Surface-water-quality data from selected monitoring stations in Connecticut were analyzed for trend, using the Seasonal Kendall test, for water years 1969-88, 1975-88, and 1981-88. The number of constituents and stations evaluated varied with the different time periods. The 39 monitoring stations included 26 freshwater streams with associated discharge data, 7 tidally affected streams, 4 harbor stations, and 2 surface impoundments. Flow-adjustment procedures were used where possible to minimize the effects of stream- flow variability on trend results.
The drainage area of the monitoring stations includes approximately 5,000 mi2 covering the State of Connecticut and about 11,000 mi2 in upstream drainage areas outside of the State. Drainage basin size for the freshwater streams ranges from 4.1 mi2 to 9,660 mi2. Land uses in the drainage basins range from undeveloped forested areas to highly urbanized metropolitan areas. During the period covered by the trend study, the State's population has grown, suburban development has increased, agricultural land use has decreased, and wastewater-treatment practices have improved.
Increases in specific conductance and in the concentrations of calcium, magnesium, chloride, sulfate, dissolved solids, and total solids were geographically widespread and numerous during water years 1975-88 and indicate a general increase statewide in dissolved constituents in streamflow, both in urbanized and less developed areas. The effects of increasing urbanization, including municipal and industrial wastewater, septic system leachate, nonpoint runoff, and atmospheric deposition of contaminants, are possible causes for these increases.
Decreases in turbidity and in the concentrations of total phosphorus, total organic carbon, and fecal coliform bacteria were geographically widespread and numerous during 1975-88. This general decrease in suspended material and bacteria may be attributable to basic improvements in the treatment of municipal and industrial wastewater during the period of record. Decreasing concentrations of total phosphorus may also be related to decreases in agricultural land use and to a decline in the use of detergents containing phosphorus. Detected decreases in total organic carbon and turbidity may have been caused, in part, by changes in sampling or analytical methods.
Increases in total nitrogen, total organic nitrogen, and total nitrite-plus- nitrate were geographically widespread and numerous during 1975-88 and appear to indicate effects from both point sources in urbanized basins and nonpoint sources in less developed basins. The number of stations with increasing concentrations of nitrogen constituents was much smaller during 1981-88 than during 1975-88. Decreases in total ammonia nitrogen were detected at 11 stations during 1981-88. Decreases in total ammonia, sometimes paired with increases in total nitrite-plus-nitrate, may result from improvements in wastewater treatment.
Increases in the concentration of dissolved oxygen, or dissolved oxygen as a percent of saturation, were geographically widespread and numerous during 1969-88 and 1975-88. Increases were less common during 1981-88. Increases in dissolved oxygen in urbanized basins may be related to major improvements in wastewater treatment during the 1970's and 1980's. The magnitude of the trends detected during 1969-88 may have been affected in part by a change, around 1974, in the model of the instrument used to measure dissolved oxygen in the field.
Statewide increases in pH were detected during 1969-88, 1975-88, and 1981-88, in both urbanized and less developed basins. The widespread increases in pH were unexpected, given the relatively acidic quality of precipitation in the region during the study period. Only two decreases in pH were detected, both in relatively undeveloped basins. Increases in pH in urbanized areas may be related to decreasing concentrations of ammonia and to requirements for neutralization of municipal and industrial wastewater.
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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4affe4b07f02db697ba6","contributors":{"authors":[{"text":"Trench, E. C.","contributorId":33346,"corporation":false,"usgs":true,"family":"Trench","given":"E.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":202852,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":22617,"text":"ofr96472 - 1996 - Spatial and temporal distribution of specific conductance, boron, and phosphorus in a sewage-contaminated aquifer near Ashumet Pond, Cape Cod, Massachusetts","interactions":[],"lastModifiedDate":"2019-12-05T16:32:21","indexId":"ofr96472","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-472","title":"Spatial and temporal distribution of specific conductance, boron, and phosphorus in a sewage-contaminated aquifer near Ashumet Pond, Cape Cod, Massachusetts","docAbstract":"Spatial and temporal distributions of specific conductance, boron, and phosphorus were determined in a sewage-contaminated sand and gravel aquifer near Ashumet Pond, Cape Cod, Massachusetts. The source of contamination is secondarily treated sewage that has been discharged onto rapid- infiltration sand beds at the Massachusetts Military Reservation since 1936. Contaminated ground water containing as much as 2 milligrams per liter of dissolved phosphorus is discharging into Ashumet Pond, and there is concern that the continued discharge of phosphorus into the pond will accelerate eutrophication of the pond. Water-quality data collected from observation wells and multilevel samplers from June through July 1995 were used to delineate the spatial distributions of specific conductance, boron, and phosphorus. Temporal distributions were determined using sample-interval-weighted average concen- trations calculated from data collected in 1993, 1994, and 1995. Specific conductances were greater than 400 microsiemens per centimeter at 25C as far as 1,200 feet downgradient from the infiltration beds. Boron concentrations were greater than 400 micrograms per liter as far as 1,800 feet down- gradient from the beds and phosphorus concen- trations were greater than 3.0 milligrams per liter as far as 1,200 feet from the beds. Variability in distributions of specific conductance and boron concentrations is attributed to the history and distribution of sewage disposal onto the infiltration beds. The distribution of phosphorus concentrations also is related to the history and distribution of sewage disposal onto the beds but additional variability is caused by chemical interactions with the aquifer materials. Temporal changes in specific conductance and boron from 1993 to 1995 were negligible, except in the lower part of the plume (below an altitude of about 5 feet above sea level), where changes in weighted-average specific conductance were greater than 100 microsiemens per centimeter at 25C. Temporal changes in phosphorus generally were small except in the lower part of the plume, where weighted-average phosphorus concentrations decreased more than 1.3 milligrams per liter from 1993 to 1994. This decrease was accompanied by an increase in specific conductance. High concen- trations of phosphorus associated with low and moderate specific conductances possibly are the result of rapid phosphorus desorption in response to an influx of uncontaminated ground water. As a result of the cessation of sewage disposal in December 1995, clean, oxygenated water moving into contaminated parts of the aquifer may cause rapid desorption of sorbed phosphorus and temporarily result in high dissolved phosphorus concentrations in the aquifer.","language":"English","publisher":"U.S. Geological Survey ","publisherLocation":"Reston, VA","doi":"10.3133/ofr96472","issn":"0094-9140","usgsCitation":"Bussey, K., and Walter, D.A., 1996, Spatial and temporal distribution of specific conductance, boron, and phosphorus in a sewage-contaminated aquifer near Ashumet Pond, Cape Cod, Massachusetts: U.S. Geological Survey Open-File Report 96-472, iv, 44 p., https://doi.org/10.3133/ofr96472.","productDescription":"iv, 44 p.","costCenters":[{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":52085,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0472/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":155389,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0472/report-thumb.jpg"}],"country":"United States","state":"Massachusetts","otherGeospatial":"Cape Cod","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -70.7794189453125,\n 41.6154423246811\n ],\n [\n -69.89501953125,\n 41.6154423246811\n ],\n [\n -69.89501953125,\n 42.1104489601222\n ],\n [\n -70.7794189453125,\n 42.1104489601222\n ],\n [\n -70.7794189453125,\n 41.6154423246811\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db6975ad","contributors":{"authors":[{"text":"Bussey, K.W.","contributorId":48210,"corporation":false,"usgs":true,"family":"Bussey","given":"K.W.","email":"","affiliations":[],"preferred":false,"id":188573,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Walter, D. A.","contributorId":75179,"corporation":false,"usgs":true,"family":"Walter","given":"D.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":188574,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":22939,"text":"ofr96360 - 1996 - Computer model of Raritan River Basin water-supply system in central New Jersey","interactions":[],"lastModifiedDate":"2012-02-02T00:07:55","indexId":"ofr96360","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-360","title":"Computer model of Raritan River Basin water-supply system in central New Jersey","docAbstract":"This report describes a computer model of the Raritan River Basin water-supply system in central New Jersey. The computer model provides a technical basis for evaluating the effects of alternative patterns of operation of the Raritan River Basin water-supply system during extended periods of below-average precipitation. The computer model is a continuity-accounting model consisting of a series of interconnected nodes. At each node, the inflow volume, outflow volume, and change in storage are determined and recorded for each month. The model runs with a given set of operating rules and water-use requirements including releases, pumpages, and diversions. The model can be used to assess the hypothetical performance of the Raritan River Basin water- supply system in past years under alternative sets of operating rules. It also can be used to forecast the likelihood of specified outcomes, such as the depletion of reservoir contents below a specified threshold or of streamflows below statutory minimum passing flows, for a period of up to 12 months. The model was constructed on the basis of current reservoir capacities and the natural, unregulated monthly runoff values recorded at U.S. Geological Survey streamflow- gaging stations in the basin.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nBranch of Information Services, distributor,","doi":"10.3133/ofr96360","issn":"0094-9140","usgsCitation":"Dunne, P., and Tasker, G.D., 1996, Computer model of Raritan River Basin water-supply system in central New Jersey: U.S. Geological Survey Open-File Report 96-360, iv, 62 p. :ill., maps ;28 cm., https://doi.org/10.3133/ofr96360.","productDescription":"iv, 62 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":154266,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0360/report-thumb.jpg"},{"id":52340,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0360/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a63fb","contributors":{"authors":[{"text":"Dunne, Paul","contributorId":86794,"corporation":false,"usgs":true,"family":"Dunne","given":"Paul","email":"","affiliations":[],"preferred":false,"id":189165,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tasker, Gary D.","contributorId":83097,"corporation":false,"usgs":true,"family":"Tasker","given":"Gary","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":189164,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":30357,"text":"wri964200 - 1996 - Hydrogeology and analysis of ground-water-flow system, Sagamore Marsh area, southeastern Massachusetts","interactions":[],"lastModifiedDate":"2018-05-17T14:08:59","indexId":"wri964200","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-4200","title":"Hydrogeology and analysis of ground-water-flow system, Sagamore Marsh area, southeastern Massachusetts","docAbstract":"A study of the hydrogeology and an analysis of the ground-water-flow system near Sagamore Marsh, southeastern Massachusetts, was undertaken to improve the understanding of the current (1994 95) hydrogeologic conditions near the marsh and how the ground-water system might respond to proposed changes in the tidal-stage regime of streams that flood and drain the marsh. Sagamore Marsh is in a coastal area that is bounded to the east by Cape Cod Bay and to the south by the Cape Cod Canal. The regional geology is characterized by deltaic and glaciolacustrine sediments. The sediments consist of gravel, sand, silt, and clay and are part of the Plymouth-Carver regional aquifer system. The glacial sediments are hounded laterally by marine sand, silt, and clay along the coast. The principal aquifer in the area consists of fine to coarse glacial sand and is locally confined by fine-grained glaciolacustrine deposits consisting of silt and sandy clay and fine-grained salt-marsh sediments consisting of peat and clay. The aquifer is underlain by finer grained glaciolacustrine sediments in upland areas and by marine clay along the coast.
