{"pageNumber":"1446","pageRowStart":"36125","pageSize":"25","recordCount":41014,"records":[{"id":30603,"text":"wri874043 - 1988 - Nitrogen transport in a shallow outwash aquifer at Olean, Cattaraugus County, New York","interactions":[],"lastModifiedDate":"2023-01-13T19:34:49.834626","indexId":"wri874043","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4043","title":"Nitrogen transport in a shallow outwash aquifer at Olean, Cattaraugus County, New York","docAbstract":"<p>Groundwater beneath an industrial park at Olean, New York, contained nitrogen compounds in concentrations that in 1983 ranged from 10 to 1,280 mg/L as nitrogen, mainly in the form of ammonium. Continuous pumping from an industrial well field creates a cone of depression that prevents the nitrogen compounds from migrating to municipal-supply wells, 7,000 ft away. A two-dimensional solute transport model was used to simulate changes in nitrogen concentrations that would result from a permanent shutdown of the well field. The model assumed the nitrogen source decayed at an exponential rate with a decay constant of 0.3/year to account for nitrogen removed from the aquifer by pumping during 1978-84. The source of contamination was found to be sensitive to the volume of pumpage at the industrial well field, which altered the rate of groundwater flow through the contaminated area. Simulations of a permanent shutdown of the well field, assuming nitrogen migrates as a conservative solute, indicated that nitrogen-bearing groundwater would reach the municipal well field within 5 years and the peak concentrations at the municipal well field would range from 2 to 5 mg/L. Simulations of Langmuir adsorption of the dissolved ammonium with a one-dimensional model indicated that the arrival of the solute front at the municipal well field would be retarded by a factor of three.&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri874043","usgsCitation":"Yager, R.M., and Bergeron, M.P., 1988, Nitrogen transport in a shallow outwash aquifer at Olean, Cattaraugus County, New York: U.S. Geological Survey Water-Resources Investigations Report 87-4043, Report: vii, 51 p.; 6 Plates: 18.70 x 14.33 inches or smaller, https://doi.org/10.3133/wri874043.","productDescription":"Report: vii, 51 p.; 6 Plates: 18.70 x 14.33 inches or smaller","costCenters":[],"links":[{"id":59363,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4043/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":59362,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4043/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":59365,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4043/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":59364,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4043/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":59361,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4043/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":59367,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4043/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":59366,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4043/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":411900,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_46727.htm","linkFileType":{"id":5,"text":"html"}},{"id":123393,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4043/report-thumb.jpg"}],"country":"United States","state":"New York","county":"Cattaraugus County","city":"Olean","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -78.5075,\n              42.1158\n            ],\n            [\n              -78.5075,\n              42.0567\n            ],\n            [\n              -78.375,\n              42.0567\n            ],\n            [\n              -78.375,\n              42.1158\n            ],\n            [\n              -78.5075,\n              42.1158\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a54e4b07f02db62c485","contributors":{"authors":[{"text":"Yager, R. M.","contributorId":8069,"corporation":false,"usgs":true,"family":"Yager","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":203523,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bergeron, M. P.","contributorId":42969,"corporation":false,"usgs":true,"family":"Bergeron","given":"M.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":203524,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":44673,"text":"pp1456 - 1988 - The Geology and Remarkable Thermal Activity of Norris Geyser Basin, Yellowstone National Park, Wyoming","interactions":[],"lastModifiedDate":"2012-02-10T00:10:10","indexId":"pp1456","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","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":"1456","title":"The Geology and Remarkable Thermal Activity of Norris Geyser Basin, Yellowstone National Park, Wyoming","docAbstract":"Norris Geyser Basin, normally shortened to Norris Basin, is adjacent to the north rim of the Yellowstone caldera at the common intersection of the caldera rim and the Norris-Mammoth Corridor, a zone of faults, volcanic vents, and thermal activity that strikes north from the caldera rim to Mammoth Hot Springs. An east-west fault zone terminates the Gallatin Range at its southern end and extends from Hebgen Lake, west of the park, to Norris Basin. \r\n\r\nNo local evidence exists at the surface in Norris Basin for the two oldest Yellowstone volcanic caldera cycles (~2.0 and 1.3 m.y.B.P.). The third and youngest cycle formed the Yellowstone caldera, which erupted the 600,000-year-old Lava Creek Tuff. No evidence is preserved of hydrothermal activity near Norris Basin during the first 300,000.years after the caldera collapse. Glaciation probably removed most of the early evidence, but erratics of hot-spring sinter that had been converted diagenetically to extremely hard, resistant chalcedonic sinter are present as cobbles in and on some moraines and till from the last two glacial stages, here correlated with the early and late stages of the Pinedale glaciation <150,000 years B.P.). \r\n\r\nIndirect evidence for the oldest hydrothermal system at Norris Basin indicates an age probably older than both stages of Pinedale glaciation. Stream deposits consisting mainly of rounded quartz phenocrysts of the Lava Creek Tuff were subaerial, perhaps in part windblown and redeposited by streams. A few small rounded pebbles are interpreted as chalcedonic sinter of a still older cycle. None of these are precisely dated but are unlikely to be more than 150,000 to 200,000 years old.\r\n\r\n...Most studies of active hydrothermal areas have noted chemical differences in fluids and alteration products but have given little attention to differences and models to explain evolution in types. This report, in contrast, emphasizes the kinds of changes in vents and their changing chemical types of waters and then provides models for explaining these differences.\r\n\r\nNorris Basin is probably not an independent volcanic-hydrothermal system. The basin and nearby acid-leached areas (from oxidation of H2S-enriched vapor) are best considered as parts of the same system, extending from Norris Basin to Roaring Mountain and possibly to Mammoth. If so, are they parts of a single large system centered within the Yellowstone caldera, or are Norris Basin and the nearby altered areas both parts of one or more young independent corridor systems confined, at least in the shallow crust, to the Norris-Mammoth Corridor? Tentatively, we favor the latter relation, probably having evolved in the past ~300,000 years.\r\n\r\nA model for large, long-lived, volcanic-hydrothermal activity is also suggested, involving all of the crust and upper mantle and using much recent geophysical data bearing on crust-mantle interrelations. Our model for large systems is much superior to previous suggestions for explaining continuing hydrothermal activity over hundreds of thousands of years, but is less attractive for the smaller nonhomogenized volcanic system actually favored here for the Norris-Mammoth Corridor.","language":"ENGLISH","publisher":"Geological Survey (U.S.)","doi":"10.3133/pp1456","collaboration":"This report is out of print but is now available on the Web","usgsCitation":"White, D.E., Hutchinson, R.A., and Keith, T.E., 1988, The Geology and Remarkable Thermal Activity of Norris Geyser Basin, Yellowstone National Park, Wyoming (Out of print): U.S. Geological Survey Professional Paper 1456, Report: ix, 84 p.; Map Sheet: 36 x 42 inches, https://doi.org/10.3133/pp1456.","productDescription":"Report: ix, 84 p.; Map Sheet: 36 x 42 inches","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":169211,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":10752,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/1456/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112,43.5 ], [ -112,45.5 ], [ -109.25,45.5 ], [ -109.25,43.5 ], [ -112,43.5 ] ] ] } } ] }","edition":"Out of print","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c584","contributors":{"authors":[{"text":"White, Donald Edward","contributorId":84731,"corporation":false,"usgs":true,"family":"White","given":"Donald","email":"","middleInitial":"Edward","affiliations":[],"preferred":false,"id":230230,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hutchinson, Roderick A.","contributorId":34579,"corporation":false,"usgs":true,"family":"Hutchinson","given":"Roderick","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":230228,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Keith, Terry E.C.","contributorId":79099,"corporation":false,"usgs":true,"family":"Keith","given":"Terry","email":"","middleInitial":"E.C.","affiliations":[],"preferred":false,"id":230229,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":30613,"text":"wri874066 - 1988 - Simulated effects of ground-water management alternatives for the Salinas Valley, California","interactions":[],"lastModifiedDate":"2012-02-02T00:08:59","indexId":"wri874066","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4066","title":"Simulated effects of ground-water management alternatives for the Salinas Valley, California","docAbstract":"A two-dimensional digital groundwater flow model was developed to analyze the geohydrology of the groundwater basin in the Salinas Valley. The model was calibrated for steady-state and transient simulations by comparing simulated with measured or estimated inflows, outflows, and water levels for 1970-81. Preliminary estimates of hydraulic properties and some inflows and outflows were adjusted during model calibration. The simulated mean annual water budget for the basin was 559,500 acre-ft/yr each of outflow and inflow. Inflow components consisted of Salinas River recharge (38.3%), percolation of irrigation water (34.0%), small stream and Arroyo Seco recharge (20.9%), seawater intrusion (3.4%), and other sources (3.4%). Outflow components consisted of agricultural pumpage (91.5%), municipal pumpage (4.0%), and riparian phreatophyte evapotranspiration (4.5%). For the steady-state calibration, 70% of the simulated water levels were within 9 ft of measured water levels for 1970-81. A sensitivity analysis determined the overall stability of the model results. The model input variable that probably contributes most to the uncertainty of the results is the quantity of groundwater recharge contributed by irrigation-return flow to the unconfined aquifer. A 15% change in the estimate of this variable causes an 11% change in the simulated river-seepage rate and a 6% change in the simulated seawater intrusion rate. The calibrated model was used to investigate several water resources management alternatives. Projected pumpage increase at a rate of 1%/yr for 20 yr caused declines in mean annual water levels of 10 to 20 ft in some areas and an increase in seawater intrusion from 18,900 to 23 ,600 acre-ft/yr. Pumpage decreases in the coastal area decreased seawater intrusion more effectively than pumpage decreases farther inland. When pumpage was decreased uniformly throughout the valley, the decrease in seawater intrusion was only one-fourteenth the decrease in pumpage. Simulations indicated that replacement of groundwater pumpage with imported surface water in a 9,000 acre service area near the coast would result in a decrease in seawater intrusion equaling nearly one-half the quantity of imported water. (Author 's abstract)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri874066","usgsCitation":"Yates, E., 1988, Simulated effects of ground-water management alternatives for the Salinas Valley, California: U.S. Geological Survey Water-Resources Investigations Report 87-4066, vii, 79 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri874066.","productDescription":"vii, 79 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":160150,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4066/report-thumb.jpg"},{"id":59380,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4066/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b19e4b07f02db6a7f54","contributors":{"authors":[{"text":"Yates, E.B.","contributorId":77973,"corporation":false,"usgs":true,"family":"Yates","given":"E.B.","email":"","affiliations":[],"preferred":false,"id":203542,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":38395,"text":"pp1457 - 1988 - Geology and uranium deposits of the Cochetopa and Marshall Pass districts, Saguache and Gunnison counties, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:09:39","indexId":"pp1457","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","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":"1457","title":"Geology and uranium deposits of the Cochetopa and Marshall Pass districts, Saguache and Gunnison counties, Colorado","docAbstract":"The Cochetopa and Marshall Pass uranium districts are in Saguache and Gunnison Counties, south-central Colorado. Geologic mapping of both districts has shown that their structural history and geologic relationships have a bearing on the distribution and origin of their uranium deposits. In both districts, the principal uranium deposits are situated at the intersection of major faults with Tertiary erosion surfaces. These surfaces were buried by early Tertiary siliceous tuffs-- a likely source of the uranium. That uranium deposits are related to such unconformities in various parts of the world has been suggested by many other authors. The purpose of this study is to understand the geology of the two districts and to define a genetic model for uranium deposits that may be useful in the discovery and evaluation of uranium deposits in these and other similar geologic settings. \r\n\r\nThe Cochetopa and Marshall Pass uranium districts produced nearly 1,200 metric tons of uranium oxide from 1956 to 1963. Several workings at the Los Ochos mine in the Cochetopa district, and the Pitch mine in the Marshall Pass district, accounted for about 97 percent of this production, but numerous other occurrences of uranium are known in the two districts. As a result of exploration of the Pitch deposit in the 1970's, a large open-pit mining operation began in 1978. \r\n\r\nProterozoic rocks in both districts comprise metavolcanic, metasedimentary, and igneous units. Granitic rocks, predominantly quartz monzonitic in composition, occupy large areas. In the northwestern part of the Cochetopa district, metavolcanic and related metasedimentary rocks are of low grade (lower amphibolite facies). In the Marshall Pass district, layered metamorphic rocks are predominantly metasedimentary and are of higher (sillimanite subfacies) grade than the Cochetopa rocks. \r\n\r\nPaleozoic sedimentary rocks in the Marshall Pass district range from Late Cambrian to Pennsylvanian in age and are 700 m thick. The Paleozoic rocks include, from oldest to youngest, the Sawatch Quartzite, Manitou Dolomite, Harding Quartzite, Fremont Dolomite, Parting Formation and Dyer Dolomite of the Chaffee Group, Leadville Dolomite, and Belden Formation. In the Cochetopa district, Paleozoic rocks are absent. \r\n\r\nMesozoic sedimentary rocks overlie the Precambrian rocks in the Cochetopa district and comprise the Junction Creek Sandstone, Morrison Formation, Dakota Sandstone, and Mancos Shale. In the Marshall Pass district, Mesozoic rocks are absent and were presumably removed by pre-Tertiary erosion. \r\n\r\nTertiary volcanic rocks were deposited on an irregular surface of unconformity; they blanketed both districts but have been eroded, away from much of the area. They include silicic ash flows as well as andesitic lava flows and breccias. In the Marshall Pass district, a 20to 20D-m thickness of waterlaid tuff of early Tertiary age indicates the former presence of a lake over much of the district. \r\n\r\nIn the Cochetopa district, faults have a predominantly east-west trend, and the major Los Ochos fault shows displacement during Laramide time. In the Marshall Pass district, the Chester fault is a major north-trending reverse fault along which Proterozoic rocks have been thrust westward over Paleozoic and Proterozoic rocks. Displacement on the Chester fault was almost entirely of Laramide age. \r\n\r\nBoth faults and old erosion surfaces or unconformities are important in the origin of uranium deposits because of their influence on the movement and localization of ore-forming solutions. In the Cochetopa district, all the known uranium occurrences crop out within 100 m of the inferred position of the unconformity surface beneath the Tertiary volcanic rocks. Much of the district was part of the drainage of an ancestral Cochetopa Creek. The principal uranium deposit, at the Los Ochos mine, is localized along the Los Ochos fault and is near the bottom of the paleovalley where the paleovalley crosses the fault. This ","language":"ENGLISH","doi":"10.3133/pp1457","usgsCitation":"Olson, J.C., 1988, Geology and uranium deposits of the Cochetopa and Marshall Pass districts, Saguache and Gunnison counties, Colorado: U.S. Geological Survey Professional Paper 1457, 44 p., https://doi.org/10.3133/pp1457.","productDescription":"44 p.","costCenters":[],"links":[{"id":119815,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1457/report-thumb.jpg"},{"id":64754,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1457/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db6841b2","contributors":{"authors":[{"text":"Olson, Jerry C.","contributorId":89202,"corporation":false,"usgs":true,"family":"Olson","given":"Jerry","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":219742,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":29498,"text":"wri874248 - 1988 - Hydrogeology and predevelopment flow in the Texas Gulf Coast aquifer systems","interactions":[],"lastModifiedDate":"2016-08-10T15:19:13","indexId":"wri874248","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4248","title":"Hydrogeology and predevelopment flow in the Texas Gulf Coast aquifer systems","docAbstract":"<p>A multilayered ground-water flow system exists in the Coastal Plain sediments of Texas. The Tertiary and Quaternary clastic deposits have an area! extent of 128,000 square miles onshore and in the Gulf of Mexico. Two distinct aquifer systems are recognized for the sediments, which range in thickness from a few feet to more than 12,000 feet. The older system the Texas coastal uplands aquifer system consists of four aquifers and two confining units in the Wilcox and Claiborne Groups. It is bounded from below by the practically impermeable Midway confining unit or by the top of the geopressured zone. It is bounded from above by the poorly permeable Vicksburg-Jackson confining unit, which separates it from the younger coastal lowlands aquifer system. The coastal lowlands aquifer system consists of five permeable zones and two confining units that range in age from Oligocene to Holocene. The hydrogeologic units of both systems are exposed in bands that parallel the coastline. The units dip and thicken toward the Gulf.</p>\n<p>Quality of water in the aquifer systems varies greatly, with dissolved solids ranging from a few hundred to more than 200,000 milligrams per liter.</p>\n<p>A three-dimensional, variable-density digital model was developed to simulate predevelopment flow in the aquifer systems, for which steady-state conditions were assumed. Horizontal hydraulic conductivities of the aquifers and permeable zones in the calibrated model range from 15 feet per day for the middle Wilcox aquifer, to 170 feet per day for the Holocene-upper Pleistocene aquifer. Vertical hydraulic conductivities range from 1 x 10<sup>-5</sup> foot per day for the Vicksburg-Jackson confining unit, to 1 x 10<sup>-2</sup> foot per day for four of the aquifers and permeable zones. The simulated values of transmissivity and leakance are functions of the percent of sand that is present in each model grid block.</p>\n<p>There is a large range in precipitation across the study area, from about 21 inches per year in the west to about 56 inches per year in the east. Eastward from a line through Corpus Christi and San Antonio, average annual precipitation ranges from about 30 to about 56 inches. A few inches per year reaches the saturated zone in topographically high areas and is discharged in low areas as evapotranspiration, seepage, springflow, and stream base flow. A smaller amount of water flows through the aquifers and permeable zones downdip from the outcrop areas. This flow results in upward or downward leakage into adjacent hydrogeologic units, but is generally upward into overlying units.</p>\n<p>Westward from the line through Corpus Christi and San Antonio, average annual precipitation ranges from about 30 to about 21 inches. The general pattern of flow in the aquifers and permeable zones is similar to that in the east, but rates of flow are somewhat smaller. In contrast to the east, ground-water discharge in the west is generally not visible. Evapotranspiration is the main mechanism for ground-water discharge, with most ground water being discharged through evapotranspiration by phreatophytes.</p>\n<p>Simulated discharge and recharge rates in the combined outcrop areas of all units do not exceed 6 inches per year. The large rates occur in small, local topographically low and high areas. The average discharge rate simulated in the outcrops of the units is 0.45 inch per year. The recharge area is considerably smaller than the discharge area, and the average recharge rate over this smaller area is 0.74 inch per year.</p>\n<p>Total simulated recharge in the outcrop areas is 269 million cubic feet per day, which is offset by an equal amount of discharge in the outcrop areas. The smallest rates of leakage are across the Vicksburg-Jackson confining unit, with downward and upward rates of less than one million cubic feet per day. The greatest rate of leakage is 47 million cubic feet per day upward into the Holocene-upper Pleistocene permeable zone.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Austin, TX","doi":"10.3133/wri874248","usgsCitation":"Ryder, P.D., 1988, Hydrogeology and predevelopment flow in the Texas Gulf Coast aquifer systems: U.S. Geological Survey Water-Resources Investigations Report 87-4248, vii, 109 p., https://doi.org/10.3133/wri874248.","productDescription":"vii, 109 p.","numberOfPages":"116","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":58346,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4248/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":126794,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4248/report-thumb.jpg"}],"country":"United States","state":"Texas","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -94.1748046875,\n              33.578014746143985\n            ],\n            [\n              -95.20751953125,\n              33.063924198120645\n            ],\n            [\n              -99.16259765625,\n              28.07198030177986\n            ],\n            [\n              -99.580078125,\n              27.60567082646547\n            ],\n            [\n              -99.11865234374999,\n              26.43122806450644\n            ],\n            [\n              -98.1298828125,\n              26.03704188651584\n            ],\n            [\n              -97.18505859374999,\n              25.997549919572112\n            ],\n            [\n              -97.36083984375,\n              27.527758206861886\n            ],\n            [\n              -96.328125,\n              28.51696944040106\n            ],\n            [\n              -95.361328125,\n              28.92163128242129\n            ],\n            [\n              -94.482421875,\n              29.53522956294847\n            ],\n            [\n              -93.91113281249999,\n              29.7453016622136\n            ],\n            [\n              -93.515625,\n              31.16580958786196\n            ],\n            [\n              -94.02099609375,\n              32.02670629333614\n            ],\n            [\n              -94.04296874999999,\n              33.578014746143985\n            ],\n            [\n              -94.1748046875,\n              33.578014746143985\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db625321","contributors":{"authors":[{"text":"Ryder, Paul D.","contributorId":60188,"corporation":false,"usgs":true,"family":"Ryder","given":"Paul","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":201611,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":28014,"text":"wri874283 - 1988 - Hydrogeology and water-supply potential of the water-table aquifer on Dauphin Island, Alabama","interactions":[],"lastModifiedDate":"2012-02-02T00:08:38","indexId":"wri874283","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4283","title":"Hydrogeology and water-supply potential of the water-table aquifer on Dauphin Island, Alabama","docAbstract":"The water table aquifer on Dauphin Island, Alabama, consists of a thin veneer of Holocene sand and an underlying Pleistocene unit locally known as the Gulfport Formation. The aquifer is from 28 to 35 ft thick with a thick marine clay at its base. Water in the aquifer generally is low in chloride content except near the coast. Excessively high iron concentrations in groundwater were found locally. A two-dimensional finite-difference groundwater flow model of the water table aquifer on Dauphin Island was used in the steady-state mode to evaluate the flow system under steady-state conditions. Model input data were obtained primarily from 40 test wells, 2 aquifer tests, continuous recording of groundwater levels, and rainfall. The model was calibrated to the low water-table conditions of July 1985 and high water table conditions of April 1985. The model was also used to simulate pumpage from the aquifer under transient conditions with no rainfall. Patterns of computed head changes compared favorably to the natural recession of water levels for the periods of April to May 1985 and May to June 1985. Simulation of groundwater withdrawals in the transient model showed the feasibility of producing 0.6 million gallons/day from eight wells that tap the water table aquifer without inducing lateral seawater encroachment. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri874283","usgsCitation":"Kidd, R.E., 1988, Hydrogeology and water-supply potential of the water-table aquifer on Dauphin Island, Alabama: U.S. Geological Survey Water-Resources Investigations Report 87-4283, vii, 49 p. :ill., (some col.), maps ;28 cm., https://doi.org/10.3133/wri874283.","productDescription":"vii, 49 p. :ill., (some col.), maps ;28 cm.","costCenters":[],"links":[{"id":120060,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4283/report-thumb.jpg"},{"id":56841,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4283/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b23e4b07f02db6ade77","contributors":{"authors":[{"text":"Kidd, R. E.","contributorId":91145,"corporation":false,"usgs":true,"family":"Kidd","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":199069,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":28321,"text":"wri874284 - 1988 - Hydrogeology and simulated effects of ground-water development on an unconfined aquifer in the Closed Basin Division, San Luis Valley, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:08:49","indexId":"wri874284","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4284","title":"Hydrogeology and simulated effects of ground-water development on an unconfined aquifer in the Closed Basin Division, San Luis Valley, Colorado","docAbstract":"Wells completed in an unconfined aquifer in the Closed Basin Division of the San Luis Valley Project, Colorado, are expected to provide about 101,800 acre-ft of groundwater/year to the Rio Grande when this project is completed. Lowering of groundwater levels in the unconfined aquifer is expected to decrease the quantity of groundwater that is lost by evapotranspiration. The aquifer system, which consists of an unconfined aquifer that is 50 to 130 ft thick, overlies a thick, leaky confined aquifer. Groundwater moves from the edge of the valley toward a topographic low near the center of the Closed Basin Division, where it is lost by evapotranspiration. A two-dimensional groundwater flow model was used to evaluate the effects of projected withdrawal of about 141 cu ft/sec by 168 wells throughout a 20-year period. The simulated pumpage resulted in a projected drawdown greater than 0.1 ft in the water-levels of the unconfined aquifer over an area of about 370 sq mi. Maximum simulated drawdown was 25 ft. Simulations indicate that about 66 % of the water to be withdrawn from the unconfined aquifer would be derived from decreases of evapotranspiration, 26% from induced leakage from an underlying confined aquifer, and 8% from storage of the unconfined aquifer. Model simulations were based only on withdrawals from wells completed in the unconfined aquifer. Pumpage from the confined aquifer was not simulated. Upward leakage from the confined aquifer predicted by the model, results from the simulated declines of the potentiometric surface in the unconfined aquifer. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri874284","usgsCitation":"Leonard, G., and Watts, K.R., 1988, Hydrogeology and simulated effects of ground-water development on an unconfined aquifer in the Closed Basin Division, San Luis Valley, Colorado: U.S. Geological Survey Water-Resources Investigations Report 87-4284, vii, 42 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri874284.","productDescription":"vii, 42 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":124044,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4284/report-thumb.jpg"},{"id":57136,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4284/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4af4e4b07f02db69200a","contributors":{"authors":[{"text":"Leonard, G.J.","contributorId":78371,"corporation":false,"usgs":true,"family":"Leonard","given":"G.J.","email":"","affiliations":[],"preferred":false,"id":199589,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Watts, Kenneth R.","contributorId":43783,"corporation":false,"usgs":true,"family":"Watts","given":"Kenneth","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":199588,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":29433,"text":"wri874220 - 1988 - Water resources of the Apostle Islands National Lakeshore, northern Wisconsin","interactions":[],"lastModifiedDate":"2015-10-20T10:39:12","indexId":"wri874220","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4220","title":"Water resources of the Apostle Islands National Lakeshore, northern Wisconsin","docAbstract":"<p>The Apostle Islands National Lakeshore consists of 21 islands, part of the Bayfield Peninsula, and the adjacent waters of Lake Superior. Selected water resources of the Apostle Islands National Lakeshore were assessed to aid the National Park Service in developing and managing the Lakeshore and to provide a data base against which future changes can be compared. This summary of water-resources data, collected by the U.S. Geological Survey during 1979-84, provides a qualitative description of selected hydrologic components of the Lakeshore.</p>\n<p>Streamflow in the Lakeshore area is characterized by typical seasonal fluctuations. Flow in Sand River at State Highway 13 ranged from 3.9 to 1,630 cubic feet per second. The recurrence interval of the maximum observed discharge was about 4 years. The minimum observed 7-day low flow was 3.86 cubic feet per second.</p>\n<p>The greatest concentrations of most chemical constituents in Bayfield Peninsula streams occurred during base flow.</p>\n<p>Annual sediment loads in Sand River at State Highway 13 ranged from 977 tons in 1980 water year to 24,600 tons in 1984 water year.The average annual sediment load transported by Bayfield Peninsula streams to the National Lakeshore area of Lake Superior is estimated to be 44,000 tons. Annual phosphorus loads ranged from 1,400 pounds in 1980 water year to 11,100 pounds in 1984 water year. The average annual phosphorus load transported by Bayfield Peninsula streams to the National Lakeshore area of Lake Superior is estimated to be 21,500 pounds.</p>\n<p>Few island streams flow perennially, but Oak Island streams generally yield more base-flow runoff than Stockton Island streams. The base flow of Oak Island streams is dominated by ground-water discharge, whereas Stockton Island stream base flow is sustained by seepage from wetlands and beaver ponds.</p>\n<p>There are two major lagoons in the Lakeshore, the Outer Island Lagoon's area is 53 acres and its maximum depth is 7 feet. Dominant inflow to the lagoon is from precipitation on its surface and seepage from an adjacent bog. Outflow during open-water periods is dominated by evaporation. Ground-water seepage from the lagoon toward Lake Superior occurs yearround. The lagoon's water is acidic and has low specific conductance and generally small concentrations of most chemical constituents.</p>\n<p>The Michigan Island Lagoon is about 4 acres in area and its maximum depth is 6.5 feet. The most significant sources of inflow appear to be precipitation and wave washover from Lake Superior.</p>\n<p>Water from four deep-water monitoring sites in Lake Superior revealed concentrations of total phosphorus, organic carbon, and recoverable mercury ranging from &lt;0.01 to 0.02 milligrams per liter, 1.1 to 5.3 milligrams per liter and &lt;0.1 to 0.1 micrograms per liter, respectively. Neither pesticide residues nor fecal coliform bacteria were detected in the water column. Total phosphorus concentrations in bottom sediment ranged from 50 to 470 milligrams per kilogram and were related directly to the percentage of fine-grained (&lt; 0.0625 millimeters) sediment particles. Traces of only two pesticide residues- DDE and DDT were detected in sediment. The most abundant benthic macroinvertebrate was Pontoporeia affinis, which was found in densities of from 960 to 2,100 organisms per square meter.</p>\n<p>No adverse affects resulting from visitor use were detected in the shallow-water, heavy-use areas in Presque Isle Bay off Stockton Island or in the waters between Rocky and South Twin Islands. Phosphorus and organic-carbon concentrations were similar to those observed in the deep-water area; mercury was not detected in water from either area.</p>\n<p>Ground-water use in the National Lakeshore is primarily for consumption by Lakeshore visitors and employees. Of 14 wells constructed from 1979-84, 4 were finished in glacial sand and gravel, and 10 were finished in sandstone. Specific capacities ranged from 0.63 to 50 gallon per minute per foot. Average concentrations of dissolved solids are moderate and concentrations of heavy metals did not exceed Wisconsin's primary health standard.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri874220","collaboration":"Prepared in cooperation with the National Park Service","usgsCitation":"Rose, W.J., 1988, Water resources of the Apostle Islands National Lakeshore, northern Wisconsin: U.S. Geological Survey Water-Resources Investigations Report 87-4220, vi, 44 p., https://doi.org/10.3133/wri874220.","productDescription":"vi, 44 p.","numberOfPages":"50","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":122647,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4220/report-thumb.jpg"},{"id":58281,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4220/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","county":"Bayfield County","otherGeospatial":"Apostle Islands National Lakeshore, Lake Superior","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -90.98876953125,\n              46.803819640791566\n            ],\n            [\n              -90.77178955078125,\n              46.702202151643455\n            ],\n            [\n              -90.54107666015625,\n              46.78501604269254\n            ],\n            [\n              -90.37628173828125,\n              46.948387301863534\n            ],\n            [\n              -90.31036376953125,\n              47.040182144806664\n            ],\n            [\n              -90.4449462890625,\n              47.14676553125098\n            ],\n            [\n              -90.75256347656249,\n              47.14676553125098\n            ],\n            [\n              -90.98602294921875,\n              47.06638028321398\n            ],\n            [\n              -91.0821533203125,\n              46.965259400349275\n            ],\n            [\n              -91.23321533203125,\n              46.880845705719146\n            ],\n            [\n              -91.219482421875,\n              46.8094594390422\n            ],\n            [\n              -90.98876953125,\n              46.803819640791566\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b15e4b07f02db6a4d0b","contributors":{"authors":[{"text":"Rose, W. J.","contributorId":14433,"corporation":false,"usgs":true,"family":"Rose","given":"W.