The Blackstone River basin encompasses 335 square miles in south-central Massachusetts, including parts of Bristol, Middlesex, Norfolk, and Worcester Counties. Drainage areas, using the latest available 1:24,000 scale topographic maps, were computed for the first time for streams draining more than 3 square miles and were recomputed for data-collection sites. Streamflow characteristics, were calculated using a new data base with records through 1980. These characteristics include annual and monthly flow statistics, duration of daily flow values, and the annual 7-day mean low flow at the 2-year and 10-year recurrence intervals. The 7-day, 10-year low-flow values are presented for 31 partial-record sites and the procedures used to determine the hydrologic characteristics of the basin are summarized. Basin characteristics representing 14 commonly used indices to estimate various streamflows are presented for the six gaged streams in the Blackstone River basin. This gazetteer will aid in the planning and siting of water-resources-related activities and will provide a common data base for governmental agencies and the engineering and planning communities.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri844286","usgsCitation":"Wandle, S.W., and Phipps, A.F., 1984, Gazetteer of hydrologic characteristics of streams in Massachusetts — Blackstone River basin: U.S. Geological Survey Water-Resources Investigations Report 84-4286, iv, 30 p., https://doi.org/10.3133/wri844286.","productDescription":"iv, 30 p.","costCenters":[],"links":[{"id":59146,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1984/4286/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122261,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1984/4286/report-thumb.jpg"},{"id":394487,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_36129.htm"}],"country":"United States","state":"Massachusetts, Rhode Island","otherGeospatial":"Blackstone River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -71.862,\n 41.9\n ],\n [\n -71.3380,\n 41.9\n ],\n [\n -71.3380,\n 42.367\n ],\n [\n -71.862,\n 42.367\n ],\n [\n -71.862,\n 41.9\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b28e4b07f02db6b124b","contributors":{"authors":[{"text":"Wandle, S. W.","contributorId":86789,"corporation":false,"usgs":true,"family":"Wandle","given":"S.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":203123,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Phipps, A. F.","contributorId":44196,"corporation":false,"usgs":true,"family":"Phipps","given":"A.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":203122,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":55695,"text":"wdrMI831 - 1984 - Water resources data, Michigan, water year 1983","interactions":[],"lastModifiedDate":"2017-08-10T14:40:49","indexId":"wdrMI831","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":340,"text":"Water Data Report","code":"WDR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"MI-83-1","title":"Water resources data, Michigan, water year 1983","docAbstract":"Water resources data for the 1983 water year for Michigan consist of records of stage, discharge, and water quality of streams; stage, contents, and water quality of lakes and reservoirs; and water levels and water temperature of ground water. This report contains discharge records for 143 gaging stations; stage only records for 3 gaging stations; stage and contents for 5 lakes and reservoirs; water quality for 33 continuous-record stations; and water levels for 53 observation wells. Also included are 74 crest-stage partial-record stations and 8 low-flow partial-record stations. Additional water data were collected at various sites, not part of the systematic data-collection program, and are published as miscellaneous measurements. These data represent that part of the National Water Data System operated by the U.S. Geological Survey and cooperating State and Federal agencies in Michigan.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wdrMI831","collaboration":"Prepared in cooperation with the State of Michigan and with other agencies","usgsCitation":"Miller, J.B., Oberg, J., and Sieger, T., 1984, Water resources data, Michigan, water year 1983: U.S. Geological Survey Water Data Report MI-83-1, ix, 289 p., https://doi.org/10.3133/wdrMI831.","productDescription":"ix, 289 p.","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":344732,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wdr/1983/mi-83-1/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":181914,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wdr/1983/mi-83-1/report-thumb.jpg"}],"country":"United 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An important step in managing water resources is the delineation of recharge and discharge areas. Geohydrologic factors to be considered when delineating recharge and discharge areas include: altitude and configuration of the potentiometric surface; direction and magnitude of the gradient between the water table and the potentiometric surface; and thickness and permeability of the overlying sediments. Recharge to the aquifer comes almost entirely from rainfall within the Water Management District. Significant recharge occurs where the aquifer is at or very near land surface, and where the overlying sediments are very permeable sand so that recharge takes place downward leakage. Recharge also occurs through sinkholes, sinkhole lakes, and other lakes that have a good connection to the aquifer. Major recharge areas are delineated on the map. 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From a practical standpoint, such measurements are limited primarily to small streams due to excessively long channel mixing lengths required of larger streams. Very good accuracy can be obtained provided:
This manual describes the slug-injection and constant-rate injection methods of performing tracer-dilution measurements. Emphasis is on the use of fluorescent dyes as tracers and the equipment, field methods, and Laboratory procedures for performing such measurements. The tracer-velocity method is also briefly discussed.