Shallow ground water discharges primarily along the edge of the marsh, whereas deeper ground water flows beneath the marsh and discharges to Cape Cod Bay. Tidal pulses originating from Cape Cod Bay and from tidal channels in the marsh are rapidly attenuated in the subsurface. Tidal ranges in Cape Cod Bay and in the tidal channels were on the order of 9 and 1.5 feet, respectively, whereas tidal ranges in the ground-water levels were less than 0.2 foot. Tidal pulses measured in the water table beneath a barrier beach between the marsh and Cape Cod Bay were more in phase with tidal pulses from Cape Cod Bay than with tidal pulses from the tidal channels in Sagamore Marsh, whereas tidal pulses in the regional aquifer were more in phase with tidal pulses from the tidal channels.
A 5-day aquifer test at a public-supply well adjacent to the marsh gave a transmissivity of the regional aquifer of 9,300 to 10,900 feet squared per day and a hydraulic conductivity of 181 to 213 feet per day, assuming a saturated thickness of the aquifer of 51.3 feet. The regional aquifer became unconfined near the pumped well during the test. The ratio of tidal ranges in the tidal channel to the ranges in the underlying aquifer at two sites (the lower and upper marsh) indicated aquifer diffusivities for the marsh sediments of 380 and 170 feet squared per day; these values correspond to hydraulic conductivities of 2.5 x 10-3 and 1.7 x 10-3 feet per day, respectively. The maximum distances from the tidal channel at the lower and upper marsh sites where tidal ranges would exceed 0.01 foot, as calculated from aquifer diffusivities and current (1995) tidal ranges in the tidal channels, were 24.4 and 26.7 feet, respectively. The maximum distances from the tidal channel where tidal pulses in the ground water would exceed 0.01 foot, using potential increased tidal stages resulting from proposed tidal-stage modifications and predicted by the U.S. Army Corps of Engineers, were 37.1 and 42.0 feet, respectively.
A numerical model of the marsh and surrounding aquifer system indicated that the contributing area for the supply well adjacent to the marsh, for current (1994) pumping conditions, extends toward Great Herring Pond, about 2 miles northwest (upgradient) of the well, and does not extend beneath the marsh. The model also indicates that the predicted increases in tidal stages in the marsh will have a negligible effect on local ground-water levels.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964200","usgsCitation":"Walter, D.A., Masterson, J.P., and Barlow, P.M., 1996, Hydrogeology and analysis of ground-water-flow system, Sagamore Marsh area, southeastern Massachusetts: U.S. Geological Survey Water-Resources Investigations Report 96-4200, v, 41 p., https://doi.org/10.3133/wri964200.","productDescription":"v, 41 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"links":[{"id":345232,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4200/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124666,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4200/report-thumb.jpg"}],"country":"United States","state":"Massachusetts","otherGeospatial":"Sagamore Marsh","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4de4b07f02db6275e0","contributors":{"authors":[{"text":"Walter, Donald A. 0000-0003-0879-4477 dawalter@usgs.gov","orcid":"https://orcid.org/0000-0003-0879-4477","contributorId":1101,"corporation":false,"usgs":true,"family":"Walter","given":"Donald","email":"dawalter@usgs.gov","middleInitial":"A.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":203111,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Masterson, John P. 0000-0003-3202-4413 jpmaster@usgs.gov","orcid":"https://orcid.org/0000-0003-3202-4413","contributorId":171510,"corporation":false,"usgs":true,"family":"Masterson","given":"John","email":"jpmaster@usgs.gov","middleInitial":"P.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true},{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true}],"preferred":false,"id":203112,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Barlow, Paul M. 0000-0003-4247-6456 pbarlow@usgs.gov","orcid":"https://orcid.org/0000-0003-4247-6456","contributorId":1200,"corporation":false,"usgs":true,"family":"Barlow","given":"Paul","email":"pbarlow@usgs.gov","middleInitial":"M.","affiliations":[{"id":493,"text":"Office of Ground Water","active":true,"usgs":true}],"preferred":true,"id":203110,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":21751,"text":"ofr95124 - 1996 - Distribution of lithostratigraphic units within the central block of Yucca Mountain, Nevada; a three-dimensional computer-based model, version YMP.R2.0","interactions":[],"lastModifiedDate":"2018-06-07T16:04:01","indexId":"ofr95124","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"95-124","title":"Distribution of lithostratigraphic units within the central block of Yucca Mountain, Nevada; a three-dimensional computer-based model, version YMP.R2.0","language":"ENGLISH","publisher":"U.S. Geological Survey :\r\nBranch of Information Services [distributor],","doi":"10.3133/ofr95124","issn":"0566-8174","usgsCitation":"Buesch, D., Nelson, J.E., Dickerson, R.P., Drake, R., Spengler, R., Geslin, J.K., Moyer, T.C., and San Juan, C.A., 1996, Distribution of lithostratigraphic units within the central block of Yucca Mountain, Nevada; a three-dimensional computer-based model, version YMP.R2.0: U.S. Geological Survey Open-File Report 95-124, iv, 61 p. :ill., maps ;28 cm., https://doi.org/10.3133/ofr95124.","productDescription":"iv, 61 p. :ill., maps ;28 cm.","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":152988,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1995/0124/report-thumb.jpg"},{"id":51253,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1995/0124/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6fe4b07f02db6409b9","contributors":{"authors":[{"text":"Buesch, D.C. 0000-0002-4978-5027","orcid":"https://orcid.org/0000-0002-4978-5027","contributorId":73633,"corporation":false,"usgs":true,"family":"Buesch","given":"D.C.","affiliations":[],"preferred":false,"id":185534,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nelson, James E.","contributorId":205480,"corporation":false,"usgs":false,"family":"Nelson","given":"James","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":737446,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dickerson, Robert P.","contributorId":6461,"corporation":false,"usgs":true,"family":"Dickerson","given":"Robert","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":737447,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Drake, Ronald M. II rmdrake@usgs.gov","contributorId":168352,"corporation":false,"usgs":true,"family":"Drake","given":"Ronald M.","suffix":"II","email":"rmdrake@usgs.gov","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":false,"id":737448,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Spengler, Richard W.","contributorId":91498,"corporation":false,"usgs":true,"family":"Spengler","given":"Richard W.","affiliations":[],"preferred":false,"id":737449,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Geslin, Jeffrey K.","contributorId":20771,"corporation":false,"usgs":true,"family":"Geslin","given":"Jeffrey","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":737450,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Moyer, Thomas C.","contributorId":58661,"corporation":false,"usgs":true,"family":"Moyer","given":"Thomas","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":737451,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"San Juan, Carma A. 0000-0002-9151-1919 csanjuan@usgs.gov","orcid":"https://orcid.org/0000-0002-9151-1919","contributorId":1146,"corporation":false,"usgs":true,"family":"San Juan","given":"Carma","email":"csanjuan@usgs.gov","middleInitial":"A.","affiliations":[{"id":35995,"text":"Geology, Geophysics, and Geochemistry Science Center","active":true,"usgs":true},{"id":171,"text":"Central Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":737452,"contributorType":{"id":1,"text":"Authors"},"rank":8}]}} ,{"id":30036,"text":"wri964118 - 1996 - Description and field analysis of a coupled ground-water/surface-water flow model (MODFLOW/BRANCH) with modifications for structures and wetlands in southern Dade County, Florida","interactions":[],"lastModifiedDate":"2012-02-02T00:08:51","indexId":"wri964118","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-4118","title":"Description and field analysis of a coupled ground-water/surface-water flow model (MODFLOW/BRANCH) with modifications for structures and wetlands in southern Dade County, Florida","docAbstract":"A coupled surface-water model (BRANCH) and ground-water model (MODFLOW) model were tested to simulate the interacting wetlands/surface-water/ ground-water system of southern Dade County. Several options created for the MODFLOW ground- ground-water model were used in representing this field situation. The primary option is the MODBRANCH interfacing software, which allows leakage to be accounted for between the MODFLOW ground-water model and the BRANCH dynamic model for simulation of flow in an interconnected network of open channels. A modification to an existing software routine, which is referred to as BCF2, allows cells in MODFLOW to rewet when dry--a requirement in representing the seasonal wetlands in Dade County. A companion to BCF2 is the modified evapotranspiration routine EVT2. The EVT2 routine changes the cells where evapotranspiration occurs, depending on which cells are wet. The Streamlink package represents direct connections between the canals and wetlands at locations where canals open directly into overland flow. Within the BRANCH model, the capability to represent the numerous hydraulic structures, gated spillways, gated culverts, and pumps was added. The application of these