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":201519,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":44822,"text":"wri884076 - 1988 - Potential yields of wells in unconsolidated aquifers in upstate New York — Niagara sheet","interactions":[],"lastModifiedDate":"2022-01-26T19:25:09.049505","indexId":"wri884076","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"88-4076","title":"Potential yields of wells in unconsolidated aquifers in upstate New York — Niagara sheet","docAbstract":"<p>This map depicts the locations and potential well yields of unconsolidated aquifers in western New York at a scale of 1:250 ,000. It also delineates segments of aquifers that are used for public water supplies and designated by the New York State Department of Environmental Conservation as Primary Water Supply Aquifers. The map also lists published reports that give detailed information on each area. Most aquifers were deposited in low areas, such as valleys and plains, during deglaciation of the region. Thick, permeable, well-sorted sand and gravel units yield large quantities of water - more than 100 gal/min - to properly constructed wells. Thin sand units and sand and gravel units and thicker gravel units that have a large content of silt and fine sand yield moderate amounts of water, 10 to 100 gal/min. Dug wells that tap till or lacustrine deposits yield less than 5 gal/min. Well yields from bedrock are not indicated. (USGS)</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri884076","usgsCitation":"Miller, T.S., 1988, Potential yields of wells in unconsolidated aquifers in upstate New York — Niagara sheet: U.S. Geological Survey Water-Resources Investigations Report 88-4076, 1 Plate: 46.43 × 41.94 inches, https://doi.org/10.3133/wri884076.","productDescription":"1 Plate: 46.43 × 41.94 inches","costCenters":[],"links":[{"id":171180,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":394891,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_46996.htm"},{"id":82156,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4076/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New York","otherGeospatial":"Niagara sheet","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -79.354248046875,\n              42.52879629320373\n            ],\n            [\n              -77.783203125,\n              42.52879629320373\n            ],\n            [\n              -77.783203125,\n              43.31718491566705\n            ],\n            [\n              -79.354248046875,\n              43.31718491566705\n            ],\n            [\n              -79.354248046875,\n              42.52879629320373\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a867a","contributors":{"authors":[{"text":"Miller, Todd S. tsmiller@usgs.gov","contributorId":1190,"corporation":false,"usgs":true,"family":"Miller","given":"Todd","email":"tsmiller@usgs.gov","middleInitial":"S.","affiliations":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"preferred":true,"id":230499,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":26019,"text":"wri884010 - 1988 - Preliminary evaluation of ground-water flow in Bear Creek Valley, the Oak Ridge Reservation, Tennessee","interactions":[],"lastModifiedDate":"2015-10-22T09:10:40","indexId":"wri884010","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"88-4010","title":"Preliminary evaluation of ground-water flow in Bear Creek Valley, the Oak Ridge Reservation, Tennessee","docAbstract":"<p>Bear Creek Valley, Tennessee contains hazardous waste disposal sites where contaminants leach into ground and surface water. Groundwater flow and the potential migration of contaminants is poorly understood. The Valley is underlain by calcareous shale that contains limestone units. Ridges to the north and south are underlain by interbedded sandstones, siltstone and shale, and by massive, siliceous dolomite, respectively. The bedrock, which dips about 45 degrees southeast, is overlain by regolith to a maximum thickness of 80 ft. Observed hydraulic conductivities for the regolith range from 0.01 to 13 ft/day, and for the bedrock, from 0.001 to 11 ft/day. Groundwater flow is probably toward streams and is preferential along strike because of an areal anisotropy in hydraulic conductivity. A cross sectional groundwater flow model was used to test the conceptualized flow system and to help identify areas where additional data are needed. The preliminary model shows a pattern of recharge at both ridges, flow toward the valley, and upward flow that discharges into Bear Creek. Final model values of hydraulic conductivity in the bedrock range from 0.01 to 0.1 ft/day and reflect an areal anisotropy ratio of 1:5. Simulated recharge was 10 inches/year. (USGS)</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri884010","collaboration":"Prepared in cooperation with the U.S. Department of Energy","usgsCitation":"Bailey, Z., 1988, Preliminary evaluation of ground-water flow in Bear Creek Valley, the Oak Ridge Reservation, Tennessee: U.S. Geological Survey Water-Resources Investigations Report 88-4010, iii, 12 p., https://doi.org/10.3133/wri884010.","productDescription":"iii, 12 p.","numberOfPages":"18","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":157624,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri884010.jpg"},{"id":310320,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1988/4010/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Tennessee","county":"Roane County","otherGeospatial":"Bear Valley, Oak Ridge Reservation","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-84.2716,35.9104],[-84.2717,35.9072],[-84.2628,35.8971],[-84.268,35.8958],[-84.2792,35.9033],[-84.2843,35.9015],[-84.285,35.8947],[-84.2797,35.8806],[-84.2814,35.8783],[-84.2848,35.8775],[-84.2972,35.8854],[-84.3005,35.8863],[-84.309,35.8882],[-84.3227,35.8866],[-84.3283,35.8899],[-84.3299,35.8931],[-84.3331,35.8791],[-84.3426,35.8316],[-84.3477,35.8325],[-84.3729,35.8224],[-84.3758,35.8166],[-84.3812,35.8058],[-84.3802,35.798],[-84.3775,35.7916],[-84.3885,35.7823],[-84.3807,35.7776],[-84.3888,35.7677],[-84.3916,35.7701],[-84.3994,35.7742],[-84.4073,35.7775],[-84.4101,35.7776],[-84.4164,35.7767],[-84.421,35.7736],[-84.424,35.7664],[-84.4242,35.7578],[-84.4294,35.751],[-84.4368,35.7502],[-84.4435,35.7549],[-84.4474,35.7604],[-84.4531,35.7554],[-84.471,35.7389],[-84.4947,35.7169],[-84.5106,35.7167],[-84.5169,35.7122],[-84.5216,35.7059],[-84.5218,35.6946],[-84.5263,35.6951],[-84.5264,35.6915],[-84.5303,35.6915],[-84.5321,35.6879],[-84.5322,35.6843],[-84.522,35.6837],[-84.5215,35.6769],[-84.5306,35.677],[-84.5313,35.6707],[-84.5398,35.6703],[-84.5399,35.6658],[-84.5489,35.6663],[-84.5491,35.6591],[-84.5751,35.6594],[-84.5758,35.6521],[-84.5843,35.6518],[-84.585,35.6445],[-84.6201,35.645],[-84.6198,35.659],[-84.6306,35.6587],[-84.631,35.666],[-84.6283,35.69],[-84.6226,35.6963],[-84.6265,35.6995],[-84.6241,35.7067],[-84.6301,35.719],[-84.6368,35.7205],[-84.6362,35.7246],[-84.6453,35.7247],[-84.6448,35.7169],[-84.6545,35.7175],[-84.654,35.7102],[-84.6631,35.7103],[-84.6638,35.7031],[-84.6723,35.7032],[-84.6716,35.7104],[-84.6761,35.7105],[-84.6766,35.7173],[-84.6986,35.718],[-84.6985,35.7253],[-84.699,35.733],[-84.6988,35.7411],[-84.7028,35.7416],[-84.7141,35.7422],[-84.7163,35.7468],[-84.7236,35.7532],[-84.7287,35.7523],[-84.7327,35.7506],[-84.7389,35.7516],[-84.7439,35.7539],[-84.7524,35.7567],[-84.7541,35.7594],[-84.7522,35.7667],[-84.751,35.7707],[-84.7464,35.7752],[-84.7419,35.7766],[-84.7379,35.7792],[-84.7383,35.7869],[-84.7377,35.7906],[-84.741,35.7933],[-84.7472,35.7948],[-84.7489,35.7952],[-84.7551,35.798],[-84.763,35.8022],[-84.7731,35.8114],[-84.7804,35.8123],[-84.7844,35.8124],[-84.7889,35.8152],[-84.7872,35.8165],[-84.7832,35.8187],[-84.7803,35.8237],[-84.7785,35.8268],[-84.7722,35.83],[-84.7659,35.8344],[-84.7578,35.8425],[-84.7492,35.8488],[-84.7383,35.8532],[-84.7309,35.859],[-84.7251,35.8653],[-84.7187,35.8734],[-84.7041,35.8941],[-84.6978,35.8999],[-84.6858,35.9025],[-84.6818,35.9052],[-84.6795,35.9075],[-84.6749,35.9115],[-84.6703,35.9155],[-84.6611,35.9181],[-84.6566,35.9199],[-84.653,35.9262],[-84.6502,35.928],[-84.6462,35.9275],[-84.6433,35.9288],[-84.6393,35.931],[-84.6319,35.9305],[-84.6256,35.9336],[-84.6194,35.934],[-84.6159,35.9385],[-84.609,35.9411],[-84.6067,35.9456],[-84.6049,35.9515],[-84.602,35.9524],[-84.5969,35.9501],[-84.5907,35.9486],[-84.5844,35.9495],[-84.5765,35.9503],[-84.5543,35.9505],[-84.5547,35.96],[-84.554,35.9645],[-84.5374,35.9707],[-84.5288,35.9738],[-84.5169,35.9759],[-84.4939,35.9847],[-84.4888,35.9851],[-84.4774,35.9849],[-84.4672,35.9839],[-84.4564,35.9842],[-84.4461,35.9863],[-84.4185,36.0027],[-84.4065,36.008],[-84.3983,36.0156],[-84.3868,36.0214],[-84.3573,36.0441],[-84.347,36.048],[-84.3418,36.0493],[-84.3397,36.0443],[-84.3359,36.0338],[-84.3343,36.0302],[-84.3327,36.0243],[-84.3257,36.0069],[-84.3204,35.9919],[-84.3094,35.9722],[-84.2854,35.9301],[-84.2721,35.9113],[-84.2716,35.9104]]]},\"properties\":{\"name\":\"Roane\",\"state\":\"TN\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c405","contributors":{"authors":[{"text":"Bailey, Z. C.","contributorId":54587,"corporation":false,"usgs":true,"family":"Bailey","given":"Z. C.","affiliations":[],"preferred":false,"id":195653,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":29379,"text":"wri874152 - 1988 - Simulated water-level and water-quality changes in the bolson-fill aquifer, Post Headquarters area, White Sands Missile Range, New Mexico","interactions":[],"lastModifiedDate":"2012-02-02T00:08:55","indexId":"wri874152","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4152","title":"Simulated water-level and water-quality changes in the bolson-fill aquifer, Post Headquarters area, White Sands Missile Range, New Mexico","docAbstract":"The quantity of freshwater available in the Post Headquarters well field, White Sand Missile Range, New Mexico, is limited and its quality is threatened by saltwater enroachment. A three-dimensional, finite-difference, groundwater flow model and a cross-sectional, density-dependent solute-transport model were constructed to simulate possible future water level declines and water quality changes in the Post Headquarters well field. A six-layer flow model was constructed using hydraulic-conductivity values in the upper 600 ft of saturated aquifer ranging from 0.1 to 10 ft/day, specific yield of 0.15, and average recharge of about 1,590 acre-ft/yr. Water levels simulated by the model closely matched measured water levels for 1948-82. Possible future water level changes for 1983-2017 were simulated using rates of groundwater withdrawal of 1,033 and 2 ,066 acre-ft/year and wastewater return flow of 0 or 30% of the groundwater withdrawal rate. The cross-sectional solute-transport model indicated that the freshwater zone is about 1,500 to 2,000 ft thick beneath the well field. Transient simulations show that solutes probably will move laterally toward the well field rather than from beneath the well field. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri874152","usgsCitation":"Risser, D.W., 1988, Simulated water-level and water-quality changes in the bolson-fill aquifer, Post Headquarters area, White Sands Missile Range, New Mexico: U.S. Geological Survey Water-Resources Investigations Report 87-4152, viii, 71 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri874152.","productDescription":"viii, 71 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":159752,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4152/report-thumb.jpg"},{"id":58224,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4152/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f9e4b07f02db5f30c2","contributors":{"authors":[{"text":"Risser, D. W.","contributorId":48211,"corporation":false,"usgs":true,"family":"Risser","given":"D.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":201434,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":33801,"text":"b1795 - 1988 - Development of a velocity model for locating aftershocks in the Sierra Pie de Palo region of western Argentina","interactions":[],"lastModifiedDate":"2012-02-02T00:09:37","indexId":"b1795","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","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":"1795","title":"Development of a velocity model for locating aftershocks in the Sierra Pie de Palo region of western Argentina","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/b1795","usgsCitation":"Bollinger, G.A., and Langer, C., 1988, Development of a velocity model for locating aftershocks in the Sierra Pie de Palo region of western Argentina: U.S. Geological Survey Bulletin 1795, iii, 16 p. :ill., maps ;28 cm., https://doi.org/10.3133/b1795.","productDescription":"iii, 16 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":167170,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1795/report-thumb.jpg"},{"id":61706,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1795/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9be4b07f02db65e19e","contributors":{"authors":[{"text":"Bollinger, G. A.","contributorId":55809,"corporation":false,"usgs":true,"family":"Bollinger","given":"G.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":211958,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Langer, C.J.","contributorId":31395,"corporation":false,"usgs":true,"family":"Langer","given":"C.J.","email":"","affiliations":[],"preferred":false,"id":211957,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":26702,"text":"wri884054 - 1988 - Potential hydrologic effects of a drainage system in McMillan delta and water impoundment in Brantley Reservoir, Eddy County, New Mexico","interactions":[],"lastModifiedDate":"2012-02-02T00:08:34","indexId":"wri884054","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"88-4054","title":"Potential hydrologic effects of a drainage system in McMillan delta and water impoundment in Brantley Reservoir, Eddy County, New Mexico","docAbstract":"Construction of a proposed drainage system could result in a moderate flow increase in the Pecos River downstream from the McMillan delta. The potential effect of a new line channel of the Pecos River in McMillan delta in southeastern New Mexico would be an increase of less than 11,000 acre-ft/year. This increase includes overflow of 300 acre-ft from the present Pecos River channel, seepage losses of 3,600 acre-ft from the river bed and tributary inflow of 7,100 acre-ft. The potential effects of drains at the north end of the study area would be additional water of about 6,100 acre-ft within the first few years. In order to drain this much water, the drains would have to be dredged to a lower depth 6 to 8 mi to the south. Impoundment in Brantley Reservoir will cause increases in groundwater storage. The quantity of increased storage will depend on average reservoir pool levels. Major Johnson Springs probably will cease to flow at the conservation-pool level, and southward groundwater leakage from the Major Johnson Springs aquifer could increase. Large quantities of water may move in and out of storage in the Major Johnson Springs aquifer as the Brantley Reservoir pool changes between minimum pool and conservation pool levels. A ground--and surface-water monitoring network is needed to determine changes in groundwater storage caused by Brantley Reservoir. Water levels in selected wells need to be measured periodically during operation of the reservoir. Additional streamflow-gaging stations need to be established and surface-water samples analyzed to determine changes caused by a drainage system and Brantley Reservoir. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri884054","usgsCitation":"Crouch, T.M., and Welder, G.E., 1988, Potential hydrologic effects of a drainage system in McMillan delta and water impoundment in Brantley Reservoir, Eddy County, New Mexico: U.S. Geological Survey Water-Resources Investigations Report 88-4054, v, 44 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri884054.","productDescription":"v, 44 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":124222,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1988/4054/report-thumb.jpg"},{"id":55573,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1988/4054/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b23e4b07f02db6ae083","contributors":{"authors":[{"text":"Crouch, T. M.","contributorId":106163,"corporation":false,"usgs":true,"family":"Crouch","given":"T.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":196853,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Welder, G. E.","contributorId":100814,"corporation":false,"usgs":true,"family":"Welder","given":"G.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":196852,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":26645,"text":"wri884160 - 1988 - Sediment inflow, outflow and deposition for Lakes Marion and Moultrie, South Carolina, October 1983 - March 1985","interactions":[],"lastModifiedDate":"2021-12-09T21:18:44.261153","indexId":"wri884160","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"88-4160","title":"Sediment inflow, outflow and deposition for Lakes Marion and Moultrie, South Carolina, October 1983 - March 1985","docAbstract":"In 1941 a Coastal Plain reach of the Santee River was impounded to form Lake Marion and diverted into a diked-off part of the Cooper River basin to form Lake Moultrie. Rates of sediment inflow and outflow of the lakes were determined by the U.S. Geological Survey for the periods July 1966 - June 1968 and October 1983 - March 1985. Total sediment discharge was estimated for two inflow stations and continuous streamflow monitors and automatic suspended-sediment samplers were used for computation of suspended-sediment discharge. Bedload discharge was computed by the modified Einstein procedure. Suspended-sediment discharge was monitored at three outflow stations, with the suspended-sediment concentration measured on a weekly basis. During the 1983-1985 study, mean annual suspended-sediment inflow to Lakes Marion and Moultrie was estimated to be 722,000 tons, and the outflow was estimated at 175,000 tons, for a trap efficiency of 76% and a deposition rate of about 547,000 tons/year. This is about 33% less than the deposition rate determined during the 1966-68 study. The deposition rate for suspended and bedload sediment during the 1983 - 1985 study was about 650,000 tons/year. (USGS)","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri884160","usgsCitation":"Cooney, T., 1988, Sediment inflow, outflow and deposition for Lakes Marion and Moultrie, South Carolina, October 1983 - March 1985: U.S. Geological Survey Water-Resources Investigations Report 88-4160, iv, 49 p., https://doi.org/10.3133/wri884160.","productDescription":"iv, 49 p.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":158389,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1988/4160/report-thumb.jpg"},{"id":55523,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1988/4160/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":392697,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_47067.htm"}],"country":"United States","state":"South Carolina","otherGeospatial":"Lake Marion, Lake Moultrie","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -80.6341552734375,\n              33.14675022877648\n            ],\n            [\n              -79.80743408203124,\n              33.14675022877648\n            ],\n            [\n              -79.80743408203124,\n              33.74489664315623\n            ],\n            [\n              -80.6341552734375,\n              33.74489664315623\n            ],\n            [\n              -80.6341552734375,\n              33.14675022877648\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fc01a","contributors":{"authors":[{"text":"Cooney, T.W.","contributorId":25194,"corporation":false,"usgs":true,"family":"Cooney","given":"T.W.","email":"","affiliations":[],"preferred":false,"id":196762,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":26569,"text":"wri874209 - 1988 - Regionalization of peak discharges for streams in Kentucky","interactions":[],"lastModifiedDate":"2015-09-24T15:27:46","indexId":"wri874209","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4209","title":"Regionalization of peak discharges for streams in Kentucky","docAbstract":"<p>Multiple regression analysis was used to delineate hydrologically distinct regions in Kentucky, and to develop regression models for estimating peak discharge for unregulated streams in these regions. The regression models provide estimates of flood quantiles with associated average recurrence intervals of 2, 5, 10, 25, 50, and 100 years. The data base used in the analysis included annual peak discharge records (through water year 1985) at 266 continuous- and partial-record gaging stations in, and adjacent to, Kentucky. Selected drainage basin characteristics upstream of each gaging station were used to develop the regression equations. Flood quantiles at the gaged stations were estimated on the basis of log-Pearson Type III distribution and the methodology recommended by the U.S. Water Resources Council. Seven hydrologic regions were delineated in Kentucky on the basis of analysis of residuals from statewide and regional regression models. Regression models for estimating flood quantiles in the hydrologic regions are based on measurements of contributing drainage area, main channel slope, basin shape index, and main channel sinuosity. The regression coefficients indicated an increase in flood discharge with increasing drainage area and channel slope, and a decrease in discharge with increasing channel sinuosity and basin elongation. Accuracy of the discharge estimates from the regression models as measured by the standard error of the estimate ranged from 21 to 52%. The procedures for estimating flood quantiles vary depending on whether the estimate is for an ungaged site, an ungaged site near a gaged site on the same stream, or a gaged site. Also considered is whether the drainage area crosses hydrologic region boundaries or state lines. The methods apply only to natural flow streams drainage areas &lt; 1 ,000 sq mi.&nbsp;</p>","largerWorkType":{"id":18,"text":"Report"},"largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri874209","usgsCitation":"Choquette, A.F., 1988, Regionalization of peak discharges for streams in Kentucky: U.S. Geological Survey Water-Resources Investigations Report 87-4209, Report: viii, 105 p.; Plate: 30 x 19 inches, https://doi.org/10.3133/wri874209.","productDescription":"Report: viii, 105 p.; Plate: 30 x 19 inches","numberOfPages":"114","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":55433,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4209/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":308566,"rank":401,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4209/report.pdf","text":"Report","size":"25.6 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,{"id":26544,"text":"wri874218 - 1988 - Geohydrology of the Furnace Creek basin and vicinity, Berks, Lancaster, and Lebanon counties, Pennsylvania","interactions":[],"lastModifiedDate":"2017-07-06T09:21:13","indexId":"wri874218","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4218","title":"Geohydrology of the Furnace Creek basin and vicinity, Berks, Lancaster, and Lebanon counties, Pennsylvania","docAbstract":"The Furnace Creek basin is an area of 8.95 square miles, about three- fourths of which is underlain by metamorphic rocks of low permeability. Reported yields for 14 wells in these rocks range from 1 to 60 gal/min (gallons per minute), with a median of 7.5 gal/min.\r\n\r\n      The northern part of the study area consists of highly permeable carbonate rocks. Nondomestic wells in these rocks typically yield from 200 to 300 gal/min and one well yields 1,200 gal/min.\r\n\r\n      Ground-water discharge from a 4.18-square-mile drainage area underlain by Precambrian granitic and hornblende gneiss averaged 868,000 gallons per day per square mile from October 1983 through September 1985. Thus, as much as 3,630,000 gallons per day could be pumped from wells in this area on a sustained basis. However, pumping this amount would have major adverse effects on streamflow.\r\n\r\n      A water-budget analysis for March 1984 to February 1985 showed that precipitation was 52.16 inches, streamflow was 26.38 inches, evapotranspiration was 29.29 inches, ground-water storage decreased by 5.94 inches and diversions made by Womelsdorf-Robesonia Joint Authority for water supply totaled 2.43 inches. Precipitation during this period was above normal.\r\n\r\n      Four of 18 wells sampled for water quality had iron, manganese, or nitrate concentrations above the U.S. Environmental Protection Agency's recommended limits. The crystalline rocks in the study area yield soft to moderately hard water that is generally acidic.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri874218","usgsCitation":"Cecil, L., 1988, Geohydrology of the Furnace Creek basin and vicinity, Berks, Lancaster, and Lebanon counties, Pennsylvania: U.S. Geological Survey Water-Resources Investigations Report 87-4218, v, 38 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri874218.","productDescription":"v, 38 p. :ill., maps ;28 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":126327,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4218/report-thumb.jpg"},{"id":55409,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4218/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55410,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4218/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a8993","contributors":{"authors":[{"text":"Cecil, L.D.","contributorId":62616,"corporation":false,"usgs":true,"family":"Cecil","given":"L.D.","email":"","affiliations":[],"preferred":false,"id":196582,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":26508,"text":"wri884066 - 1988 - Freshwater supply potential of the Atlantic Intracoastal Waterway near Myrtle Beach, South Carolina","interactions":[],"lastModifiedDate":"2017-01-25T08:54:32","indexId":"wri884066","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"88-4066","title":"Freshwater supply potential of the Atlantic Intracoastal Waterway near Myrtle Beach, South Carolina","docAbstract":"A study was conducted to determine the low-flow frequency of freshwater flow in the Atlantic Intracoastal Waterway (AICW) near Myrtle Beach, South Carolina and to determine the effects of proposed freshwater withdrawals of 45 cu ft/sec at the location of the saltwater-freshwater interface. Discharges simulated in the AICW for 1982-86 using BRANCH one-dimensional flow model were used to establish a relation of 7-day average flows in the AICW to summed 7-day average flows of four tributary streams. This relation was used with the tributary records for 1954-86 climatic years to generate 7-day minimum flows of the AICW, which were then used to develop a low-flow frequency relation. The relation indicated that the 7-day, 10-year flow of the Atlantic Intracoastal Waterway is 192 ct ft/s. A relation of the mile position of the saltwater-freshwater interface to recorded specific conductances at Vereen 's Marina was established. The 1982-85 period of record of specific conductance was used to simulate interface positions which were then used to establish a relation of 7-day average interface position to 7-day average discharge of the AICW. This relation indicated that the 7-day average interface position would be at mile 355.5 for the 7Q10 and at mile 356.2 if 45 cu ft were withdrawn during the 7Q10. The analysis indicates that the AICW can provide a reliable supply of freshwater at the proposed withdrawal location at mi 363.3 in the vicinity of Myrtle Beach, even during the 7Q10 low-flow conditions. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri884066","usgsCitation":"Carswell, W., Sanders, C., and Johnson, D., 1988, Freshwater supply potential of the Atlantic Intracoastal Waterway near Myrtle Beach, South Carolina: U.S. Geological Survey Water-Resources Investigations Report 88-4066, v, 45 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri884066.","productDescription":"v, 45 p. :ill., maps ;28 cm.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":55343,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55344,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55351,"rank":421,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-22.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55345,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55346,"rank":416,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-17.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55352,"rank":422,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-23.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55353,"rank":423,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-24.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55347,"rank":417,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-18.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55348,"rank":418,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-19.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55349,"rank":419,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-20.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55350,"rank":420,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-21.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55354,"rank":424,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-25.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55355,"rank":425,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-26.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55356,"rank":426,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-27.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55357,"rank":427,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-28.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55358,"rank":428,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-29.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55359,"rank":429,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-30.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55360,"rank":430,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-31.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55361,"rank":431,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-32.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55362,"rank":432,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-33.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55363,"rank":433,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-34.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55364,"rank":434,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-35.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55365,"rank":435,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-36.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55366,"rank":436,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-37.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55367,"rank":437,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-38.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55368,"rank":438,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-39.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55369,"rank":439,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-40.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55372,"rank":442,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-43.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55373,"rank":443,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-44.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55374,"rank":444,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-45.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55375,"rank":445,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-46.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55376,"rank":446,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-47.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":55377,"rank":447,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1988/4066/plate-48.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id"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States","state":"South Carolina","city":"Myrtle Beach","otherGeospatial":"Atlantic Intracoastal Waterway","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -79.25537109375,\n              33.39934533042092\n            ],\n            [\n              -79.25537109375,\n              34.05265942137599\n            ],\n            [\n              -78.54537963867188,\n              34.05265942137599\n            ],\n            [\n              -78.54537963867188,\n              33.39934533042092\n            ],\n            [\n              -79.25537109375,\n              33.39934533042092\n            ]\n          ]\n        ]\n      }\n    }\n  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J.","contributorId":71213,"corporation":false,"usgs":true,"family":"Carswell","given":"W. J.","affiliations":[],"preferred":false,"id":196515,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sanders, C.L. Jr.","contributorId":57496,"corporation":false,"usgs":true,"family":"Sanders","given":"C.L.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":196513,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Johnson, D.M.","contributorId":58266,"corporation":false,"usgs":true,"family":"Johnson","given":"D.M.","email":"","affiliations":[],"preferred":false,"id":196514,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":27127,"text":"wri854331 - 1988 - Low-flow routing in the Lehigh and Delaware Rivers, Pennsylvania","interactions":[],"lastModifiedDate":"2017-07-05T11:25:17","indexId":"wri854331","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"85-4331","title":"Low-flow routing in the Lehigh and Delaware Rivers, Pennsylvania","docAbstract":"Flow-routing studies were made to evaluate the response of the Lehigh and Delaware Rivers to low-flow augmentative releases from two reservoirs --Francis E. Walter Reservoir and Beltzville Lake--in the Lehigh River basin. Digital routing models that use diffusion-analogy methods to convolute flows with system-response functions were developed to simulate daily flows at selected sites. Model errors, for five sites and for periods of 1 year or more, were mostly between 3 and 12 percent in terms of absolute errors in daily flows and were mostly within 4 percent for flow volumes.\r\n\r\n      The developed models were satisfactory for predicting hydrographic response at eight sites in the reach from White Haven, Pennsylvania to Trenton, New Jersey. However, abrupt changes in the flow rate of the Lehigh River at the Bethlehem and the Glendon gaging stations could not be adequately replicated with the model. The model tends to underestimate peaks by as much as 30 percent and to overestimate some low flows of short duration by as much as 20 percent. This occurs primarily because inflows from ungaged areas could not be reliably modeled throughout their ranges by use of flow records for gaged streams. The model will underestimate long-duration low flows at the Glendon site for periods when underflows at the gaging stations on Little Lehigh and Monocacy Creeks are significant.\r\n\r\n      The models were used to route hypothetical releases from Francis E. Walter Reservoir during a low-flow period. The model for the Lehigh River indicated that an added release of 50 ft3/s (cubic feet per second) over a 64-day period during the severe drought in the summer of 1965 would have increased minimum flows for this period at Bethlehem and Glendon by approximately the same amount. A hypothetical release of 200 ft3/s for the period July 20-22, 1965, which is about eight times the actual release in this period, would have been attenuated by about 25 percent when it reached the Bethlehem gage. The synthesized hydrograph for the Bethlehem gage showed such a release would have passed their by July 27. Unresolvable timing errors in the models created an unrealistic hydrographic response for this release at the Trenton gage; but, such a release probably would have passed Trenton by July 29.\r\n\r\n      In order to time the movement of a release wave more accurately than could be done with the developed model, travel times for the wave of an augmentative low-flow release were obtained by field observations and comparisons of gage-height records. The observed leading edge of an abrupt release of 153 ft3/s from Francis E. Walter Reservoir, which ended a 2-day release at a rate of 48 ft3/s, arrived at the gage below the reservoir in 0.5 hour, at White Haven in 3.7 hours, at the mouth of Pohopoco Creek in about 23.1 hours, at Walnutport in 27 hours, at Bethlehem in 39 hours, and at Glendon in 42 hours.\r\n\r\n      This release could not be detected in the record for the Trenton gage. Travel time for an augmentative release in the Lehigh River is dependent upon the pre-release discharge, the relative magnitude of the release, and antecedent rainfall. Relationships are provided for estimating the time of arrival at Walnutport, Bethlehem, and Glendon of the leading edge of waves generated by augmentative releases of 75 to 600 ft3/s. Stage observations on Pohopoco Creek indicated a 2.1-hour travel time between Beltzville Lake and the Lehigh River for the elading edge of a wave produced by a typical augmentative release from this reservoir.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri854331","usgsCitation":"Flippo, H., 1988, Low-flow routing in the Lehigh and Delaware Rivers, Pennsylvania: U.S. Geological Survey Water-Resources Investigations Report 85-4331, iv, 30 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri854331.","productDescription":"iv, 30 p. :ill., maps ;28 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":124730,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1985/4331/report-thumb.jpg"},{"id":55988,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1985/4331/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db6487c3","contributors":{"authors":[{"text":"Flippo, H.N. Jr.","contributorId":96301,"corporation":false,"usgs":true,"family":"Flippo","given":"H.N.","suffix":"Jr.","affiliations":[],"preferred":false,"id":197599,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":27757,"text":"wri884122 - 1988 - Review of mechanisms, methods, and theory for determining recharge to shallow aquifers in North Dakota","interactions":[],"lastModifiedDate":"2018-03-08T13:08:25","indexId":"wri884122","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"88-4122","title":"Review of mechanisms, methods, and theory for determining recharge to shallow aquifers in North Dakota","docAbstract":"<p>Effective management of ground-water resources requires knowledge of all components of the water budget for the aquifer of interest. Efforts to simulate ground-water flow prior to development and the effects of proposed pumping in several of North Dakota's shallow glacial aquifers have been hindered by the lack of reliable estimates of ground-water recharge. This study was done to (1) review the methods that have been used to measure recharge, (2) review the theory of unsaturated flow and the methods for characterizing the physical properties of unsaturated media, (3) consider the relative merits of a rigorous data-intensive approach versus an estimation approach to the study of recharge, and (4) review past and current agronomic research in North Dakota for applicability of the research and the data generated to the study of recharge.