The stage of Lake Brooklyn, in southwestern Clay County, Florida, has varied over a range of 27 feet since measurements by the U.S. Geological Survey began in July 1957. The large stage changes have been attributed to the relation between highly transient surface-water inflow to the lake and subsurface conduits of karstic origin that permit a high rate of leakage from the lake to the Upper Floridan aquifer. After the most recent and severe stage decline (1990-1994), the U.S. Geological Survey began a study that entailed the use of numerical ground-water flow models to simulate the interaction of the lake with the Upper Floridan aquifer and the large fluctuations of stage that were a part of that process. A package (set of computer programs) designed to represent lake/aquifer interaction in the U.S. Geological Survey Modular Finite-Difference Ground-Water Flow Model (MODFLOW-96) and the Three-Dimensional Method-of-Characteristics Solute-Transport Model (MOC3D) simulators was prepared as part of this study, and a demonstration of its capability was a primary objective of the study. (Although the official names are Brooklyn Lake and Magnolia Lake (Florida Geographic Names), in this report the local names, Lake Brooklyn and Lake Magnolia, are used.)
In the simulator of lake/aquifer interaction used in this investigation, the stage of each lake in a simulation is updated in successive time steps by a budget process that takes into account ground-water seepage, precipitation upon and evaporation from the lake surface, stream inflows and outflows, overland runoff inflows, and augmentation or depletion by artificial means. The simulator was given the capability to simulate both the division of a lake into separate pools as lake stage falls and the coalescence of several pools into a single lake as the stage rises. This representational capability was required to simulate Lake Brooklyn, which can divide into as many as 10 separate pools at sufficiently low stage.
In the first of two calibrated models, recharge to the water table, specified as a monthly rate, was set equal to 40 percent of the monthly rainfall rate. The specified rate of inflow to the uppermost stream segment was set equal to outflows from Lake Lowry estimated from lake stage and the 1994-97 rating table. Leakage to the intermediate and Upper Floridan aquifers was assumed to occur from the surficial aquifer system through the confining layers directly beneath deeper parts of the lake bottom. A leakance coefficient value of 0.001 feet per day per foot of thickness was used beneath Lake Magnolia, and a value of 0.005 feet per day per foot of thickness was used beneath most of Lake Brooklyn. With these values, the conductance through the confining layers beneath Lake Brooklyn was about 19 times that beneath Lake Magnolia.
The simulated stages of Lake Brooklyn matched the measured stages reasonably well in the early (1957-72) and later (1990-98) parts of the simulation time period, but the match was unsatisfactory in an intermediate time period (1973-89). To resolve this discrepancy, the hypothesis was proposed that undocumented losses of water from Alligator Creek upstream from Lake Brooklyn or from the lake itself occurred between 1973 and 1989 when there was sufficient streamflow. The resulting simulation of lake stages matched the measured lake stages accurately during the entire simulation time period. The model was then revised to incorporate the assumption that only 20 percent of precipitation recharged the water table (the second calibrated model). Recalibration of the model required that leakance values for the confining units under deeper parts of the lakes also be reduced by nearly 50 percent. The stages simulated with the new parameter assumptions, but retaining the assumption of surface-water losses, were an excellent match of the measured values. The stage of Lake Magnolia was also simulated accurately. The results of sensitivity analyses show that simulated streamflow between Lakes Magnolia and Brooklyn tends to be water-budget controlled, and is not appreciably affected by the specified outflow altitude or channel characteristics of the receiving stream.
To match heads measured in observation wells of the surficial aquifer network, the assigned hydraulic conductivity values were zoned, and ranged from a minimum of 4 feet per day to a maximum of 400 feet per day in the first calibrated model. These values were reduced by about 50 percent in the second calibrated model. Differences between observation wells were noted in the abruptness of changes of measured head values, and in the relation of the timing of peak measured heads and simulated peak heads. These differences seemed to be correlated with the depth of the water table below land surface. Spatially uniform values of transmissivity were specified for the intermediate (10,000 feet squared per day) and Upper Floridan (100,000 feet squared per day) aquifers. Simulated heads in the Upper Floridan aquifer layer follow the trend of the heads measured in a long-term observation well with data beginning in 1960. This result suggests that the observed head decline could be explained entirely in terms of the stage decline in Lake Brooklyn and may not indicate a regional trend.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004204","usgsCitation":"Merritt, M.L., 2001, Simulation of the interaction of karstic lakes Magnolia and Brooklyn with the upper Floridan Aquifer, southwestern Clay County, Florida: U.S. Geological Survey Water-Resources Investigations Report 2000-4204, vi, 62 p., https://doi.org/10.3133/wri004204.","productDescription":"vi, 62 p.","costCenters":[],"links":[{"id":161469,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":415188,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_37335.htm","linkFileType":{"id":5,"text":"html"}},{"id":2785,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri00-4204/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Florida","county":"Clay County","otherGeospatial":"Lake Brooklyn, Lake Magnolila","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -82.0833,\n 29.833\n ],\n [\n -82.0833,\n 29.783\n ],\n [\n -82,\n 29.783\n ],\n [\n -82,\n 29.833\n ],\n [\n -82.0833,\n 29.833\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f7e4b07f02db5f1fcd","contributors":{"authors":[{"text":"Merritt, M. L.","contributorId":47401,"corporation":false,"usgs":true,"family":"Merritt","given":"M.