modifications to model surface-water/ground-water interactions in southern Dade County demonstrated the usefulness of the coupled MODFLOW/BRANCH model. Ground-water and surface-water flows are both simulated with dynamic models. Flow exchange between models, intermittent wetting and drying, evapotranspiration, and hydraulic structure operations are all represented appropriately. Comparison was made with a simulation using the RIV1 package instead of MODBRANCH to represent the canals. RIV1 represents the canals by user-defined stages, and computes leakage to the aquifer. Greater accuracy in reproducing measured ground- water heads was achieved with MODBRANCH, which also computes dynamic flow conditions in the canals, unlike RIV1. The surface-water integrated flow and transport two-dimensional model (SWIFT2D) was also applied to the southeastern coastal wetlands for comparison with the wetlands flow approximation made in MODFLOW. MODFLOW simulates the wetlands as a highly conductive upper layer of the aquifer, whereas SWIFT2D solves the hydrodynamic equations. Comparison in this limited test demonstrated no specific advantage for either method of representation. However, much additional testing on a wider variety of geometric and hydraulic situations, such as in areas with greater tidal or other dynamic forcing effects, is needed to make definite conclusions. A submodel of the existing southern Dade County model schematization was used to examine water-delivery alternatives proposed by the U.S. Army Corps of Engineers. For this application, the coupled MODFLOW/BRANCH model was used as a design tool. A new canal and several pumps to be tested to maintain lower water levels in a residential area (while water levels in the Everglades are raised) were added to the model schematization. The pumps were assumed to have infinite supply capacity in the model so that their maximum pumping rates during the simulation could be used to determine pump sizes.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nU.S. Geological Survey, Branch of Information Services [distributor],","doi":"10.3133/wri964118","usgsCitation":"Swain, E., Howie, B., and Dixon, J., 1996, Description and field analysis of a coupled ground-water/surface-water flow model (MODFLOW/BRANCH) with modifications for structures and wetlands in southern Dade County, Florida: U.S. Geological Survey Water-Resources Investigations Report 96-4118, iv, 67 p. :ill. (some col.), maps (some col.) 28 cm., https://doi.org/10.3133/wri964118.","productDescription":"iv, 67 p. :ill. (some col.), maps (some col.) 28 cm.","costCenters":[],"links":[{"id":123743,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4118/report-thumb.jpg"},{"id":58839,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4118/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66db99","contributors":{"authors":[{"text":"Swain, E.D. 0000-0001-7168-708X","orcid":"https://orcid.org/0000-0001-7168-708X","contributorId":29007,"corporation":false,"usgs":true,"family":"Swain","given":"E.D.","affiliations":[],"preferred":false,"id":202573,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Howie, Barbara","contributorId":54248,"corporation":false,"usgs":true,"family":"Howie","given":"Barbara","email":"","affiliations":[],"preferred":false,"id":202574,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dixon, Joann","contributorId":19981,"corporation":false,"usgs":true,"family":"Dixon","given":"Joann","affiliations":[],"preferred":false,"id":202572,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":24365,"text":"ofr96150 - 1996 - Precipitation, streamflow and water quality data from selected sites in the City of Charlotte and Mecklenburg County, North Carolina, 1993-95","interactions":[],"lastModifiedDate":"2017-01-04T12:56:53","indexId":"ofr96150","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-150","title":"Precipitation, streamflow and water quality data from selected sites in the City of Charlotte and Mecklenburg County, North Carolina, 1993-95","docAbstract":"Charlotte and Mecklenburg County from October 1993 through June 1995 to identify the type, concentration, and amount of nonpoint-source stormwater runoff within the area. The data collected include measurements of precipitation; streamflow; physical characteristics, such as water temperature, pH, specific conductance, biochemical oxygen demand, oil and grease, and suspended sediment concentrations; and concentrations of nutrients, metals and minor constituents, and organic compounds.\r\n\r\nThese data should provide valuable information needed for (1) planned watershed simulation models, (2) early warning of possible flooding, (3) estimates of nonpoint-source constituent loadings to the Catawba River, and (4) characterization of water quality in relation to basin conditions.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nInformation Services [distributor],","doi":"10.3133/ofr96150","issn":"0094-9140","usgsCitation":"Robinson, J.B., Hazell, W., and Garrett, R.G., 1996, Precipitation, streamflow and water quality data from selected sites in the City of Charlotte and Mecklenburg County, North Carolina, 1993-95: U.S. Geological Survey Open-File Report 96-150, iv, 136 p. :ill. (some col.), col maps ;28 cm., https://doi.org/10.3133/ofr96150.","productDescription":"iv, 136 p. :ill. (some col.), col maps ;28 cm.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":156241,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0150/report-thumb.jpg"},{"id":53463,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0150/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"North Carolina","county":"Mecklenburg County","city":"Charlotte","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-80.7823,35.5113],[-80.7867,35.5031],[-80.7889,35.4949],[-80.7831,35.4836],[-80.7819,35.475],[-80.7779,35.4668],[-80.7778,35.4614],[-80.7744,35.4578],[-80.7549,35.423],[-80.7525,35.4148],[-80.7553,35.4125],[-80.7638,35.4134],[-80.7693,35.402],[-80.7551,35.3944],[-80.7364,35.3786],[-80.7187,35.3624],[-80.704,35.3552],[-80.6983,35.3507],[-80.6822,35.3131],[-80.6677,35.2705],[-80.6214,35.2499],[-80.5954,35.2369],[-80.5485,35.2108],[-80.6245,35.1487],[-80.7328,35.0627],[-80.7645,35.0375],[-80.7684,35.0348],[-80.7746,35.0329],[-80.7858,35.0315],[-80.7892,35.0314],[-80.8009,35.0286],[-80.8155,35.0204],[-80.8194,35.019],[-80.8216,35.018],[-80.8216,35.0167],[-80.8288,35.0098],[-80.835,35.0061],[-80.8405,35.0016],[-80.8604,35.0246],[-80.8854,35.0535],[-80.9016,35.0716],[-80.9312,35.1049],[-80.9373,35.1018],[-81.0383,35.0452],[-81.0419,35.0432],[-81.0447,35.0468],[-81.0464,35.0482],[-81.0483,35.0507],[-81.0503,35.0527],[-81.0528,35.0557],[-81.0548,35.0582],[-81.0568,35.0611],[-81.0577,35.0636],[-81.0586,35.067],[-81.0582,35.0722],[-81.0577,35.0788],[-81.0566,35.0834],[-81.0554,35.0868],[-81.0541,35.0904],[-81.0533,35.0927],[-81.0523,35.0956],[-81.0503,35.0975],[-81.0487,35.099],[-81.0462,35.1003],[-81.0437,35.1014],[-81.042,35.1022],[-81.0391,35.1027],[-81.0369,35.1036],[-81.0352,35.1054],[-81.0344,35.1072],[-81.0341,35.1095],[-81.0341,35.1136],[-81.0358,35.1186],[-81.0363,35.1213],[-81.038,35.124],[-81.0408,35.1267],[-81.0425,35.1281],[-81.0454,35.1289],[-81.0476,35.1295],[-81.0499,35.1302],[-81.051,35.1313],[-81.0521,35.1335],[-81.0523,35.1365],[-81.0517,35.1392],[-81.0501,35.142],[-81.0476,35.1463],[-81.0448,35.1494],[-81.0238,35.1486],[-81.0176,35.1536],[-81.0109,35.1532],[-81.0076,35.1569],[-81.0088,35.165],[-81.0049,35.1728],[-81.0045,35.1814],[-81.0046,35.1864],[-81.0063,35.1923],[-81.0064,35.1973],[-81.0054,35.2055],[-81.0071,35.2109],[-81.0129,35.2231],[-81.0113,35.2309],[-81.012,35.2349],[-81.0082,35.2509],[-81.0139,35.2585],[-81.0152,35.2685],[-81.0143,35.2876],[-81.0133,35.293],[-81.0105,35.2944],[-81.0033,35.3017],[-81.0022,35.3045],[-80.9961,35.3113],[-80.9938,35.3132],[-80.9894,35.3205],[-80.9844,35.3237],[-80.9805,35.3287],[-80.9823,35.3341],[-80.984,35.3373],[-80.9818,35.3446],[-80.9706,35.3501],[-80.9656,35.3506],[-80.9593,35.3489],[-80.9537,35.3521],[-80.9442,35.3521],[-80.9374,35.3572],[-80.9285,35.3614],[-80.9268,35.3627],[-80.9296,35.3636],[-80.9432,35.3658],[-80.9505,35.3675],[-80.9563,35.3738],[-80.9597,35.3756],[-80.9625,35.3756],[-80.9647,35.3738],[-80.9669,35.3688],[-80.9697,35.3669],[-80.9742,35.3642],[-80.9776,35.3646],[-80.9844,35.3695],[-80.9868,35.38],[-80.9846,35.3822],[-80.9806,35.3823],[-80.9761,35.3828],[-80.9632,35.3901],[-80.9554,35.3925],[-80.9549,35.4006],[-80.959,35.4133],[-80.9569,35.4288],[-80.9587,35.436],[-80.9527,35.446],[-80.9465,35.4524],[-80.9421,35.457],[-80.9432,35.4602],[-80.9506,35.4656],[-80.9518,35.4701],[-80.948,35.481],[-80.947,35.486],[-80.951,35.4942],[-80.9612,35.4986],[-80.9664,35.509],[-80.9637,35.5131],[-80.9586,35.5163],[-80.9569,35.5177],[-80.7823,35.5113]]]},\"properties\":{\"name\":\"Mecklenburg\",\"state\":\"NC\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67baea","contributors":{"authors":[{"text":"Robinson, J. B.","contributorId":32564,"corporation":false,"usgs":true,"family":"Robinson","given":"J.