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Three people were killed, and damages were estimated at $31 million. Cascade Lake Dam, downstream from Lawn Lake Dam, subsequently failed as a result of the flood, increasing the peak flow at this point from 7,210 cubic feet per second to 16,000 cubic feet per second. The flood wave took 3.28 hours to travel 12.5 miles to Lake Estes, where all the floodwater was stored. The channel of the Roaring River was scoured as much as 50 feet and widened 300 feet. An alluvial fan of 42.3 acres, containing 10 million cubic feet of material, was deposited at the mouth of the Roaring River, damming the Fall River and forming a 17-acre lake. Various methods were used to indirectly compute peak discharge, attenuation of flow, and flood traveltime. A version of the National Weather Service dam-break flood model was used to evaluate its performance on high-gradient streams, to provide supplemental hydrologic information, and to evaluate various scenarios of dam-break development. 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High-flow information given in this report is for streamflows unaffected by major regulation, such as by large reservoirs. High-flow magnitude and frequency data are given for 91 streamflow-gaging stations through-out Kansas. Results of frequency calculations are given for durations of high flow of 1, 3, 7, 15, 30, 60, 90, 120, and 183 consecutive days. Accuracy of the magnitude-frequency values is influenced by the variability of flow, the number of years of flow record, and the recurrence interval calculated.
High-flow magnitude and frequency for ungaged sites can be estimated from regression equations using significant drainage-basin characteristics of contributing-drainage area; 50-year, 24-hour rainfall; and free-water-surface evaporation. Standard errors of estimate for ungaged sites on ungaged streams range from 31 to 49 percent, generally increasing with recurrence interval. If an ungaged site is near a gaging station having 10 or more years of record on the same stream, the data for the gaging station may be used to improve the regression estimates.
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J.","contributorId":73575,"corporation":false,"usgs":true,"family":"Grimes","given":"D.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":173906,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Chaffee, M.A.","contributorId":108049,"corporation":false,"usgs":true,"family":"Chaffee","given":"M.A.","affiliations":[],"preferred":false,"id":173908,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cooley, E.F.","contributorId":83072,"corporation":false,"usgs":true,"family":"Cooley","given":"E.F.","email":"","affiliations":[],"preferred":false,"id":173907,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Nokleberg, W. J. 0000-0002-1574-8869","orcid":"https://orcid.org/0000-0002-1574-8869","contributorId":68312,"corporation":false,"usgs":true,"family":"Nokleberg","given":"W. 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In response the artesian head declined 180-240 ft. The land surface subsided 12.7 ft in San Jose, due to compaction of the fine-grained compressible beds. The subsidence resulted in flooding of lands, and the compaction of the sediments caused compressional failure of many well casings. From 1967 to 1975, the artesian head recovered 70 to 100 feet due to a fivefold increase in surface water imports, favorable local water supply, decreased withdrawal, and increased recharge. In 1960, the Geological Survey installed extensometers in core holes 1,000 ft deep in San Jose and Sunnyvale. Measurements of compaction of the confined aquifer system obtained from these extensometers demonstrate the marked decrease in rate of compaction in response to the major head recovery since 1967. In San Jose the rate decreased from about 1 ft/yr in 1961 to 0.1 ft/yr in 1973. The subsidence has been stopped by raising the artesian head in the aquifers until it equaled or exceeded the maximum pore pressures in the fine-grained beds. However, the subsidence will recommence if the artesian head is drawn down appreciably below the levels of 1971-73. (USGS)","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr84818","usgsCitation":"Poland, J.F., and Ireland, R.L., 1984, Land subsidence in the Santa Clara Valley, California as of 1980: U.S. Geological Survey Open-File Report 84-818, vi, 93 p. , https://doi.org/10.3133/ofr84818.","productDescription":"vi, 93 p. 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These characteristics are important to scientists and engineers who study the surface faulting and earthquakes and should also be helpful to those concerned with land use and development on or near faults in swetern Surprose Valley. In addition, faults apparently control the location of modern geothermal activity in Surprise Valley (Hedel, 1981) and are thus important to geothermal exploration.
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