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":204252,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":30904,"text":"wri014035 - 2001 - Hydrogeology, model description, and flow analysis of the Mississippi River alluvial aquifer in northwestern Mississippi","interactions":[],"lastModifiedDate":"2018-03-29T08:27:01","indexId":"wri014035","displayToPublicDate":"2001-08-01T00:00:00","publicationYear":"2001","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":"2001-4035","title":"Hydrogeology, model description, and flow analysis of the Mississippi River alluvial aquifer in northwestern Mississippi","docAbstract":"The Mississippi River alluvial aquifer underlies a 7,000-square-mile area of the Mississippi River alluvial plain in northwestern Mississippi, an area locally known as the Delta. The alluvial aquifer is the most heavily pumped aquifer in Mississippi, and wells yielding more than 2,000 gallons per minute are common. About 98 percent of the pumpage from the alluvial aquifer is for agriculture. The sand and gravel that form the alluvial aquifer averages about 110 feet in thickness. The aquifer is confined over most of the Delta, and the upper confining unit averages about 25 feet in thickness. The average depth to water in the alluvial aquifer during fall 1999 was about 25 feet. The alluvial aquifer receives lateral recharge at the western boundary from the Mississippi River and at the eastern boundary from aquifers that directly underlie the Bluff Hills. The alluvial aquifer receives water vertically from precipitation, internal streams and lakes, and locally from the Cockfield and Sparta aquifers where they directly underlie the alluvial aquifer. The alluvial aquifer also discharges water to the underlying aquifers, and during extended periods with no surface runoff, to the Mississippi River and to the internal streams and lakes. The magnitude of recharge from the Mississippi River, precipitation, and internal lakes and streams can vary greatly depending upon hydrologic and climatic conditions. The U.S. Geological Survey modular threedimensional finite-difference ground-water flow model, MODFLOW, was used to simulate the Mississippi River alluvial aquifer flow system in northwestern Mississippi. The model uses one layer with a rectangular-grid and 1-mile square cells to represent the alluvial aquifer. The model was calibrated and verified by using spring and fall water-level measurements from January 1988 through December 1996. The values of selected model calibration-derived parameters for the alluvial aquifer are hydraulic conductivity, 425 feet per day; specific yield, 0.32; and storage coefficient, 0.016. The model showed that the aquifer lost water from storage at an average rate of 404 cubic feet per second during the 9-year simulation period. During this period, the average pumpage rate was 1,270 million gallons per day (1,980 cubic feet per second). Simulated areal recharge from precipitation averaged 2.6 inches per year (1,360 cubic feet per second). Vertical recharge from the internal streams and lakes and lateral recharge from aquifers underlying the Bluff Hills averaged 113 and 108 cubic feet per second, respectively. Model results indicated that net recharge from the Mississippi River and from aquifers directly underlying the alluvial aquifer was small. ","language":"English","doi":"10.3133/wri014035","usgsCitation":"Arthur, J.K., 2001, Hydrogeology, model description, and flow analysis of the Mississippi River alluvial aquifer in northwestern Mississippi: U.S. Geological Survey Water-Resources Investigations Report 2001-4035, 47 p., https://doi.org/10.3133/wri014035.","productDescription":"47 p.","costCenters":[],"links":[{"id":160835,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":352893,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://permanent.access.gpo.gov/LPS104393/LPS104393/ms.water.usgs.gov/ms_proj/reports/WRIR_01-4035.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":2839,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://ms.water.usgs.gov/ms_proj/reports/WRIR_01-4035.pdf ","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Mississippi","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.263671875,\n 35.06597313798418\n ],\n [\n -90.7470703125,\n 34.903952965590065\n ],\n [\n -91.25244140624999,\n 33.99802726234877\n ],\n [\n -91.40625,\n 33.00866349457558\n ],\n [\n -91.16455078125,\n 32.24997445586331\n ],\n [\n -90.81298828125,\n 32.30570601389429\n ],\n [\n -90.966796875,\n 33.43144133557529\n ],\n [\n -90.90087890624999,\n 33.90689555128866\n ],\n [\n -90.59326171875,\n 34.27083595165\n ],\n [\n -90.263671875,\n 35.06597313798418\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e479fe4b07f02db492f52","contributors":{"authors":[{"text":"Arthur, J. K.","contributorId":56223,"corporation":false,"usgs":true,"family":"Arthur","given":"J.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":204326,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70171268,"text":"70171268 - 2001 - Hydrogeologic conditions in the upper aquifer of Puerto Rico, Manatí-Vega Baja area, as simulated by U.S. Geological Survey Modflow 96","interactions":[],"lastModifiedDate":"2016-06-02T12:57:00","indexId":"70171268","displayToPublicDate":"2001-02-13T09:15:00","publicationYear":"2001","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Hydrogeologic conditions in the upper aquifer of Puerto Rico, Manatí-Vega Baja area, as simulated by U.S. Geological Survey Modflow 96","largerWorkType":{"id":24,"text":"Conference Paper"},"largerWorkTitle":"Proceedings of the Sixth Caribbean Islands Water Resources Congress","largerWorkSubtype":{"id":19,"text":"Conference Paper"},"conferenceTitle":"Sixth Caribbean Islands Water Resources Congress","conferenceDate":"February 2001","conferenceLocation":"Mayagüez, Puerto Rico","language":"English","publisher":"U.S. Dept. of the Interior, Geological Survey","usgsCitation":"Cherry, G., 2001, Hydrogeologic conditions in the upper aquifer of Puerto Rico, Manatí-Vega Baja area, as simulated by U.S. Geological Survey Modflow 96, in Proceedings of the Sixth Caribbean Islands Water Resources Congress, Mayagüez, Puerto Rico, February 2001, 47 p.","productDescription":"47 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":156,"text":"Caribbean Water Science Center","active":true,"usgs":true}],"links":[{"id":321713,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":322095,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://www.uvi.edu/files/documents/Research_and_Public_Service/WRRI/Sixth_Water_Congress.pdf","text":"Table of Contents","size":"666kb","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57481e34e4b07e28b664dbc2","contributors":{"authors":[{"text":"Cherry, G.S.","contributorId":23576,"corporation":false,"usgs":true,"family":"Cherry","given":"G.S.","email":"","affiliations":[],"preferred":false,"id":630374,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":45064,"text":"wri004251 - 2001 - Simulation of ground-water discharge to Biscayne Bay, southeastern Florida","interactions":[],"lastModifiedDate":"2022-01-04T18:43:24.622742","indexId":"wri004251","displayToPublicDate":"2001-01-01T21:40:00","publicationYear":"2001","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":"2000-4251","displayTitle":"Simulation of Ground-Water Discharge to Biscayne Bay, Southeastern Florida","title":"Simulation of ground-water discharge to Biscayne Bay, southeastern Florida","docAbstract":"As part of the Place-Based Studies Program, the U.S. Geological Survey initiated a project in 1996, in cooperation with the U.S. Army Corps of Engineers, to quantify the rates and patterns of submarine ground-water discharge to Biscayne Bay. Project objectives were achieved through field investigations at three sites (Coconut Grove, Deering Estate, and Mowry Canal) along the coastline of Biscayne Bay and through the development and calibration of variable-density, ground-water flow models. Two-dimensional, vertical cross-sectional models were developed for steady-state conditions for the Coconut Grove and Deering Estate transects to quantify local-scale ground-water discharge patterns to Biscayne Bay. A larger regional-scale model was developed in three dimensions to simulate submarine ground-water discharge to the entire bay. The SEAWAT code, which is a combined version of MODFLOW and MT3D, was used to simulate the complex variable-density flow patterns. Field data suggest that ground-water discharge to Biscayne Bay relative to the shoreline is restricted to within 300 meters at Coconut Grove, 600 to 1,000 meters at Deering Estate, and 100 meters at Mowry Canal. The vertical cross-sectional models, which were calibrated to the field data using the assumption of steady state, tend to focus ground-water discharge to within 50 to 200 meters of the shoreline. With homogeneous distributions for aquifer parameters and a constant-concentration boundary for Biscayne Bay, the numerical models could not reproduce the lower ground-water salinities observed beneath the bay, which suggests that further research may be necessary to improve the accuracy of the numerical simulations. Results from the cross-sectional models, which were able to simulate the approximate position of the saltwater interface, suggest that longitudinal dispersivity ranges between 1 and 10 meters, and transverse dispersivity ranges from 0.1 to 1 meter for the Biscayne aquifer. The three-dimensional, regional-scale model was calibrated to ground-water heads, canal baseflow, and the general position of the saltwater interface for nearly a 10-year period from 1989 to 1998. The mean absolute error between observed and simulated head values is 0.15 meter. The mean absolute error between observed and simulated baseflow is 3 x 105 cubic meters per day. The position of the simulated saltwater interface generally matches the position observed in the field, except for areas north of the Miami Canal where the simulated saltwater interface is located about 5 kilometers inland of the observed saltwater interface. Results from the regional-scale model suggest that the average rate of fresh ground-water discharge to Biscayne Bay for the 10-year period (1989-98) is about 2 x 105 cubic meters per day for 100 kilometers of coastline. This simulated discharge rate is about 6 percent of the measured surface-water discharge to Biscayne Bay for the same period. The model also suggests that nearly 100 percent of the fresh ground-water discharge is to the northern half of Biscayne Bay, north of the Cutler Drain Canal. South of the Cutler Drain Canal, coastal lowlands prevent the water table from rising high enough to drive measurable quantities of ground water to Biscayne Bay. Annual variations in sea-level elevation, which can be as large as 0.3 meter, have a substantial effect on rates of ground-water discharge. During 1989-98, simulated rates of ground-water discharge to Biscayne Bay generally are highest when sea level is relatively low.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri004251","collaboration":"Prepared in cooperation with the U.S. Army Corps of Engineers","usgsCitation":"Langevin, C.D., 2001, Simulation of ground-water discharge to Biscayne Bay, southeastern Florida: U.S. Geological Survey Water-Resources Investigations Report 2000-4251, Report: vi, 127 p.; 3 Plates: 8.5 x 11 in, https://doi.org/10.3133/wri004251.","productDescription":"Report: vi, 127 p.; 3 Plates: 8.5 x 11 in","costCenters":[{"id":27821,"text":"Caribbean-Florida Water Science Center","active":true,"usgs":true}],"links":[{"id":99370,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2000/4251/wri004251_plate3.pdf","text":"Plate 3","size":"1.06 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 3"},{"id":99369,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2000/4251/wri004251_plate2.pdf","text":"Plate 2","size":"0.98 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 2"},{"id":167923,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4251/report-thumb.jpg"},{"id":99367,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4251/wri004251.pdf","text":"Report","size":"8.79 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":99368,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/2000/4251/wri004251_plate1.pdf","text":"Plate 1","size":"820 KB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"}],"country":"United States","state":"Florida","otherGeospatial":"Biscayne Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.134033203125,\n 25.44823489808649\n ],\n [\n -80.255126953125,\n 25.030861410390447\n ],\n [\n -80.03814697265625,\n 26.125850185680356\n ],\n [\n -80.79620361328125,\n 26.480407161007275\n ],\n [\n -81.134033203125,\n 25.44823489808649\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
A steady-state finite difference model was developed to simulate ground-water flow in four regional aquifers in Michigan’s Lower Peninsula. The Glaciofluvial, Saginaw, Parma-Bayport, and Marshall aquifers were simulated as layers 1 through 4, respectively, in the model. Separately calculated vertical conductances input to the model were used to simulate the intervening Till/“Red Beds”, Saginaw, and Michigan confining units, respectively. The model domain was laterally bound by a continuous specifiedhead boundary, formed from Lakes Michigan, Huron, St. Clair, and Erie, together with the St. Clair and Detroit River connecting channels.