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":191780,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hazell, W. F.","contributorId":40625,"corporation":false,"usgs":true,"family":"Hazell","given":"W. F.","affiliations":[],"preferred":false,"id":191781,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Garrett, R. G.","contributorId":93929,"corporation":false,"usgs":true,"family":"Garrett","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":191782,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":27582,"text":"wri964182 - 1996 - Hydrogeology of the area near the J4 test cell, Arnold Air Force Base, Tennessee","interactions":[],"lastModifiedDate":"2012-02-02T00:08:40","indexId":"wri964182","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-4182","title":"Hydrogeology of the area near the J4 test cell, Arnold Air Force Base, Tennessee","docAbstract":"The U.S. Air Force operates a major aerospace systems testing facility at Arnold Engineering Development Center (AEDC) in Coffee County, Tennessee. Dewatering operations at one of the test facilities, the J4 test cell, has affected the local ground-water hydrology. The J4 test cell is approximately 100 feet in diameter, extends approximately 250 feet below land surface, and penetrates several aquifers. Ground water is pumped continuously from around the test cell to keep the cell structurally intact. Because of the test cell's depth, dewatering has depressed water levels in the aquifers surrounding the site. The depressions that have developed exhibit anisotropy that is controlled by zones of high permeability in the aquifers. Additionally, contaminants - predominately volatile organic compounds - are present in the ground-water discharge from the test cell and in ground water at several other Installation Restoration Program (IRP) sites within the AEDC facility. The dewatering activities at J4 are drawing these contaminants from the nearby sites. The effects of dewatering at the J4 test cell were investigated by studying the lithologic and hydraulic characteristics of the aquifers, investigating the anisotropy and zones of secondary permeability using geophysical techniques, mapping the potentiometric surfaces of the underlying aquifers, and developing a conceptual model of the ground-water-flow system local to the test cell. Contour maps of the potentiometric surfaces in the shallow, Manchester, and Fort Payne aquifers (collectively, part of the Highland Rim aquifer system) show anisotropic water-level depressions centered on the J4 test cell. This anisotropy is the result of features of high permeability such as chert-gravel zones in the regolith and fractures, joints, and bedding planes in the bedrock. The presence of these features of high permeability in the Manchester aquifer results in complex flow patterns in the Highland Rim aquifers near the J4 test cell. The occurrence, distribution, and orientation of these features has a great effect on ground-water flow to the J4 test cell. The depression caused by dewatering extends out horizontally through the aquifers along the most permeable pathways. Since the aquifers above the Chattanooga Shale are not separated by distinct confining units, areas in adjacent aquifers above and below these zones of high permeability in the Manchester aquifer are also dewatered. Conditions in all Highland Rim aquifers approximate steady-state equilibrium because ground-water withdrawal at the test cell has been continuous since the late 1960's. The average ground-water discharge from the dewatering system at the J4 test cell was 105 gallons per minute, for 1992-95. The ground-water capture areas in each aquifer extend into all or parts of landfill #2 and leaching pit #2 (IRP site 1), the main testing area (IRP site 7), and the old fire training area (IRP site 10). IRP sites 8 and 12 are outside the ground-water capture areas. Of the 35 sampled wells in the J4 area, 10 produced water samples containing chlorinated organic compounds such as 1,2-dichloroethane (1,2-DCA), 1,1-dichloroethylene (1,1-DCE), and trichloroethylene (TCE) in concentrations which exceeded the Tennessee Department of Environment and Conservation Maximum Contaminant Levels (MCL's) for public water-supply systems. The highest concentrations were detected in samples from well AEDC-274 with 45 micrograms per liter (mg/L) 1,2-DCA, 320 mg/L 1,1-DCE, and 1,200 mg/L TCE. These compounds are synthetic and do not occur naturally in the environment. A sample of the ground-water discharge from the J4 test cell also contained concentrations of these compounds that exceed MCL's. Chlorinated organic compounds, including 1,2-DCA; 1,1-DCE; and TCE also have been detected at IRP sites 1, 7, 8, nd 10. The six dewatering wells surrounding the J4 test cell penetrate the Chattanooga Shale and are open to the Highland Rim aquifer system, there","language":"ENGLISH","publisher":"U.S. Geological Survey ;","doi":"10.3133/wri964182","usgsCitation":"Haugh, C., 1996, Hydrogeology of the area near the J4 test cell, Arnold Air Force Base, Tennessee: U.S. Geological Survey Water-Resources Investigations Report 96-4182, v, 43 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri964182.","productDescription":"v, 43 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":119980,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4182/report-thumb.jpg"},{"id":56438,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4182/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649739","contributors":{"authors":[{"text":"Haugh, C.J.","contributorId":24380,"corporation":false,"usgs":true,"family":"Haugh","given":"C.J.","email":"","affiliations":[],"preferred":false,"id":198365,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":33101,"text":"b00O - 1996 - Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation","interactions":[{"subject":{"id":33101,"text":"b00O - 1996 - Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation","indexId":"b00O","publicationYear":"1996","noYear":false,"chapter":"O","title":"Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation"},"predicate":"IS_PART_OF","object":{"id":33201,"text":"b2000 - 1993 - Evolution of sedimentary basins: Paradox Basin","indexId":"b2000","publicationYear":"1993","noYear":false,"title":"Evolution of sedimentary basins: Paradox Basin"},"id":1}],"isPartOf":{"id":33201,"text":"b2000 - 1993 - Evolution of sedimentary basins: Paradox Basin","indexId":"b2000","publicationYear":"1993","noYear":false,"title":"Evolution of sedimentary basins: Paradox Basin"},"lastModifiedDate":"2021-11-24T20:07:41.454988","indexId":"b00O","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"2000","chapter":"O","title":"Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation","docAbstract":"The Ismay-Desert Creek interval and Cane Creek cycle of the Alkali Gulch interval of the Middle Pennsylvanian Paradox Formation in the Paradox Basin of Utah and Colorado contain excellent organic-rich source rocks having total organic carbon contents ranging from 0.5 to 11.0 percent. The source rocks in both intervals contain types I, II, and III organic matter and are potential source rocks for both oil and gas. Organic matter in the Ismay-Desert Creek interval and Cane Creek cycle of the Alkali Gulch interval (hereinafter referred to in this report as the \"Cane Creek cycle\") probably is more terrestrial in origin in the eastern part of the basin and is interpreted to have contributed to some of the gas produced there.
Thermal maturity increases from southwest to northeast for both the Ismay-Desert Creek interval and Cane Creek cycle, following structural and burial trends throughout the basin. In the northernmost part of the basin, the combination of a relatively thick Tertiary sedimentary sequence and high basinal heat flow has produced very high thermal maturities. Although general thermal maturity trends are similar for both the Ismay-Desert Creek interval and Cane Creek cycle, actual maturity levels are higher for the Cane Creek due to the additional thickness (as much as several thousand feet) of Middle Pennsylvanian section.
Throughout most of the basin, the Ismay-Desert Creek interval is mature and in the petroleum-generation window (0.10 to 0.50 production index (PI)), and both oil and gas are produced; in the south-central to southwestern part of the basin, however, the interval is marginally mature (<0.10 PI) for petroleum generation, and mainly oil is produced. In contrast, the more mature Cane Creek cycle contains no marginally immature areas—it is mature (>0.10 PI) in the central part of the basin and is overmature (past the petroleum-generation window (>0.50 PI)) throughout most of the eastern part of the basin. The Cane Creek cycle generally produces oil and associated gas throughout the western and central parts of the basin and thermogenic gas in the eastern part of the basin.
Burial and thermal-history models were constructed for six different areas of the Paradox Basin. In the Monument upwarp area, the least mature part of the basin, the Ismay-Desert Creek interval and Cane Creek cycle have thermal maturities of 0.10 and 0.20 PI and were buried to 13,400 ft and 14,300 ft, respectively. A constant heat flow through time of 40 mWm-2 (milliwatts per square meter) is postulated for this area. Significant petroleum generation began at 45 Ma for the Ismay-Desert Creek interval and at 69 Ma for the Cane Creek cycle.
In the area around the confluence of the Green and Colorado Rivers, the Ismay-Desert Creek interval and Cane Creek cycle have thermal maturities of 0.20 and 0.25 PI and were buried to 13,000 ft and 14,200 ft, respectively. A constant heat flow through time of 42 mWm-2 is postulated for this area. Significant petroleum generation began at 60 Ma for the Ismay-Desert Creek interval and at 75 Ma for the Cane Creek cycle.
In the area around the town of Green River, Utah, the Ismay-Desert Creek interval and Cane Creek cycle have thermal maturities of 0.60 and greater and were buried to 14,000 ft and 15,400 ft, respectively. A constant heat flow through time of 53 mWm-2 is proposed for this area. Significant petroleum generation began at 82 Ma for the Ismay-Desert Creek interval and at 85 Ma for the Cane Creek cycle.
Around Moab, Utah, in the deeper, eastern part of the basin, the Ismay-Desert Creek interval and Cane Creek cycle have thermal maturities of 0.30 and around 0.35 PI and were buried to 18,250 ft and 22,000 ft, respectively. A constant heat flow through time of 40 mWm-2 is postulated for this area. Significant petroleum generation began at 79 Ma for the Ismay-Desert Creek interval and at 90 Ma for the Cane Creek cycle.
