includes sediment discharges; particle-size analyses of total load, of measured suspended sediment, and of bed material; water discharges and other hydraulic data for the turbulence flume and the selected sections. \r\n\r\nSediment discharges have been computed with several different formulas, and insofar as possible, each computed load has been compared with data from the turbulence flume. Sediment discharges computed with the Einstein procedure did not agree well, in general, with comparable measured loads. However, a satisfactory representative cross section for the reach could not be determined with the cross sections that were selected for this investigation. If the computed cross section was narrower and deeper than a representative cross section for the reach, computed loads were high; and if the computed cross section was wider and shallower than a representative cross section for the reach, computed loads were low. Total sediment discharges computed with the modified Einstein procedure compared very well with the loads of individual size ranges and the measured total loads at the turbulence flume. Sediment discharges computed with the Straub equation averaged about twice the measured total sediment discharge at the turbulence flume. Bed-load discharges computed with the Kalinske equation were of about the right magnitude; however, high computed loads were associated with low total loads, low unmeasured loads, and low concentrations of measured suspended sediment coarser than 0.125 millimeter. Bed-load discharges computed with the Schoklitsch equation seemed somewhat high; about one-third of the computed loads were slightly higher than comparable unmeasured loads. Although, in general, high computed discharges with the Schoklitsch equation were associated with high measured total loads, high unmeasured loads, and high concentrations of measured suspended sediment coarser than 0.125 millimeter, the trend was not consistent. Bed-load discharges computed ","language":"ENGLISH","publisher":"Geological Survey (U.S.)","doi":"10.3133/wsp1476","collaboration":"Prepared in cooperation with the U.S. Bureau of Reclamation as part of a program of the Department of the Interior \r\nfor development of the Missouri River basin","usgsCitation":"Hubbell, D.W., and Matejka, D.Q., 1959, Investigations of Sediment Transportation, Middle Loup River at Dunning, Nebraska: With Application of Data from Turbulence Flume: U.S. Geological Survey Water Supply Paper 1476, vi, 123 p., https://doi.org/10.3133/wsp1476.","productDescription":"vi, 123 p.","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":138428,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1476/report-thumb.jpg"},{"id":27279,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1476/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":247069,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-06.pdf","size":"869","linkFileType":{"id":1,"text":"pdf"}},{"id":247070,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-07.pdf","size":"1038","linkFileType":{"id":1,"text":"pdf"}},{"id":247071,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-08.pdf","size":"2110","linkFileType":{"id":1,"text":"pdf"}},{"id":247072,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-09.pdf","size":"4117","linkFileType":{"id":1,"text":"pdf"}},{"id":247073,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-10.pdf","size":"4227","linkFileType":{"id":1,"text":"pdf"}},{"id":247074,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-11.pdf","size":"3435","linkFileType":{"id":1,"text":"pdf"}},{"id":247075,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-12.pdf","size":"1509","linkFileType":{"id":1,"text":"pdf"}},{"id":247076,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1476/plate-13.pdf","size":"3463","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afde4b07f02db696b8a","contributors":{"authors":[{"text":"Hubbell, David Wellington","contributorId":88330,"corporation":false,"usgs":true,"family":"Hubbell","given":"David","email":"","middleInitial":"Wellington","affiliations":[],"preferred":false,"id":144418,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Matejka, Donald Quintin","contributorId":103658,"corporation":false,"usgs":true,"family":"Matejka","given":"Donald","email":"","middleInitial":"Quintin","affiliations":[],"preferred":false,"id":144419,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}