The model was developed to quantify regional ground-water flow in the aquifer systems using independently determined recharge estimates. The flow model showed that groundwater heads and flows in the Glaciofluvial aquifer are controlled by local stream stages and discharges, resulting in localized flow cells accounting for 95-percent of the overall model water budget. Simulation of recharge to an unspecified water table also enabled the estimation of ground-water discharge to three Great Lakes.
A computer diskette contains all MODFLOW and MODFLOWP input files, as well as digital model surfaces and several Fortran processing routines used to construct the surfaces. The diskette also provides the data used for calibration and sensitivity analysis.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr00504","usgsCitation":"Hoaglund, J.R., Huffman, G., and Granneman, N., 2000, Simulation of ground water flow in the Glaciofluvial, Saginaw, Parma-Bayport, and Marshall Aquifers, Central Lower Peninsula of Michigan: U.S. Geological Survey Open-File Report 2000-504, iv, 36 p., https://doi.org/10.3133/ofr00504.","productDescription":"iv, 36 p.","numberOfPages":"36","costCenters":[],"links":[{"id":392379,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2000/0504/ofr00504.pdf","text":"Report","size":"4.73 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 00-504"},{"id":176862,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2000/0504/coverthb2.jpg"}],"country":"United States","state":"Michigan","otherGeospatial":"Saginaw, Parma-Bayport, and Marshall Aquifers","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -86.3525390625,\n 42.13082130188811\n ],\n [\n -83.3203125,\n 42.13082130188811\n ],\n [\n -83.3203125,\n 44.11914151643737\n ],\n [\n -86.3525390625,\n 44.11914151643737\n ],\n [\n -86.3525390625,\n 42.13082130188811\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7ee4b07f02db648545","contributors":{"authors":[{"text":"Hoaglund, John Robert III","contributorId":13685,"corporation":false,"usgs":true,"family":"Hoaglund","given":"John","suffix":"III","email":"","middleInitial":"Robert","affiliations":[],"preferred":false,"id":241296,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Huffman, G.C.","contributorId":44150,"corporation":false,"usgs":true,"family":"Huffman","given":"G.C.","email":"","affiliations":[],"preferred":false,"id":241298,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Granneman, N.J.","contributorId":32978,"corporation":false,"usgs":true,"family":"Granneman","given":"N.J.","email":"","affiliations":[],"preferred":false,"id":241297,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":22328,"text":"ofr00342 - 2000 - MODFLOW-2000, the U.S. Geological Survey Modular Ground-Water Model -Documentation of the Hydrogeologic-Unit Flow (HUF) Package","interactions":[],"lastModifiedDate":"2017-07-14T10:13:29","indexId":"ofr00342","displayToPublicDate":"2002-03-01T00:00:00","publicationYear":"2000","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":"2000-342","title":"MODFLOW-2000, the U.S. Geological Survey Modular Ground-Water Model -Documentation of the Hydrogeologic-Unit Flow (HUF) Package","docAbstract":"This report documents the Hydrogeologic-Unit Flow (HUF) Package for the groundwater\r\nmodeling computer program MODFLOW-2000. The HUF Package is an alternative\r\ninternal flow package that allows the vertical geometry of the system hydrogeology to be defined\r\nexplicitly within the model using hydrogeologic units that can be different than the definition of\r\nthe model layers. The HUF Package works with all the processes of MODFLOW-2000. For the\r\nGround-Water Flow Process, the HUF Package calculates effective hydraulic properties for the\r\nmodel layers based on the hydraulic properties of the hydrogeologic units, which are defined by\r\nthe user using parameters. The hydraulic properties are used to calculate the conductance\r\ncoefficients and other terms needed to solve the ground-water flow equation. The sensitivity of\r\nthe model to the parameters defined within the HUF Package input file can be calculated using\r\nthe Sensitivity Process, using observations defined with the Observation Process. Optimal values\r\nof the parameters can be estimated by using the Parameter-Estimation Process. The HUF\r\nPackage is nearly identical to the Layer-Property Flow (LPF) Package, the major difference being\r\nthe definition of the vertical geometry of the system hydrogeology. Use of the HUF Package is\r\nillustrated in two test cases, which also serve to verify the performance of the package by\r\nshowing that the Parameter-Estimation Process produces the true parameter values when exact\r\nobservations are used.","language":"English","publisher":"U.SU.S. Geological Survey","publisherLocation":"Denver, CO ","doi":"10.3133/ofr00342","issn":"0094-9140","usgsCitation":"Anderman, E., and Hill, M.C., 2000, MODFLOW-2000, the U.S. Geological Survey Modular Ground-Water Model -Documentation of the Hydrogeologic-Unit Flow (HUF) Package: U.S. Geological Survey Open-File Report 2000-342, vi, 89 p. :ill. ;28 cm., https://doi.org/10.3133/ofr00342.","productDescription":"vi, 89 p. :ill. ;28 cm.","costCenters":[],"links":[{"id":51737,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2000/0342/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":1415,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://water.usgs.gov/nrp/gwsoftware/modflow2000/ofr00-342.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":155944,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2000/0342/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db648c90","contributors":{"authors":[{"text":"Anderman, E.R.","contributorId":62241,"corporation":false,"usgs":true,"family":"Anderman","given":"E.R.","affiliations":[],"preferred":false,"id":188048,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hill, M. C.","contributorId":48993,"corporation":false,"usgs":true,"family":"Hill","given":"M.