At Lisbon Valley, also in the structurally deeper part of the basin, the Ismayy–Desert Creek interval and Cane Creek cycle have thermal maturities of 0.30 and greater than 0.60 PI and were buried to 15,750 ft and 21,500 ft, respectively. A constant heat flow through time of 44 mWm–2 is postulated for this area. Significant petroleum generation began at 79 Ma for the Ismay–Desert Creek interval and at 100 Ma for the Cane Creek cycle.
The area around Hermosa, Colo., in the southeastern part of the basin, has experienced a shallower burial history than the other areas in the basin, yet it has one of the highest thermal maturities. Here, the Ismay–Desert Creek interval and Cane Creek cycle have vitrinite reflectance values of 1.58 and 1.63 percent and were buried to 13,700 ft and 15,500 ft, respectively. Due to Tertiary igneous activity in this part of the basin, a variable heat flow is proposed: from 600 to 30 Ma, 45 mWm–2; from 30 to 25 Ma, 63 mWm–2; and from 25 Ma to present, 50 mWm–2. Significant petroleum generation began at 72 Ma for the Ismay–Desert Creek interval and at 76 Ma for the Cane Creek cycle.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Evolution of sedimentary basins: Paradox basin","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b00O","usgsCitation":"Nuccio, V.F., and Condon, S.M., 1996, Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation: U.S. Geological Survey Bulletin 2000, iii, 41 p., https://doi.org/10.3133/b00O.","productDescription":"iii, 41 p.","costCenters":[],"links":[{"id":392102,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_22256.htm"},{"id":3297,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/bul/b2000o/b2000o.html","linkFileType":{"id":5,"text":"html"}},{"id":160624,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"Colorado, Utah","otherGeospatial":"Paradox Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -110.5,\n 36.417\n ],\n [\n -107.5,\n 36.417\n ],\n [\n -107.5,\n 39.250\n ],\n [\n -110.5,\n 39.250\n ],\n [\n -110.5,\n 36.417\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48b4e4b07f02db532964","contributors":{"authors":[{"text":"Nuccio, Vito F. vnuccio@usgs.gov","contributorId":853,"corporation":false,"usgs":true,"family":"Nuccio","given":"Vito","email":"vnuccio@usgs.gov","middleInitial":"F.","affiliations":[],"preferred":true,"id":209893,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Condon, Steven M.","contributorId":95464,"corporation":false,"usgs":true,"family":"Condon","given":"Steven","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":209894,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":27484,"text":"wri964056 - 1996 - Water resources of Spink County, South Dakota","interactions":[],"lastModifiedDate":"2012-02-02T00:08:35","indexId":"wri964056","displayToPublicDate":"1997-02-01T00:00:00","publicationYear":"1996","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":"96-4056","title":"Water resources of Spink County, South Dakota","docAbstract":"Spink County, an agricultural area of about 1,505 square miles, is in the flat to gently rolling James River lowland of east-central South Dakota. The water resources are characterized by the highly variable flows of the James River and its tributaries and by aquifers both in glacial deposits of sand and gravel, and in sandstone in the bedrock. Glacial aquifers underlie about half of the county, and bedrock aquifers underlie most of the county. The James River is an intermittent prairie stream that drains nearly 8,900 square miles north of Spink County and has an average annual discharge of about 124 cubic feet per second where it enters the county. The discharge is augmented by the flow of Snake and Turtle Creeks, each of which has an average annual flow of about 25 to 30 cubic feet per second. Streamflow is unreliable as a water supply because precipitation, which averages 18.5 inches annually, is erratic both in volume and in distribution, and because the average annual potential evapotranspiration rate is 43 inches. The flow of tributaries generally ceases by summer, and zero flows are common in the James River in fall and winter. Aquifers in glacial drift deposits store nearly 3.3 million acre-feet of fresh to slightly saline water at depths of from near land surface to more than 500 feet below land surface beneath an area of about 760 square miles. Yields of properly developed wells in the more productive aquifers exceed 1,000 gallons per minute in some areas. Withdrawals from the aquifers, mostly for irrigation, totaled about 15,000 acre-feet of water in 1990. Water levels in observation wells generally have declined less than 15 feet over several decades of increasing pumpage for irrigation, but locally have declined nearly 30 feet. Water levels generally rose during the wet period of 1983-86. In Spink County, bedrock aquifers store more than 40 million acre-feet of slightly to moderately saline water at depths of from 80 to about 1,300 feet below land surface. Yields of properly developed wells range from 2 to 600 gallons per minute. The artesian head of the heavily used Dakota aquifer has declined about 350 feet in the approximately 100 years since the first artesian wells were drilled in the county, but water levels have stabilized locally as a result of decreases in the discharge of water from the wells. Initial flows of from 4 gallons per minute to as much as 30 gallons per minute of very hard water can be obtained in the southwestern part of the county, where drillers report artesian heads of nearly 100 feet above land surface. The quality of water from aquifers in glacial drift varies greatly, even within an aquifer. Concentrations of dissolved solids in samples ranged from 151 to 9,610 milligrams per liter, and hardness ranged from 84 to 3,700 milligrams per liter. Median concentrations of dissolved solids, sulfate, iron, and manganese in some glacial aquifers are near or exceed Secondary Maximum Contaminant Levels (SMCL's) established by the U.S. Environmental Protection Agency (EPA). Some of the water from aquifers in glacial drift is suitable for irrigation use. Water samples from aquifers in the bedrock contained concentrations of dissolved solids that ranged from 1,410 to 2,670 milligrams per liter (sum of constituents) and hardness that ranged from 10 to 1,400 milligrams per liter; these concentrations generally are largest for aquifers below the Dakota aquifer. Median concentrations of dissolved solids, sulfate, iron, and manganese in Dakota wells either are near or exceed EPA SMCL's. Dissolved solids, sodium, and boron concentrations in water from bedrock aquifers commonly are too large for the water to be suitable for irrigation use.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nInformation Services, [distributor],","doi":"10.3133/wri964056","usgsCitation":"Hamilton, L., and Howells, L., 1996, Water resources of Spink County, South Dakota: U.S. Geological Survey Water-Resources Investigations Report 96-4056, v, 68 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri964056.","productDescription":"v, 68 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":123757,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4056/report-thumb.jpg"},{"id":56335,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4056/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e3e4b07f02db5e58c9","contributors":{"authors":[{"text":"Hamilton, L.J.","contributorId":102917,"corporation":false,"usgs":true,"family":"Hamilton","given":"L.J.","email":"","affiliations":[],"preferred":false,"id":198198,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Howells, L.W.","contributorId":89887,"corporation":false,"usgs":true,"family":"Howells","given":"L.W.","email":"","affiliations":[],"preferred":false,"id":198197,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":25781,"text":"wri964142 - 1996 - Streambed stresses and flow around bridge piers","interactions":[],"lastModifiedDate":"2021-01-27T19:50:24.564815","indexId":"wri964142","displayToPublicDate":"1997-02-01T00:00:00","publicationYear":"1996","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":"96-4142","title":"Streambed stresses and flow around bridge piers","docAbstract":"The effect of irrigation drainage on the water quality and wildlife of the Klamath Basin in California and Oregon was evaluated during 1990-92 as part of the National Irrigation Water Quality Program of the U.S. Department of the Interior. The study focused on land serviced by the Bureau of Reclamation Klamath Project, which supplies irrigation water to agricultural land in the Klamath Basin and the Lost River Basin. The Tule Lake and Lower Klamath National Wildlife Refuges, managed by the U.S. Fish and Wildlife Service, are in the study area. These refuges provide critical resting and breeding habitat for waterfowl on the Pacific flyway and are dependent on irrigation drainwater from upstream agriculture for most of their water supply.
Water-quality characteristics throughout the study area were typical of highly eutrophic systems during the summer months of 1991 and 1992. Dissolved-oxygen concentrations and pH tended to fluctuate each day in response to diurnal patterns of photosynthesis, and frequently exceeded criteria for protection of aquatic organisms.
Nitrogen and phosphorus concentrations were generally at or above threshold levels characteristic of eutrophic lakes and streams. At most sites the bulk of dissolved nitrogen was organically bound. Elevated ammonia concentrations were common in the study area, especially downstream of drain inputs. High pH of water increased the toxicity of ammonia, and concentrations exceeded criteria at sites upstream and downstream of irrigated land. Concentrations of ammonia in samples from small drains on the Tule Lake refuge leaseland were higher than those measured in the larger, integrating drains at primary monitoring sites. The mean ammonia concentration in leaseland drains [1.21 milligrams per liter (mg/L)] was significantly higher than the mean concentration in canals delivering water to the leaseland fields (0.065 mg/L) and higher than concentrations reported to be lethal to Daphnia magna (median lethal concentration of 0.66 mg/L). Dissolved-oxygen concentrations also were lower, and Daphnia survivability measured during in situ bioassays was correspondingly lower in the leaseland drains than in water delivery canals.
In static laboratory bioassays, water samples collected at the primary monitoring sites caused toxicity in up to 78 percent of Lemna minor tests, in up to 49 percent of Xenopus laevis tests, in 17 percent and 8 percent of Hyalella azteca and Pimephales promelas tests, respectively, and 0 percent in Daphnia magna tests. In situ exposure at the sites caused mortality in more than 83 percent of Pimephales tests and in more than 41 percent of Daphnia and Hyalella tests. Much of the observed toxicity appears to have been caused by low dissolved oxygen, high pH, and ammonia. Although water in the study area was toxic to a variety of organisms, no statistically significant differences in the degree of toxicity between sites were observed above or below irrigated agricultural land in any of the bioassays.