</p><p>Direct, quantitative techniques for evaluating recharge are rarely applied. The theory for computing fluxes in unsaturated media is well established and numerous physics-based models that effectively implement the theory are available, but the data required for the models generally are lacking. Many parametric approaches have been developed to avoid the large data requirements of the physics-based approaches for analyzing flow in the unsaturated zone. However, the parametric approaches normally include fitting coefficients that must be calibrated for every study site, thereby detracting from the general utility of the parametric approach. </p><p>The functional relation of matric potential to moisture content is required for physics-based soil-water models, whether analytic or numeric. Laboratory methods to determine these relations are tedious, costly, and may not give results representative of the soils as they occur in the field. Many models have been proposed to estimate the moisture-characteristic curve and hydraulic-conductivity function from basic soil properties, but none yield results that are universally satisfactory. In situ methods, because they require minimal disturbance of the soil profile and may be used repeatedly on the same soil mass, have become the preferred means for acquiring physical data, especially hydraulic conductivity. Hydro logic investigations, except for recent studies of hazardous-waste disposal sites, rarely have included physical characterizations of unsaturated media. </p><p>Any of four phenomena could hinder attempts to simulate unsaturated flow in settings typical of North Dakota; variability of soil properties, hysteresis, frozen ground, and macropore development. The spatial and temporal variability of soil properties probably is the greatest complicating phenomenon and must be dealt with by detailed characterization of the properties. Hysteresis can detract from the accuracy of flow calculations&nbsp;for some soils under certain conditions but, for the present, our scant knowledge of soil physical properties is a greater hindrance to reliable soi1-water mode 1 ing than is the hysteresis phenomenon. A1 though seasona1ly frozen ground undoubtedly affects hydrologic processes in North Dakota, much more research is needed before meaningful quantitative treatment is possible. Finally, macropores can influence soil-water movement significantly, but macropore development may not be common on the intensively farmed, coarse-textured soils that typically overlie North Dakota's glacial aquifers. Lysimetry currently is the only reliable means of analyzing macropore flow.</p><p>The soil-related research that has been conducted in North Dakota to date (1983) provides little of the type of information required to estimate ground-water recharge. Useful data could be developed by systematically evaluating the hydraulic characteristics of the prominent soil types overlying North Dakota's shallow glacial aquifers. These data would be required to enable use of a physics-based approach to estimating recharge. The size of the aquifer under study, its economic value, and the resources available for data collection should be considered when choosing between parametric or physics-based methods. </p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri884122","usgsCitation":"Horak, W., 1988, Review of mechanisms, methods, and theory for determining recharge to shallow aquifers in North Dakota: U.S. Geological Survey Water-Resources Investigations Report 88-4122, iv, 54 p., https://doi.org/10.3133/wri884122.","productDescription":"iv, 54 p.","costCenters":[{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":157960,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1988/4122/report-thumb.jpg"},{"id":56604,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1988/4122/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a80f4","contributors":{"authors":[{"text":"Horak, W.F.","contributorId":82326,"corporation":false,"usgs":true,"family":"Horak","given":"W.F.","email":"","affiliations":[],"preferred":false,"id":198648,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":29122,"text":"wri874273 - 1988 - Effects of agricultural irrigation on water resources in the St. Joseph River basin, Indiana, and implications for aquifer yield","interactions":[],"lastModifiedDate":"2016-06-21T13:56:09","indexId":"wri874273","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4273","title":"Effects of agricultural irrigation on water resources in the St. Joseph River basin, Indiana, and implications for aquifer yield","docAbstract":"<p>During the past decade, the acreage of irrigated agricultural land in Indiana has tripled, causing public concern about competition for water and resulting in several State laws for regulating water withdrawals. The St. Joseph River basin represents less than one-tenth of the area of the State, but it contains one-third of the State 's irrigated land. Irrigated land in the basin is composed of permeable soils that are underlain by productive glacial aquifers. A computer model was used to analyze the effects of maximum irrigation withdrawals on aquifer drawdown and streamflow in a 16.5 sq mi area of intensive irrigation. Simulation of maximum pumping resulted in predicted aquifer drawdowns of one-fourth of the total available drawdown. Flow in a nearby stream was decreased by 40%. Areas of most intensive irrigation in the basin also are areas that have productive aquifers and well-sustained streamflows. Aquifer yield is based on the concept of capture - the volume of increased recharge to the aquifer or decreased discharge from the aquifer that results from pumping. The high rates of capture for aquifers in the basin supply ample water for present (1982) irrigation and for substantial future development. (USGS)</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Indianapolis, IN","doi":"10.3133/wri874273","usgsCitation":"Peters, J.G., and Renn, D., 1988, Effects of agricultural irrigation on water resources in the St. Joseph River basin, Indiana, and implications for aquifer yield: U.S. Geological Survey Water-Resources Investigations Report 87-4273, vii, 35 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri874273.","productDescription":"vii, 35 p. :ill., maps ;28 cm.","startPage":"1","endPage":"35","numberOfPages":"42","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":122904,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4273/report-thumb.jpg"},{"id":57992,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4273/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Indiana","county":"Elkhart, Kosciusko, Lagrange, Noble, Saint Joseph, Steuben, Berrien, Branch, Calhoun, cass, Hillsdale, Kalamazoo, Saint Joseph, Van Buren","otherGeospatial":"Saint Joseph River Basin","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-85.7663,42.4196],[-85.5421,42.4195],[-85.5328,42.4194],[-85.4172,42.4199],[-85.3091,42.4185],[-85.2979,42.4188],[-85.0736,42.4211],[-85.0667,42.4215],[-84.9561,42.4221],[-84.8375,42.4215],[-84.83,42.421],[-84.7207,42.4209],[-84.7195,42.2464],[-84.7144,42.1586],[-84.7116,42.0709],[-84.5948,42.0715],[-84.3666,42.0734],[-84.3623,41.7082],[-84.3989,41.7074],[-84.4979,41.705],[-84.6319,41.7018],[-84.6756,41.7007],[-84.8067,41.6958],[-84.8064,41.5598],[-84.8063,41.5303],[-84.8554,41.53],[-84.969,41.5287],[-85.0819,41.5282],[-85.1947,41.5276],[-85.1939,41.4395],[-85.1943,41.3519],[-85.1935,41.2643],[-85.309,41.265],[-85.3096,41.265],[-85.4245,41.2655],[-85.5387,41.2664],[-85.5384,41.295],[-85.6527,41.2949],[-85.6518,41.2668],[-85.6522,41.1787],[-85.6876,41.179],[-85.6856,41.0896],[-85.6849,41.0465],[-85.9457,41.0424],[-86.017,41.0414],[-86.0179,41.0863],[-86.0758,41.0851],[-86.0777,41.1736],[-86.0539,41.1735],[-86.0574,41.3033],[-86.059,41.4336],[-86.059,41.4367],[-86.0594,41.4644],[-86.0593,41.474],[-86.0593,41.479],[-86.0789,41.479],[-86.0979,41.4791],[-86.1181,41.4792],[-86.1273,41.4792],[-86.1421,41.4792],[-86.1562,41.4793],[-86.234,41.479],[-86.3063,41.4787],[-86.3302,41.4778],[-86.3492,41.4778],[-86.378,41.4774],[-86.4356,41.4765],[-86.4559,41.4765],[-86.4645,41.4765],[-86.4669,41.4765],[-86.4669,41.4616],[-86.4669,41.4339],[-86.5245,41.4339],[-86.5245,41.5201],[-86.5012,41.5206],[-86.5,41.5287],[-86.4982,41.531],[-86.4982,41.5669],[-86.4865,41.5769],[-86.4871,41.649],[-86.5068,41.6499],[-86.5264,41.6499],[-86.5264,41.6572],[-86.5258,41.6731],[-86.5252,41.7085],[-86.524,41.7603],[-86.5284,41.7603],[-86.6391,41.7606],[-86.7387,41.7608],[-86.7677,41.7608],[-86.7814,41.7609],[-86.8262,41.7609],[-86.8182,41.7641],[-86.7758,41.7864],[-86.7482,41.8037],[-86.7285,41.8147],[-86.7064,41.8265],[-86.6886,41.8402],[-86.6418,41.8761],[-86.6122,41.9006],[-86.6092,41.9029],[-86.5956,41.9202],[-86.5833,41.9374],[-86.5698,41.9647],[-86.5667,41.9711],[-86.5636,41.9829],[-86.563,41.9842],[-86.5402,42.0274],[-86.5136,42.0701],[-86.5112,42.0737],[-86.5025,42.0864],[-86.4895,42.1046],[-86.4883,42.1137],[-86.474,42.1287],[-86.4555,42.1441],[-86.4418,42.1591],[-86.4381,42.1632],[-86.4158,42.1836],[-86.3904,42.2127],[-86.3637,42.2453],[-86.3625,42.2467],[-86.3544,42.2612],[-86.3401,42.2807],[-86.3388,42.2821],[-86.327,42.3034],[-86.3133,42.332],[-86.3039,42.3507],[-86.2877,42.3906],[-86.2814,42.4065],[-86.2745,42.4201],[-86.2248,42.4191],[-85.995,42.4193],[-85.8975,42.4185],[-85.7663,42.4196]]]},\"properties\":{\"name\":\"Elkhart\",\"state\":\"IN\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a49e4b07f02db623d41","contributors":{"authors":[{"text":"Peters, J. G.","contributorId":56216,"corporation":false,"usgs":true,"family":"Peters","given":"J.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":200982,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Renn, D.E.","contributorId":36941,"corporation":false,"usgs":true,"family":"Renn","given":"D.E.","email":"","affiliations":[],"preferred":false,"id":200981,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":31092,"text":"ofr8879 - 1988 - Estimating soil matric potential in Owens Valley, California","interactions":[{"subject":{"id":31092,"text":"ofr8879 - 1988 - Estimating soil matric potential in Owens Valley, California","indexId":"ofr8879","publicationYear":"1988","noYear":false,"title":"Estimating soil matric potential in Owens Valley, California"},"predicate":"SUPERSEDED_BY","object":{"id":31068,"text":"wsp2370C - 1989 - Estimating soil matric potential in Owens Valley, California","indexId":"wsp2370C","publicationYear":"1989","noYear":false,"chapter":"C","title":"Estimating soil matric potential in Owens Valley, California"},"id":1}],"supersededBy":{"id":31068,"text":"wsp2370C - 1989 - Estimating soil matric potential in Owens Valley, California","indexId":"wsp2370C","publicationYear":"1989","noYear":false,"title":"Estimating soil matric potential in Owens Valley, California"},"lastModifiedDate":"2019-11-26T14:06:47","indexId":"ofr8879","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","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":"88-79","title":"Estimating soil matric potential in Owens Valley, California","docAbstract":"Much of the floor of the Owens Valley, California, is covered with alkaline scrub and alkaline meadow plant communities, whose existence is dependent partly on precipitation and partly on water infiltrated into the rooting zone from the shallow water table. The extent to which these plant communities are capable of adapting to and surviving fluctuations in the water table depends on physiological adaptations of the plants and on the water content, matric potential characteristics of the soils. Two methods were used to estimate soil matric potential in test sites in Owens Valley. The first was the filter-paper method, which uses water content of filter papers equilibrated to water content of soil samples taken with a hand auger. The other method of estimating soil matric potential was a modeling approach based on data from this and previous investigations. These data indicate that the base 10 logarithm of soil matric potential is a linear function of gravimetric soil water content for a particular soil. Estimates of soil water characteristic curves were made at two sites by averaging the gravimetric soil water content and soil matric potential values from multiple samples at 0.1 m depths derived by using the hand auger and filter paper method and entering these values in the soil water model. The characteristic curves then were used to estimate soil matric potential from estimates of volumetric soil water content derived from neutron-probe readings. Evaluation of the modeling technique at two study sites indicated that estimates of soil matric potential within 0.5 pF units of the soil matric potential value derived by using the filter paper method could be obtained 90 to 95% of the time in soils where water content was less than field capacity. The greatest errors occurred at depths where there was a distinct transition between soils of different textures. (Lantz-PTT)","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr8879","usgsCitation":"Sorenson, S.K., Miller, R., Welch, M., Groeneveld, D., and Branson, F., 1988, Estimating soil matric potential in Owens Valley, California: U.S. Geological Survey Open-File Report 88-79, 42 p., https://doi.org/10.3133/ofr8879.","productDescription":"42 p.","costCenters":[],"links":[{"id":160889,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1988/0079/report-thumb.jpg"},{"id":369676,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1988/0079/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"California","otherGeospatial":"Owens Valley","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -119.3280029296875,\n              36.54053616262899\n            ],\n            [\n              -117.48229980468749,\n              36.54053616262899\n            ],\n            [\n              -117.48229980468749,\n              38.039438891821746\n            ],\n            [\n              -119.3280029296875,\n              38.039438891821746\n            ],\n            [\n              -119.3280029296875,\n              36.54053616262899\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48e2e4b07f02db54e1c5","contributors":{"authors":[{"text":"Sorenson, Stephen