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":188047,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":25769,"text":"wri004268 - 2000 - Simulation of projected water demand and ground-water levels in the Coffee Sand and Eutaw-McShan aquifers in Union County, Mississippi, 2010 through 2050","interactions":[],"lastModifiedDate":"2012-02-02T00:08:23","indexId":"wri004268","displayToPublicDate":"2001-09-01T00:00:00","publicationYear":"2000","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":"2000-4268","title":"Simulation of projected water demand and ground-water levels in the Coffee Sand and Eutaw-McShan aquifers in Union County, Mississippi, 2010 through 2050","docAbstract":"Ground water from the Eutaw-McShan and the Coffee Sand aquifers is the major source of supply for residential, commercial, and industrial purposes in Union County, Mississippi. Unbiased, scientifically sound data and assessments are needed to assist agencies in better understanding and managing available water resources as continuing development and growth places more stress on available resources. The U.S. Geological Survey, in cooperation with the Tennessee Valley Authority, conducted an investigation using water-demand and ground-water models to evaluate the effect of future water demand on groundwater levels. Data collected for the 12 public-supply facilities and the self-supplied commercial and industrial facilities in Union County were used to construct water-demand models. The estimates of water demand to year 2050 were then input to a ground-water model based on the U.S. Geological Survey finite-difference computer code, MODFLOW. Total ground-water withdrawals for Union County in 1998 were estimated as 2.85 million gallons per day (Mgal/d). Of that amount, municipal withdrawals were 2.55 Mgal/d with about 1.50 Mgal/d (59 percent) delivered to residential users. Nonmunicipal withdrawals were 0.296 Mgal/d. About 80 percent (2.27 Mgal/d) of the total ground-water withdrawal is produced from the Eutaw-McShan aquifer and about 13 percent (0.371 Mgal/d) from the Coffee Sand aquifer. Between normal- and high-growth conditions, total water demand could increase from 72 to 131 percent (2.9 Mgal/d in 1998 to 6.7 Mgal/d in year 2050) with municipal demand increasing from 77 to 146 percent (2.6 to 6.4 Mgal/d). Increased pumping to meet the demand for water was simulated to determine the effect on water levels in the Coffee Sand and Eutaw- McShan aquifers. Under baseline-growth conditions, increased water use by year 2050 could result in an additional 65 feet of drawdown in the New Albany area below year 2000 water levels in the Coffee Sand aquifer and about 120 feet of maximum drawdown in the Eutaw-McShan aquifer. Under normal-growth conditions, increased water use could result in an additional 65 feet of drawdown in the New Albany area below year 2000 water levels in the Coffee Sand aquifer and about 135 feet of maximum drawdown in the Eutaw-McShan aquifer. Under high-growth conditions, increased water use could result in 75 feet of drawdown in the New Albany area below year 2000 water levels in the Coffee Sand aquifer and about 190 feet of maximum drawdown in the Eutaw-McShan aquifer. The resulting highgrowth projected water level for the year 2050 at the center of the drawdown cone in the New Albany area is between 450 and 500 feet above the top of the Eutaw-McShan aquifer. ","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/wri004268","usgsCitation":"Hutson, S.S., Strom, E.W., Burt, D., and Mallory, M.J., 2000, Simulation of projected water demand and ground-water levels in the Coffee Sand and Eutaw-McShan aquifers in Union County, Mississippi, 2010 through 2050: U.S. Geological Survey Water-Resources Investigations Report 2000-4268, v, 36 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri004268.","productDescription":"v, 36 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":1875,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri004268","linkFileType":{"id":5,"text":"html"}},{"id":157798,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f7e4b07f02db5f223a","contributors":{"authors":[{"text":"Hutson, Susan S. sshutson@usgs.gov","contributorId":2040,"corporation":false,"usgs":true,"family":"Hutson","given":"Susan","email":"sshutson@usgs.gov","middleInitial":"S.","affiliations":[{"id":374,"text":"Maryland Water Science Center","active":true,"usgs":true}],"preferred":true,"id":194994,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Strom, E. W.","contributorId":90776,"corporation":false,"usgs":true,"family":"Strom","given":"E.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":194997,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Burt, D.E.","contributorId":65885,"corporation":false,"usgs":true,"family":"Burt","given":"D.E.","affiliations":[],"preferred":false,"id":194996,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mallory, M. J.","contributorId":10398,"corporation":false,"usgs":true,"family":"Mallory","given":"M.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":194995,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":28696,"text":"wri004167 - 2000 - Documentation of a computer program to simulate lake-aquifer interaction using the MODFLOW ground water flow model and the MOC3D solute-transport model","interactions":[],"lastModifiedDate":"2020-02-26T19:11:38","indexId":"wri004167","displayToPublicDate":"2001-09-01T00:00:00","publicationYear":"2000","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":"2000-4167","title":"Documentation of a computer program to simulate lake-aquifer interaction using the MODFLOW ground water flow model and the MOC3D solute-transport model","docAbstract":"Heads and flow patterns in surficial aquifers can be strongly influenced by the presence of stationary surface-water bodies (lakes) that are in direct contact, vertically and laterally, with the aquifer. Conversely, lake stages can be significantly affected by the volume of water that seeps through the lakebed that separates the lake from the aquifer. For these reasons, a set of computer subroutines called the Lake Package (LAK3) was developed to represent lake/aquifer interaction in numerical simulations using the U.S. Geological Survey three-dimensional, finite-difference, modular ground-water flow model MODFLOW and the U.S. Geological Survey three-dimensional method-of-characteristics solute-transport model MOC3D. In the Lake Package described in this report, a lake is represented as a volume of space within the model grid which consists of inactive cells extending downward from the upper surface of the grid. Active model grid cells bordering this space, representing the adjacent aquifer, exchange water with the lake at a rate determined by the relative heads and by conductances that are based on grid cell dimensions, hydraulic conductivities of the aquifer material, and user-specified leakance distributions that represent the resistance to flow through the material of the lakebed. Parts of the lake may become ?dry? as upper layers of the model are dewatered, with a concomitant reduction in lake surface area, and may subsequently rewet when aquifer heads rise. An empirical approximation has been encoded to simulate the rewetting of a lake that becomes completely dry. The variations of lake stages are determined by independent water budgets computed for each lake in the