Pesticides were frequently detected in water samples collected at the monitoring sites during the 1991 and 1992 irrigation seasons. Among the most frequently detected compounds were the herbicides simazine, metribuzin, EPTC, and metolachlor and the insecticide terbufos. All the insecticides detected were at concentrations substantially below acute toxicity values reported for aquatic organisms.
The herbicide acrolein has been used extensively in the basin to manage aquatic plant growth in irrigation canals and drains. The concentration of acrolein was monitored in a canal near Tule Lake after an application in order to evaluate the potential for the pesticide to be transported to refuge waters. Although acrolein concentrations were toxic to fish in the channels adjacent to Tule Lake, very little of the canal water entered the refuge during the monitoring period.
Organochlorine pesticide concentrations in 25 surficial sediment samples collected in 1990 were below baseline levels commonly found in soils and sediment. Seventeen sediment samples were analyzed for chlorophenoxy acid herbicides and two samples were analyzed for organophosphorus and carbamate insecticides in 1992. No pesticides were detected in any of these samples.
Residues of the trace elements selenium, mercury, and arsenic in algae, invertebrates, fish, and avian eggs revealed no bioaccumulation problems. Concentrations of organochlorine compounds, especially of p,p' DDE, were associated with a mean 11-percent eggshell thinning in white-faced ibis. However, ibis populations appear to be increasing, and some eggs of ibis were relatively low in DDE concentration. DDE concentrations in eggs of western grebes were not as high as in the eggs of ibis. Concentrations and types of organochlorine compounds detected in grebe and ibis eggs were highly variable, indicating that the birds were exposed to these compounds outside the basin.
Fish and invertebrates inhabiting drainwater were representative of pollution-tolerant species assemblages. The aquatic communities retained little of their historic ecological structure. Extensive hydrologic modifications and hypereutrophic conditions in Klamath Basin waterways have degraded the quality of aquatic habitat and altered aquatic communities.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954232","usgsCitation":"Dileanis, P.D., Schwarzbach, S.E., and Bennett, J., 1996, Detailed study of water quality, bottom sediment, and biota associated with irrigation drainage in the Klamath Basin, California and Oregon, 1990-92: U.S. Geological Survey Water-Resources Investigations Report 95-4232, vii, 68 p., https://doi.org/10.3133/wri954232.","productDescription":"vii, 68 p.","costCenters":[],"links":[{"id":122795,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4232/report-thumb.jpg"},{"id":54170,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4232/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"California, Oregon","otherGeospatial":"Klamath Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122,\n 41.75\n ],\n [\n -121,\n 41.75\n ],\n [\n -121,\n 42.3\n ],\n [\n -122,\n 42.3\n ],\n [\n -122,\n 41.75\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa8e4b07f02db667afe","contributors":{"authors":[{"text":"Dileanis, Peter D. dileanis@usgs.gov","contributorId":71541,"corporation":false,"usgs":true,"family":"Dileanis","given":"Peter","email":"dileanis@usgs.gov","middleInitial":"D.","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":false,"id":193704,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schwarzbach, Steven E. steven_schwarzbach@usgs.gov","contributorId":1025,"corporation":false,"usgs":true,"family":"Schwarzbach","given":"Steven","email":"steven_schwarzbach@usgs.gov","middleInitial":"E.","affiliations":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"preferred":true,"id":193703,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bennett, Jewel","contributorId":28632,"corporation":false,"usgs":true,"family":"Bennett","given":"Jewel","email":"","affiliations":[],"preferred":false,"id":193702,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":25869,"text":"wri954217 - 1996 - Geohydrologic site characterization of the municipal solid waste landfill facility, U.S. Army Air Defense Artillery Center and Fort Bliss, El Paso County, Texas","interactions":[],"lastModifiedDate":"2024-01-16T21:15:01.036973","indexId":"wri954217","displayToPublicDate":"1997-02-01T00:00:00","publicationYear":"1996","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":"95-4217","title":"Geohydrologic site characterization of the municipal solid waste landfill facility, U.S. Army Air Defense Artillery Center and Fort Bliss, El Paso County, Texas","docAbstract":"Geohydrologic conditions of the Municipal Solid Waste Landfill Facility (MSWLF) on the U.S. Army Air Defense Artillery Center and Fort Bliss, El Paso County, Texas, were evaluated by the U.S. Geological Survey in cooperation with the U.S. Army. The 106.03-acre MSWLF has been in operation since January 1974. The landfill contains household refuse, Post solid wastes, bulky items, grass and tree trimmings from family housing, refuse from litter cans, construction debris, classified waste (dry), dead animals, asbestos, and empty oil cans.
The MSWLF, located about 1,200 feet east of the nearest occupied structure, is estimated to receive an average of approximately 56 tons of municipal solid waste per day and, at a fill rate of 1-4 acres per year, is expected to reach its capacity by the year 2004. The MSWLF is located in the Hueco Bolson, 4 miles east of the Franklin Mountains. Elevations at the MSWLF range from 3,907 to 3,937 feet above sea level. The climate at the MSWLF and vicinity is arid continental, characterized by an abundance of sunny days, high summer temperatures, relatively cool winters typical of arid areas, scanty rainfall, and very low humidity throughout the year. Average annual temperature near the MSWLF and vicinity is 63.3 degrees Fahrenheit and annual precipitation is 7.8 inches. Potential evaporation in the El Paso area was estimated to be 65 inches per year. Soils at and adjacent to the MSWLF are nearly level to gently sloping, have a fine sandy loam subsoil, and are moderately deep over caliche.
The MSWLF is underlain by Hueco Bolson deposits of Tertiary age and typically are composed of unconsolidated to slightly consolidated interbedded sands, clay, silt, gravel, and caliche. Individual beds are not well defined and range in thickness from a fraction of an inch to about 100 feet. The primary source of ground water in the MSWLF area is in the deposits of the Hueco Bolson. A relatively thick vadose zone of approximately 300 feet overlies the aquifer of the Hueco Bolson deposits in the vicinity of the MSWLF. A deep water table prevails for all of the study area. Whether any perched water zones exist below the MSWLF is unknown. Under current conditions, extensive ground-water development by the City of El Paso encompasses the MSWLF. Hydraulic characteristics of the Hueco Bolson vary significantly as a result of the nonuniform nature of the individual beds. Wells in the vicinity of the MSWLF range in depth from about 600 feet to greater than 1,200 feet. Recharge resulting from direct infiltration of precipitation is minor due to the high evaporation and low precipitation rates. The hydraulic gradient in the vicinity of the MSWLF is generally to the south but may vary due to pumpage of a well located on the northeast corner of the perimeter boundary. Ground-water monitoring data for the MSWLF vicinity show a water-level decline of 55.65 feet from November 1958 to December 1987. Depth to water at the northeast corner of the MSWLF as of July 26, 1994, was 325.8 feet below land surface.
The city-operated Shearman Well Field, located north of the MSWLF, is a primary source of ground water for the City of El Paso. The test-pumping rate of well JL-49-05-914 (the well nearest to the MSWLF having test-pumping data) was 1,972 gallons per minute on July 20, 1992; the static water level prior to pumping was 317.54 feet below land surface. El Paso Water Utilities reports that the pumping level after 8 hours of pumping was 367.80 feet below land surface, resulting in a drawdown of 50.26 feet, transmissivity of 22,200 feet squared per day (166,000 gallons per day per foot), and specific capacity of 39.2 gallons per minute per foot of drawdown. After the well was shut off, the well recovered to a static water level of 317.46 feet below land surface on July 21, 1992.
Ground water in the El Paso area is chemically suitable for most uses. El Paso Water Utilities reports that concentrations of dissolved solids in the vicinity of the MSWLF generally range from 297 to 625 milligrams per liter (wells JL-49-05-904 and JL-49-05-915, respectively).