K.","contributorId":90314,"corporation":false,"usgs":true,"family":"Sorenson","given":"Stephen","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":204945,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, R.F.","contributorId":83882,"corporation":false,"usgs":true,"family":"Miller","given":"R.F.","email":"","affiliations":[],"preferred":false,"id":204944,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Welch, M.R.","contributorId":14464,"corporation":false,"usgs":true,"family":"Welch","given":"M.R.","email":"","affiliations":[],"preferred":false,"id":204941,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Groeneveld, D.P.","contributorId":77161,"corporation":false,"usgs":true,"family":"Groeneveld","given":"D.P.","email":"","affiliations":[],"preferred":false,"id":204943,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Branson, F.A.","contributorId":31430,"corporation":false,"usgs":true,"family":"Branson","given":"F.A.","affiliations":[],"preferred":false,"id":204942,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":29114,"text":"wri844092 - 1988 - Statistical summary of the chemical quality of surface water in the Powder River coal basin, the Hanna coal field, and the Green River coal region, Wyoming","interactions":[],"lastModifiedDate":"2012-02-02T00:08:53","indexId":"wri844092","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"84-4092","title":"Statistical summary of the chemical quality of surface water in the Powder River coal basin, the Hanna coal field, and the Green River coal region, Wyoming","docAbstract":"A summary of the chemical quality of surface water in the three principal coal-producing areas of Wyoming was intensified by the U.S. Geologic Survey during 1975-81, in response to interest spurred by a dramatic increase in surface mining of the areas. This statistical summary consists of descriptive statistics and regression analyses of data from 72 stations on streams in the Powder River coal basin, the Hanna coal field, and the Green River coal region of Wyoming. The mean dissolved-solids concentrations in streams ranged from 15 to 4,800 mg/L. Samples collected near mountainous areas or in the upstream reaches of perennial streams in the plains had the smallest concentrations of dissolved solids, and the predominant ions were calcium and bicarbonate. Samples from ephemeral, intermittent, and the downstream reaches of perennial streams in the plains contained relatively large dissolved-solids concentrations, and the predominant ions usually were sodium and sulfate. Regression models showed that the concentrations of dissolved solids, calcium, magnesium, sodium, alkalinity, sulfate, and chloride correlated well with specific-conductance values in many of the streams. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri844092","usgsCitation":"Peterson, D.A., 1988, Statistical summary of the chemical quality of surface water in the Powder River coal basin, the Hanna coal field, and the Green River coal region, Wyoming: U.S. Geological Survey Water-Resources Investigations Report 84-4092, iv, 109 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri844092.","productDescription":"iv, 109 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":159644,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1984/4092/report-thumb.jpg"},{"id":57982,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1984/4092/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":57983,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1984/4092/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4885e4b07f02db518e97","contributors":{"authors":[{"text":"Peterson, D. A.","contributorId":6453,"corporation":false,"usgs":true,"family":"Peterson","given":"D.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":200969,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":26414,"text":"wri884012 - 1988 - Computer-program documentation of an interactive-accounting model to simulate streamflow, water quality, and water-supply operations in a river basin","interactions":[],"lastModifiedDate":"2012-02-02T00:08:33","indexId":"wri884012","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"88-4012","title":"Computer-program documentation of an interactive-accounting model to simulate streamflow, water quality, and water-supply operations in a river basin","docAbstract":"This report describes an interactive-accounting model used to simulate streamflow, chemical-constituent concentrations and loads, and water-supply operations in a river basin. The model uses regression equations to compute flow from incremental (internode) drainage areas. Conservative chemical constituents (typically dissolved solids) also are computed from regression equations. Both flow and water quality loads are accumulated downstream. Optionally, the model simulates the water use and the simplified groundwater systems of a basin. Water users include agricultural, municipal, industrial, and in-stream users , and reservoir operators. Water users list their potential water sources, including direct diversions, groundwater pumpage, interbasin imports, or reservoir releases, in the order in which they will be used. Direct diversions conform to basinwide water law priorities. The model is interactive, and although the input data exist in files, the user can modify them interactively. A major feature of the model is its color-graphic-output options. This report includes a description of the model, organizational charts of subroutines, and examples of the graphics. Detailed format instructions for the input data, example files of input data, definitions of program variables, and listing of the FORTRAN source code are Attachments to the report. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri884012","usgsCitation":"Burns, A., 1988, Computer-program documentation of an interactive-accounting model to simulate streamflow, water quality, and water-supply operations in a river basin: U.S. Geological Survey Water-Resources Investigations Report 88-4012, iv, 241 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri884012.","productDescription":"iv, 241 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":123236,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1988/4012/report-thumb.jpg"},{"id":55209,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1988/4012/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a6324","contributors":{"authors":[{"text":"Burns, A.W.","contributorId":65498,"corporation":false,"usgs":true,"family":"Burns","given":"A.W.","email":"","affiliations":[],"preferred":false,"id":196345,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":28999,"text":"wri884009 - 1988 - Fracture characterization and fracture-permeability estimation at the underground research laboratory in southeastern Manitoba, Canada","interactions":[],"lastModifiedDate":"2012-02-02T00:08:52","indexId":"wri884009","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"88-4009","title":"Fracture characterization and fracture-permeability estimation at the underground research laboratory in southeastern Manitoba, Canada","docAbstract":"Various conventional geophysical well logs were obtained in conjunction with acoustic tube-wave amplitude and experimental heat-pulse flowmeter measurements in two deep boreholes in granitic rocks on the Canadian shield in southeastern Manitoba. The objective of this study is the development of measurement techniques and data processing methods for characterization of rock volumes that might be suitable for hosting a nuclear waste repository. One borehole, WRA1, intersected several major fracture zones, and was suitable for testing quantitative permeability estimation methods. The other borehole, URL13, appeared to intersect almost no permeable fractures; it was suitable for testing methods for the characterization of rocks of very small permeability and uniform thermo-mechanical properties in a potential repository horizon. Epithermal neutron , acoustic transit time, and single-point resistance logs provided useful, qualitative indications of fractures in the extensively fractured borehole, WRA1. A single-point log indicates both weathering and the degree of opening of a fracture-borehole intersection. All logs indicate the large intervals of mechanically and geochemically uniform, unfractured granite below depths of 300 m in the relatively unfractured borehole, URL13. Some indications of minor fracturing were identified in that borehole, with one possible fracture at a depth of about 914 m, producing a major acoustic waveform anomaly. Comparison of acoustic tube-wave attenuation with models of tube-wave attenuation in infinite fractures of given aperture provide permeability estimates ranging from equivalent single-fractured apertures of less than 0.01 mm to apertures of &gt; 0.5 mm. One possible fracture anomaly in borehole URL13 at a depth of about 914 m corresponds with a thin mafic dike on the core where unusually large acoustic contrast may have produced the observed waveform anomaly. No indications of naturally occurring flow existed in borehole URL13; however, flowmeter measurements indicated flow at &lt; 0.05 L/min from the upper fracture zones in borehole WRA1 to deeper fractures at depths below 800 m. (Author 's abstract)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri884009","usgsCitation":"Paillet, F.L., 1988, Fracture characterization and fracture-permeability estimation at the underground research laboratory in southeastern Manitoba, Canada: U.S. Geological Survey Water-Resources Investigations Report 88-4009, 42 p. :ill. ;28 cm., https://doi.org/10.3133/wri884009.","productDescription":"42 p. :ill. ;28 cm.","costCenters":[],"links":[{"id":124154,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1988/4009/report-thumb.jpg"},{"id":57866,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1988/4009/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a9025","contributors":{"authors":[{"text":"Paillet, Frederick L.","contributorId":63820,"corporation":false,"usgs":true,"family":"Paillet","given":"Frederick","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":200762,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":27164,"text":"wri874260 - 1988 - Hydrogeology and flow of water in a sand and gravel aquifer contaminated by wood-preserving compounds, Pensacola, Florida","interactions":[],"lastModifiedDate":"2012-02-02T00:08:26","indexId":"wri874260","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"87-4260","title":"Hydrogeology and flow of water in a sand and gravel aquifer contaminated by wood-preserving compounds, Pensacola, Florida","docAbstract":"The sand and gravel aquifer in southern Escambia County, Florida , is a typical surficial aquifer composed of quartz sands and gravels interbedded locally with silts and clays. Problems of groundwater contamination from leaking surface impoundments are common in surficial aquifers and are a subject of increasing concern and attention. A potentially widespread contamination problem involves organic chemicals from wood-preserving processes. Because creosote is the most extensively used industrial preservative in the United States, an abandoned wood-treatment plant near Pensacola was chosen for investigation. This report describes the hydrogeology and groundwater flow system of the sand and gravel aquifer near the plant. A three-dimensional simulation of groundwater flow in the aquifer was evaluated under steady-state conditions. The model was calibrated on the basis of observed water levels from January 1986. Calibration criteria included reproducing all water levels within the accuracy of the data (one-half contour interval in most cases). Sensitivity analysis showed that the simulations were most sensitive to recharge and vertical leakance of the confining units between layers 1 and 2, and relatively insensitive to changes in hydraulic conductivity and transmissivity and to other changes in vertical leakance. Applications of the results of the calibrated flow model in evaluation of solute transport may require further discretization of the contaminated area, including more sublayers, than were needed for calibration of the groundwater flow system itself. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/wri874260","usgsCitation":"Franks, B., 1988, Hydrogeology and flow of water in a sand and gravel aquifer contaminated by wood-preserving compounds, Pensacola, Florida: U.S. Geological Survey Water-Resources Investigations Report 87-4260, v, 72 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri874260.","productDescription":"v, 72 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":123427,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4260/report-thumb.jpg"},{"id":56040,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4260/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b23e4b07f02db6ade66","contributors":{"authors":[{"text":"Franks, B.J.","contributorId":107739,"corporation":false,"usgs":true,"family":"Franks","given":"B.J.","email":"","affiliations":[],"preferred":false,"id":197671,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
]}