model grid. This lake budget process makes the package a simulator of the response of lake stage to hydraulic stresses applied to the aquifer. Implementation of a lake water budget requires input of parameters including those representing the rate of lake atmospheric recharge and evaporation, overland runoff, and the rate of any direct withdrawal from, or augmentation of, the lake volume. The lake/aquifer interaction may be simulated in both transient and steady-state flow conditions, and the user may specify that lake stages be computed explicitly, semi-implicitly, or fully-implicitly in transient simulations. The lakes, and all sources of water entering the lakes, may have solute concentrations associated with them for use in solute-transport simulations using MOC3D. The Stream Package of MODFLOW-2000 and MOC3D represents stream connections to lakes, either as inflows or outflows. Because lakes with irregular bathymetry can exist as separate pools of water at lower stages, that coalesce to become a single body of water at higher stages, logic was added to the Lake Package to allow the representation of this process as a user option. If this option is selected, a system of linked pools (sublakes) is identified in each time step and stages are equalized based on current relative sublake surface areas. ","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004167","usgsCitation":"Merritt, M.L., and Konikow, L.F., 2000, Documentation of a computer program to simulate lake-aquifer interaction using the MODFLOW ground water flow model and the MOC3D solute-transport model: U.S. Geological Survey Water-Resources Investigations Report 2000-4167, vi, 146 p., https://doi.org/10.3133/wri004167.","productDescription":"vi, 146 p.","costCenters":[{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":159207,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2273,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri00-4167/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6ae4b07f02db63cbb9","contributors":{"authors":[{"text":"Merritt, Michael L.","contributorId":29392,"corporation":false,"usgs":true,"family":"Merritt","given":"Michael","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":200248,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Konikow, Leonard F. 0000-0002-0940-3856 lkonikow@usgs.gov","orcid":"https://orcid.org/0000-0002-0940-3856","contributorId":158,"corporation":false,"usgs":true,"family":"Konikow","given":"Leonard","email":"lkonikow@usgs.gov","middleInitial":"F.","affiliations":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"preferred":true,"id":200247,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":22844,"text":"ofr00255 - 2000 - Fate and transport modeling of selected chlorinated organic compounds at Operable Unit 3, U.S. Naval Air Station, Jacksonville, Florida","interactions":[],"lastModifiedDate":"2012-02-02T00:07:57","indexId":"ofr00255","displayToPublicDate":"2001-08-01T00:00:00","publicationYear":"2000","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":"2000-255","title":"Fate and transport modeling of selected chlorinated organic compounds at Operable Unit 3, U.S. Naval Air Station, Jacksonville, Florida","docAbstract":"Ground water contaminated by the chlorinated organic compounds trichloroethene (TCE), cis-dichloroethene (DCE), and vinyl chloride (VC) has been found in the surficial aquifer beneath the Naval Aviation Depot at the U.S. Naval Air Station, Jacksonville, Florida. The affected area is designated Operable Unit 3 (OU3) and covers 134 acres adjacent to the St. Johns River. \rSite-specific ground-water flow modeling was conducted at OU3 using MODFLOW, and solute-transport modeling was conducted using MT3DMS. Simulations using a low dispersivity value, which resulted in the highest concentration discharging to the St. Johns River, gave the following results. At 60 years traveltime, the highest concentration of TCE associated with the Area C plume had discharged to St. Johns River at a level that exceeded 1x103 micrograms per liter (ug/L). At 100 years traveltime, the highest concentration of TCE associated with the Area D plume had discharged to the river at a level exceeding 3x103 ug/L. At 200 years traveltime, the Area B plume had not begun discharging to the river. \rSimulations using a first-order decay rate half-life of 13.5 years (the slowest documented) at Area G caused the TCE to degrade before reaching the St. Johns River. If the ratio of the concentrations of TCE to cis-DCE and VC remained relatively constant, these breakdown products would not reach the river. However, the actual breakdown rates of cis-DCE and VC are unknown. \rSimulations were repeated using average dispersivity values with the following results. At 60 years traveltime, the highest concentration of TCE associated with the Area C plume had discharged to St. Johns River at a level exceeding 4x102 ug/L. At 100 years traveltime, the highest concentration of TCE associated with the Area D plume had discharged to the river at a level exceeding 1x103 ug/L. At 200 years traveltime, the Area B plume had not begun discharging to the river. \r'Pump and treat' was simulated as a remedial alternative. The concentration of TCE at Area B trended rapidly downward; however, one isolated pocket of TCE remained because of the low-permeability sediments present at this area. The concentration of TCE at Area C trended rapidly downward and was below 1 ug/L in about 16 years. The concentration of TCE at Area D also trended rapidly downward and was below 1 mg/L in about 18 years. ","language":"ENGLISH","publisher":"U.S. Department of the Interior, U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/ofr00255","issn":"0094-9140","usgsCitation":"Davis, J., 2000, Fate and transport modeling of selected chlorinated organic compounds at Operable Unit 3, U.S. Naval Air Station, Jacksonville, Florida: U.S. Geological Survey Open-File Report 2000-255, vi, 36 p. :ill., maps ;28 cm., https://doi.org/10.3133/ofr00255.","productDescription":"vi, 36 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":155205,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":1307,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/ofr00255/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d5e4b07f02db5dde0a","contributors":{"authors":[{"text":"Davis, J. Hal","contributorId":53832,"corporation":false,"usgs":true,"family":"Davis","given":"J. Hal","affiliations":[],"preferred":false,"id":188984,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28821,"text":"wri004096 - 2000 - Characterization and simulation of ground-water flow in the Kansas River Valley at Fort Riley, Kansas, 