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954217","collaboration":"Prepared in cooperation with the U.S. Department of the Army, U.S. Army Air Defense Artillery Center, and Fort Bliss","usgsCitation":"Abeyta, C.G., 1996, Geohydrologic site characterization of the municipal solid waste landfill facility, U.S. Army Air Defense Artillery Center and Fort Bliss, El Paso County, Texas: U.S. Geological Survey Water-Resources Investigations Report 95-4217, v, 36 p., https://doi.org/10.3133/wri954217.","productDescription":"v, 36 p.","costCenters":[],"links":[{"id":424453,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48305.htm","linkFileType":{"id":5,"text":"html"}},{"id":54622,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4217/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":119121,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4217/report-thumb.jpg"}],"country":"United States","state":"Texas","county":"El Paso County","otherGeospatial":"Fort Bliss","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -106.3972,\n 31.8847\n ],\n [\n -106.3972,\n 31.8764\n ],\n [\n -106.3883,\n 31.8764\n ],\n [\n -106.3883,\n 31.8847\n ],\n [\n -106.3972,\n 31.8847\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a8de2","contributors":{"authors":[{"text":"Abeyta, Cynthia G.","contributorId":52187,"corporation":false,"usgs":true,"family":"Abeyta","given":"Cynthia","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":195398,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28228,"text":"wri964102 - 1996 - Water-chemistry and chloride fluctuations in the Upper Floridan Aquifer in the Port Royal Sound area, South Carolina, 1917-93","interactions":[],"lastModifiedDate":"2019-12-30T12:57:52","indexId":"wri964102","displayToPublicDate":"1997-02-01T00:00:00","publicationYear":"1996","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":"96-4102","title":"Water-chemistry and chloride fluctuations in the Upper Floridan Aquifer in the Port Royal Sound area, South Carolina, 1917-93","docAbstract":"Withdrawal of water from the Upper Floridan aquifer south of Port Royal Sound in Beaufort and Jasper Counties, South Carolina, has lowered water levels and reversed the hydraulic gradient beneath Hilton Head Island, South Carolina. Ground water that had previously discharged at the Sound is now being deflected southwest, toward withdrawals located near the city of Savannah, Georgia, and the island of Hilton Head. The reversal of this hydraulic gradient and the decline of water levels have caused saltwater in the Upper Floridan aquifer north of Port Royal Sound to begin moving southwest, toward water-supply wells for the town of Hilton Head and toward industries pumping ground water near Savannah. Analytical results from ground-water samples collected from wells in the Upper Floridan aquifer beneath and adjacent to Port Royal Sound show two plumes in the aquifer with chloride concentrations above the drinking- water standard. One plume of high chloride concentration extends slightly south of the theoretical predevelopment location of the steady- state freshwater-saltwater interface as indicated by numerical modeling. The other plume is present beneath the town of Port Royal, where the upper confining unit above the Upper Floridan aquifer is thin or absent. In these areas, the decline in water levels caused by ground-water withdrawals may have made it possible for water from tidal creeks to enter the Upper Floridan aquifer. Many wells completed in the upper permeable zone of the Upper Floridan aquifer show a distinct specific- conductance profile. One non-producing, monitoring well on Hilton Head Island (BFT-1810) was selected to depict a worst-case scenario to examine the short- and long-term water-chemistry and chloride fluctuations in the aquifer. Specific conductance was monitored at depths of 170, 190, and 200 feet below the top of the well casing. The specific conductance measured in 1987 ranged from approximately 450 microsiemens per centimeter near the top of the Upper Floridan aquifer to 1,500 microsiemens per centimeter near the lower, less permeable zone. Short-term fluctuations in conductance were measured at each probe and were found to be related to water-level fluctuations in the well caused by tidal cycles. The conductance varied regularly up to 100 microsiemens per centimeter, with an increasing time lag between high and low tides and low and high specific conductance for progressively shallower depths. Well BFT-1810 was monitored for specific conductance and water levels from October 1987 through September 1993. Specific conductance at the 170-foot probe showed little long-term change, while the 190- and the 200-foot probes showed long-term increases to approximately 4,000 and 10,000 microsiemens per centimeter, respectively. This well is located closest to one of the two plumes of saltwater delineated in the Upper Floridan aquifer, and the long-term chloride increases are a result of the movement of saltwater in the Upper Floridan aquifer toward Hilton Head Island under the influence of regional ground-water withdrawals.","language":"English","publisher":"U.S. Geological Survey ","doi":"10.3133/wri964102","usgsCitation":"Landmeyer, J., and Belval, D., 1996, Water-chemistry and chloride fluctuations in the Upper Floridan Aquifer in the Port Royal Sound area, South Carolina, 1917-93: U.S. Geological Survey Water-Resources Investigations Report 96-4102, vii, 106 p., https://doi.org/10.3133/wri964102.","productDescription":"vii, 106 p.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":125017,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4102/report-thumb.jpg"},{"id":57059,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4102/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"South Carolina","otherGeospatial":"Port Royal Sound, Upper Floridan Aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.80419921875,\n 31.868227816180674\n ],\n [\n -79.34326171875,\n 31.868227816180674\n ],\n [\n -79.34326171875,\n 33.0178760185549\n ],\n [\n -81.80419921875,\n 33.0178760185549\n ],\n [\n -81.80419921875,\n 31.868227816180674\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cfe4b07f02db545b3f","contributors":{"authors":[{"text":"Landmeyer, J. E.","contributorId":91140,"corporation":false,"usgs":true,"family":"Landmeyer","given":"J. E.","affiliations":[],"preferred":false,"id":199428,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Belval, D.L.","contributorId":52186,"corporation":false,"usgs":true,"family":"Belval","given":"D.L.","affiliations":[],"preferred":false,"id":199427,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":30404,"text":"wri964154 - 1996 - Low-flow characteristics and profiles for selected streams in the Roanoke River basin, North Carolina","interactions":[],"lastModifiedDate":"2019-02-25T14:25:07","indexId":"wri964154","displayToPublicDate":"1997-02-01T00:00:00","publicationYear":"1996","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":"96-4154","title":"Low-flow characteristics and profiles for selected streams in the Roanoke River basin, North Carolina","docAbstract":"An understanding of the magnitude and frequency of low-flow discharges is an important part of protecting surface-water resources and planning for municipal and industrial economic expansion. Low-flow characteristics are summarized for 22 continuous-record gaging stations in North Carolina (19 sites) and Virginia (3 sites) and 60 partial-record gaging stations in the North Carolina Roanoke River Basin. Records of discharge collected through the 1994 water year are used. Flow characteristics included in the summary are (1) average annual unit flow, (2) 7Q10 low-flow discharge, the minimum average discharge for a 7 consecutive-day period occurring, on average, once in 10 years; (3) 30Q2 low-flow discharge; (4) W7Q10 low-flow discharge, similar to 7Q10 discharge except that flow during November through March only is considered; and (5) 7Q2 low-flow discharge. The potential for sustaining base flows is moderate to high in the western part of the basin as well as in the eastern and western fringes of the Piedmont and Coastal Plain physiographic provinces, respectively. Areas of low potential for sustaining base flow exist in the central part of the basin (between eastern Caswell County and western Warren County), where soils have low infiltration rates, and in lower regions of the Coastal Plain, where small streams tend to have zero flow during prolonged drought.
Drainage area and low-flow discharge profiles are presented for 10 streams in the Roanoke River Basin in North Carolina and reflect a wide range in basin size, characteristics, and streamflow conditions. The selected streams are Town Fork Creek, Hogans Creek, Mayo River, Buffalo Creek, Smith River, Country Line Creek, Dan River, Marlowe Creek, Hyco River, and Roanoke River. The drainage-area profiles show the increases in drainage areas as streams travel their course in the basin. At the mouths of streams profiled, the drainage areas range from 22 miles to about 9,700 miles. Low-flow discharges for each stream include 7Q10, 30Q2, W7Q10, and 7Q2 discharges in a continuous profile with contributions from major tributaries included.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964154","collaboration":"Prepared in cooperation with the Division of Environmental Management of the North Carolina Department of Environment, Health, and Natural Resources","usgsCitation":"Weaver, J.C., 1996, Low-flow characteristics and profiles for selected streams in the Roanoke River basin, North Carolina: U.S. Geological Survey Water-Resources Investigations Report 96-4154, Report: iv, 56 p.; 1 Plate: 23.40 x 12.37 inches, https://doi.org/10.3133/wri964154.","productDescription":"Report: iv, 56 p.; 1 Plate: 23.40 x 12.37 inches","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":126793,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4154/report-thumb.jpg"},{"id":59173,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4154/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":361507,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1996/4154/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"North Carolina","otherGeospatial":"Roanoke River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -83.71307373046874,\n 35.67068501330236\n ],\n [\n -83.71307373046874,\n 35.67068501330236\n ],\n [\n -83.7103271484375,\n 35.67068501330236\n ],\n [\n -83.7103271484375,\n 35.67068501330236\n ],\n [\n -83.71307373046874,\n 35.67068501330236\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.39593505859375,\n 35.833401703805094\n ],\n [\n -77.12677001953125,\n 35.69968630125204\n ],\n [\n -76.82601928710938,\n 35.71083783530009\n ],\n [\n -76.651611328125,\n 35.91685961322499\n ],\n [\n -76.77383422851562,\n 36.010228040656735\n ],\n [\n -77.04437255859375,\n 36.1312200154285\n ],\n [\n -77.41653442382812,\n 36.43896124085945\n ],\n [\n -77.56484985351562,\n 36.493077506552744\n ],\n [\n -78.3984375,\n 36.54053616262899\n ],\n [\n -79.40917968749999,\n 36.55377524336089\n ],\n [\n -80.37597656249999,\n 36.56260003738545\n ],\n [\n -80.32516479492188,\n 36.14896463588831\n ],\n [\n -79.76898193359375,\n 36.1312200154285\n ],\n [\n -79.46273803710938,\n 36.33393438759289\n ],\n [\n -79.12490844726562,\n 36.379279167407965\n ],\n [\n -79.03358459472656,\n 36.377620677623874\n ],\n [\n -78.89076232910156,\n 36.387571085823566\n ],\n [\n -78.83308410644531,\n 36.40359962073253\n ],\n [\n -77.39593505859375,\n 35.833401703805094\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a61e4b07f02db6358fd","contributors":{"authors":[{"text":"Weaver, J. Curtis 0000-0001-7068-5445 jcweaver@usgs.gov","orcid":"https://orcid.org/0000-0001-7068-5445","contributorId":2229,"corporation":false,"usgs":true,"family":"Weaver","given":"J.","email":"jcweaver@usgs.gov","middleInitial":"Curtis","affiliations":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true},{"id":476,"text":"North Carolina Water Science Center","active":true,"usgs":true}],"preferred":false,"id":203193,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":27703,"text":"wri964062 - 1996 - Hydrogeologic setting and simulation of pesticide fate and transport in the unsaturated zone of a regolith-mantled, carbonate-rock terrain near Newville, Pennsylvania","interactions":[],"lastModifiedDate":"2017-06-27T11:16:37","indexId":"wri964062","displayToPublicDate":"1997-02-01T00:00:00","publicationYear":"1996","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":"96-4062","title":"Hydrogeologic setting and simulation of pesticide fate and transport in the unsaturated zone of a regolith-mantled, carbonate-rock terrain near Newville, Pennsylvania","docAbstract":"Physical and chemical data were collected from May 1991 through April 1993 at a 4.5 hectare field site in Cumberland County, Pa., about 5 kilometers southeast of Newville. These data were used to define the hydrogeologic setting of a field site representative of the intensively farmed carbonate valleys of southeastern and south-central Pennsylvania. The environmental processing of commonly used pesticides (herbicides, fungicides, and insecticides) in the unsaturated zone was simulated with a process- oriented digital model to evaluate the environmental fate and transport of pesticides to ground water. Site data and modelling results provide a basis for a discussion of water-quality implications of agricultural best-management practices. The carbonate valleys of Pennsylvania comprise regolith-mantled carbonate-rock terrains that consist of broad undulating upland areas dissected by mostly dry valleys and widely spaced spring-fed creeks. The upland areas are farmed and exhibit possess a doline karst topography with many closed depressions, sinkholes, and bedrock outcrops. Unsaturated materials at the field site consist of an almost continuous soil cover composed of fine-grained residuum underlain by an intermediate vadose zone composed of karstified limestone. Soils are absent on scattered bedrock outcrops and are more than 12 meters thick in other areas of the site. The soil profile stores appreciable quantities of water with a volumetric average of about 36 percent water at field capacity. Organic carbon content of soil materials is about 1.7 percent in the Ap-horizon and from 0.1 to 0.3 percent throughout the full thickness of the B- and C-horizons. Atrazine, metolachlor, simazine, and the atrazine soil metabolites deethylatrazine and deisopropylatrazine were detected at concentrations above 0.05 mg/L in just the upper 0.6 meters of soil materials. However, detectable concentrations of atrazine, simazine, and atrazine soil metabolites were measured in water samples from lysimeters installed in soil materials at depths of 1.2, 2.1, and 3.7 meters and from monitor wells completed in the saturated zone to depths of 122 meters. Data collected from the field site were used to configure a pesticide screening model based on the pesticide version of the leaching estimation and chemistry model (LEACHP) developed by Wagenet and Hutson (1987). Model simulations show that most field-applied pesticides volatilize to the atmosphere, accumulate in soils, degrade in the subsurface environment, or leach to ground water. Model results were used to rank the leaching potentials of 66 pesticides. Eighteen of 32 herbicides, 4 of 9 fungicides, and 10 of 25 insecticides have moderate to large potential for leaching to ground water. A review of available pesticide monitoring data suggests that many compounds given moderate or high leaching potentials have not been tested for in ground water and the presence of pesticides in Pennsylvania's ground water may be underreported. Monitoring data do not exist for more than two-thirds of the pesticide compounds currently used in agricultural, carbonate areas of Pennsylvania. Knowledge of processes that govern fate and transport of pesticides is needed to facilitate development of effective pesticide best-management practices. In addition to comprehensive monitoring for pesticides and pesticide degradation products in ground water downgradient of areas of pesticide use, improved (1) characterization of unsaturated flow and transport through regolith mantled carbonate rocks, (2) estimates of pesticide degradation rates, (3) understanding of soil-property controls on pesticide movement, and (4) management models developed from process-oriented research would aid in understanding the processes.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964062","usgsCitation":"Hippe, D., and Hall, D.W., 1996, Hydrogeologic setting and simulation of pesticide fate and transport in the unsaturated zone of a regolith-mantled, carbonate-rock terrain near Newville, Pennsylvania: U.S. Geological Survey Water-Resources Investigations Report 96-4062, vi, 56 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri964062.","productDescription":"vi, 56 p. :ill., maps ;28 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":56550,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4062/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124030,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4062/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ee4b07f02db62793f","contributors":{"authors":[{"text":"Hippe, D. J.","contributorId":83951,"corporation":false,"usgs":true,"family":"Hippe","given":"D. J.","affiliations":[],"preferred":false,"id":198561,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hall, D. W.","contributorId":106528,"corporation":false,"usgs":true,"family":"Hall","given":"D.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":198562,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2979,"text":"wsp2469 - 1996 - Lake-level frequency analysis for Devils Lake, North Dakota","interactions":[],"lastModifiedDate":"2018-03-13T13:49:59","indexId":"wsp2469","displayToPublicDate":"1997-02-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2469","title":"Lake-level frequency analysis for Devils Lake, North Dakota","docAbstract":"Two approaches were used to estimate future lake-level probabilities for Devils Lake. The first approach is based on an annual lake-volume model, and the second approach is based on a statistical water mass-balance model that generates seasonal lake volumes on the basis of seasonal precipitation, evaporation, and inflow.
Autoregressive moving average models were used to model the annual mean lake volume and the difference between the annual maximum lake volume and the annual mean lake volume. Residuals from both models were determined to be uncorrelated with zero mean and constant variance. However, a nonlinear relation between the residuals of the two models was included in the final annual lakevolume model.
Because of high autocorrelation in the annual lake levels of Devils Lake, the annual lake-volume model was verified using annual lake-level changes. The annual lake-volume model closely reproduced the statistics of the recorded lake-level changes for 1901-93 except for the skewness coefficient. However, the model output is less skewed than the data indicate because of some unrealistically large lake-level declines.
The statistical water mass-balance model requires as inputs seasonal precipitation, evaporation, and inflow data for Devils Lake. Analysis of annual precipitation, evaporation, and inflow data for 1950-93 revealed no significant trends or long-range dependence so the input time series were assumed to be stationary and short-range dependent.
Normality transformations were used to approximately maintain the marginal probability distributions; and a multivariate, periodic autoregressive model was used to reproduce the correlation structure. Each of the coefficients in the model is significantly different from zero at the 5-percent significance level. Coefficients relating spring inflow from one year to spring and fall inflows from the previous year had the largest effect on the lake-level frequency analysis.
Inclusion of parameter uncertainty in the model for generating precipitation, evaporation, and inflow indicates that the upper lake-level exceedance levels from the water mass-balance model are particularly sensitive to parameter uncertainty. The sensitivity in the upper exceedance levels was caused almost entirely by uncertainty in the fitted probability distributions of the quarterly inflows. A method was developed for using long-term streamflow data for the Red River of the North at Grand Forks to reduce the variance in the estimated mean.
Comparison of the annual lake-volume model and the water mass-balance model indicates the upper exceedance levels of the water mass-balance model increase much more rapidly than those of the annual lake-volume model. As an example, for simulation year 5, the 99-percent exceedance for the lake level is 1,417.6 feet above sea level for the annual lake-volume model and 1,423.2 feet above sea level for the water mass-balance model. The rapid increase is caused largely by the record precipitation and inflow in the summer and fall of 1993. Because the water mass-balance model produces lake-level traces that closely match the hydrology of Devils Lake, the water mass-balance model is superior to the annual lake-volume model for computing exceedance levels for the 50-year planning horizon.
The U.S. Geological Survey investigated ground-water resources of northeastern St. Joseph County, Indiana, during 1990-93. The investigation included field measurements of water levels and numerical models of ground-water flow. This report documents results of that work and includes descriptions of (1) hydrogeologic framework, (2) water levels, (3) model sensitivity to variations in hydrogeologic parameters, (4) simulated aquifer response to increased ground-water withdrawals, (5) recharge areas for significant water- withdrawal facilities, (6) flow paths and discharge points for ground-water solutes originating beneath known contamination sites. Water-level data indicated (1) regional ground- water flow towards the St. Joseph River, (2) depth to water is small in the St. Joseph aquifer system compared to that in the Hilltop and Nappanee aquifer systems, (3) water levels in deep and shallow parts of the aquifer system are not equal where a confining unit is present. Model results indicate increasing withdrawals by 50 percent at significant water-withdrawal facilities would cause drawdowns less than 6 feet in the 1/4-square-mile area surrounding pumping sites. The response of Juday Creek and the St. Joseph River to increased ground-water pumpage is reductions of ground-water contribution to streamflow of 23 percent and 6 percent, respectively. Particle-tracking analyses indicate flow paths for solutes originating beneath known contamination sites may pass near to, or be intercepted by, significant water-withdrawal facilities. Most particles are discharged to the St. Joseph River but some may be discharged to Juday Creek.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954225","usgsCitation":"Bayless, E.R., and Arihood, L.D., 1996, Hydrogeology and simulated ground-water flow through the unconsolidated aquifers of northeastern St. Joseph County, Indiana: U.S. Geological Survey Water-Resources Investigations Report 95-4225, v, 47 p. : ill., maps ; 28 cm., https://doi.org/10.3133/wri954225.","productDescription":"v, 47 p. : ill., maps ; 28 cm.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":54922,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4225/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123519,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4225/report-thumb.jpg"}],"country":"United States","state":"Indiana","county":"Saint Joseph","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-86.2255,41.7615],[-86.0624,41.7619],[-86.0598,41.4999],[-86.0592,41.4935],[-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],[-86.4526,41.7599],[-86.2846,41.7611],[-86.2255,41.7615]]]},\"properties\":{\"name\":\"Saint Joseph\",\"state\":\"IN\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ae4b07f02db625295","contributors":{"authors":[{"text":"Bayless, E. Randall 0000-0002-0357-3635","orcid":"https://orcid.org/0000-0002-0357-3635","contributorId":42586,"corporation":false,"usgs":true,"family":"Bayless","given":"E.","email":"","middleInitial":"Randall","affiliations":[{"id":35860,"text":"Ohio-Kentucky-Indiana Water Science Center","active":true,"usgs":true}],"preferred":true,"id":195846,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Arihood, L. D. 0000-0001-5792-3699","orcid":"https://orcid.org/0000-0001-5792-3699","contributorId":74388,"corporation":false,"usgs":true,"family":"Arihood","given":"L.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":195847,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}