1990-98","interactions":[],"lastModifiedDate":"2012-02-02T00:08:52","indexId":"wri004096","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2000","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":"2000-4096","title":"Characterization and simulation of ground-water flow in the Kansas River Valley at Fort Riley, Kansas, 1990-98","docAbstract":"Hydrologic data and a ground-water flow model were used to characterize ground-water flow in the Kansas River alluvial aquifer at Fort Riley in northeast Kansas. The ground-water flow model was developed as a tool to project ground-water flow and potential contaminant-transport paths in the alluvial aquifer on the basis of past hydrologic conditions. The model also was used to estimate historical and hypothetical ground-water flow paths with respect to a private- and several public-supply wells. The ground-water flow model area extends from the Smoky Hill and Republican Rivers downstream to about 2.5 miles downstream from the city of Ogden. The Kansas River Valley has low relief and, except for the area within the Fort Riley Military Reservation, is used primarily for crop production. Sedimentary deposits in the Kansas River Valley, formed after the ancestral Kansas River eroded into bedrock, primarily are alluvial sediment deposited by the river during Quaternary time. The alluvial sediment consists of as much as about 75 feet of poorly sorted, coarse-to-fine sand, silt, and clay, 55 feet of which can be saturated with ground water. The alluvial aquifer is unconfined and is bounded on the sides and bottom by Permian-age shale and limestone bedrock. Hydrologic data indicate that ground water in the Kansas River Valley generally flows in a downstream direction, but flow direction can be quite variable near the Kansas River due to changes in river stage. Ground-water-level changes caused by infiltration of precipitation are difficult to detect because they are masked by larger changes caused by fluctuation in Kansas River stage. Ratios of strontium isotopes Sr87 and Sr86 in water collected from wells in the Camp Funston Area indicate that the ground water along the northern valley wall originates, in part, from upland areas north of the river valley. Water from Threemile Creek, which flows out of the uplands north of the river valley, had Sr87:Sr86 ratios similar to those in ground water from wells in the northern Camp Funston Area. In addition, comparison of observed water levels from wells CF90-06, CF97-101, and CF97-401 in the Camp Funston Area and ground-water levels simulated for these wells using floodwave-response analysis indicates that ground-water inflow from bedrock is a hydraulic stress that, in addition to the changing stage in the Kansas River, acts on the aquifer. This hydraulic stress seems to be located near the northern valley wall because the effect of this stress is greater for well CF97-101, which is the well closest to the valley wall. Ground-water flow was simulated using a modular, three-dimensional, finite-difference ground-water flow model (MODFLOW). Particle tracking, used to visualize ground-water flow paths in the alluvial aquifer, was accomplished using MODPATH. Forward-in-time particle tracking indicated that, in general, particles released near the Kansas River followed much more variable paths than particles released near the valley wall. Although particle tracking does not simulate solute transport, this increased path variability indicates that, near the river, ground-water contaminants could follow many possible paths towards the river, whereas more distant from the river, ground-water contaminants likely would follow a narrower corridor. Particle tracks in the Camp Funston Area indicate that, for the 1990-98 simulation period, contaminants from the ground-water study sites in the Camp Funston Area would be unlikely to move into the vicinity of Ogden's supply wells. Backward-in-time particle tracking indicated that the flow-path and recharge areas for model cells corresponding to Ogden's supply wells lie near the northern valley wall and extend into the northern Camp Funston Area. The flow-path and recharge areas for model cells corresponding to Morris County Rural Water District wells lie within Clarks Creek Valley and probably extend outside the model area. Three hypothetical simulations, i","language":"ENGLISH","publisher":"U.S. Department of the Interior, U.S. Geological Survey ;\r\nInformation Services [distributor],","doi":"10.3133/wri004096","usgsCitation":"Myers, N.C., 2000, Characterization and simulation of ground-water flow in the Kansas River Valley at Fort Riley, Kansas, 1990-98: U.S. Geological Survey Water-Resources Investigations Report 2000-4096, viii, 122 p. :ill. (some col.), maps (some col.) ;28 cm., https://doi.org/10.3133/wri004096.","productDescription":"viii, 122 p. :ill. (some col.), maps (some col.) ;28 cm.","costCenters":[],"links":[{"id":95728,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4096/report.pdf","size":"34781","linkFileType":{"id":1,"text":"pdf"}},{"id":159663,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4096/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4ebe","contributors":{"authors":[{"text":"Myers, Nathan C. 0000-0002-7469-3693 nmyers@usgs.gov","orcid":"https://orcid.org/0000-0002-7469-3693","contributorId":1055,"corporation":false,"usgs":true,"family":"Myers","given":"Nathan","email":"nmyers@usgs.gov","middleInitial":"C.","affiliations":[{"id":472,"text":"New Mexico Water Science Center","active":true,"usgs":true}],"preferred":true,"id":200454,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":22402,"text":"ofr00466 - 2000 - MODFLOW-2000, the U.S. Geological Survey Modular Ground-Water Model; documentation of packages for simulating evapotranspiration with a segmented function (ETS1) and drains with return flow (DRT1)","interactions":[],"lastModifiedDate":"2019-02-05T16:11:13","indexId":"ofr00466","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","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":"2000-466","title":"MODFLOW-2000, the U.S. Geological Survey Modular Ground-Water Model; documentation of packages for simulating evapotranspiration with a segmented function (ETS1) and drains with return flow (DRT1)","docAbstract":"Two new packages for the U.S. Geological Survey modular finite-difference ground-water-flow model MODFLOW-2000 are documented. The new packages provide flexibility in simulating evapotranspiration and drain features not provided by the MODFLOW-2000 Evapotranspiration (EVT) and Drain (DRN) Packages. The report describes conceptualization of the packages, input instructions, listings and explanations of the source code, and example simulations.
The new Evapotranspiration Segments (ETS1) Package allows simulation of evapotranspiration with a user-defined relation between evapotranspiration rate and hydraulic head. This capability provides a degree of flexibility not supported by the EVT Package, which has been available in MODFLOW since its initial release. In the ETS1 Package, the relation of evapotranspiration rate to hydraulic head is conceptualized as a segmented line between an evaporation surface, defined as the elevation where the evapotranspiration rate reaches a maximum, and an elevation located at an extinction depth below the evaporation surface, where the evapotranspiration rate reaches zero. The user supplies input to define as many intermediate segment endpoints as desired to define the relation of evapotranspiration rate to head between these two elevations. The EVT Package, in contrast, simulates evapotranspiration with a single linear function.
The new Drain Return (DRT1) Package can be used to simulate the return flow of water discharged from a drain feature back into the ground-water system. The DRN Package, which has been available in MODFLOW since its initial release, does not have the capability to simulate return of flow. If the return-flow option of the DRT1 Package is selected, for each cell designated as a drain-return cell, the user has the option of specifying a proportion of the water simulated as leaving the ground-water system through the drain feature that is to be simulated as returning simultaneously to one other cell in the model.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr00466","issn":"0094-9140","usgsCitation":"Banta, E., 2000, MODFLOW-2000, the U.S. Geological Survey Modular Ground-Water Model; documentation of packages for simulating evapotranspiration with a segmented function (ETS1) and drains with return flow (DRT1): U.S. Geological Survey Open-File Report 2000-466, vi, 127 p., https://doi.org/10.3133/ofr00466.","productDescription":"vi, 127 p.","costCenters":[],"links":[{"id":155983,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2000/0466/report-thumb.jpg"},{"id":51826,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2000/0466/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db648cd0","contributors":{"authors":[{"text":"Banta, Edward R.","contributorId":49820,"corporation":false,"usgs":true,"family":"Banta","given":"Edward R.","affiliations":[],"preferred":false,"id":188182,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":29813,"text":"wri20004015 - 2000 - Aquifer-system compaction and land subsidence: Measurements, analyses, and simulations – The Holly Site, Edwards Air Force Base, Antelope Valley, California","interactions":[],"lastModifiedDate":"2022-01-07T19:28:44.362115","indexId":"wri20004015","displayToPublicDate":"2001-05-01T00:00:00","publicationYear":"2000","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":"2000-4015","title":"Aquifer-system compaction and land subsidence: Measurements, analyses, and simulations – The Holly Site, Edwards Air Force Base, Antelope Valley, California","docAbstract":"Land subsidence resulting from ground-water-level declines has long been recognized as a problem in Antelope Valley, California. At Edwards Air Force Base (EAFB), ground-water extractions have caused more than 150 feet of water-level decline, resulting in nearly 4 feet of subsidence. Differential land subsidence has caused sinklike depressions and earth fissures and has accelerated erosion of the playa lakebed surface of Rogers Lake at EAFB, adversely affecting the runways on the lakebed which are used for landing aircraft such as the space shuttles. Since 1990, about 0.4 foot of aquifer-system compaction has been measured at a deep (840 feet) borehole extensometer (Holly site) at EAFB. More than 7 years of paired ground-water-level and aquifer-system compaction measurements made at the Holly site were analyzed for this study. Annually, seasonal water-level fluctuations correspond to steplike variations in aquifer-system compaction; summer water-level drawdowns are associated with larger rates of compaction, and winter water-level recoveries are associated with smaller rates of compaction. The absence of aquifer-system expansion during recovery is consistent with the delayed drainage and resultant delayed, or residual, compaction of thick aquitards. A numerical one-dimensional MODFLOW model of aquitard drainage was used to refine estimates of aquifer-system hydraulic parameters that control compaction and to predict potential future compaction at the Holly site. The analyses and simulations of aquifer-system compaction are based on established theories of aquitard drainage. Historical ground-water-level and land-subsidence data collected near the Holly site were used to constrain simulations of aquifer-system compaction and land subsidence at the site for the period 1908-90, and ground-water-level and aquifer- system compaction measurements collected at the Holly site were used to constrain the model for the period 1990-97. Model results indicate that two thick aquitards, which total 129 feet or about half the aggregate thickness of all the aquitards penetrated by the Holly boreholes, account for most (greater than 99 percent) of the compaction measured at the Holly site during the period 1990-97. The results of three scenarios of future water-level changes indicate that these two thick aquitards account for most of the future compaction. The results also indicate that if water levels decline to about 30 feet below the 1997 water levels an additional 1.7 feet of compaction may occur during the next 30 years. If water levels remain at 1997 levels, the model predicts that only 0.8 foot of compaction may occur during the same period, and even if water levels recover to about 30 feet above 1997 water levels, another 0.5 foot of compaction may occur in the next 30 years. In addition, only a portion of the compaction that ultimately will occur likely will occur within the next 30 years; therefore, the residual compaction and associated land subsidence attributed to slowly equilibrating aquitards is important to consider in the long-term management of land and water resources at EAFB.
","language":"English","publisher":"U. S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri20004015","usgsCitation":"Sneed, M., and Galloway, D.L., 2000, Aquifer-system compaction and land subsidence: Measurements, analyses, and simulations – The Holly Site, Edwards Air Force Base, Antelope Valley, California: U.S. Geological Survey Water-Resources Investigations Report 2000-4015, vii, 65 p., https://doi.org/10.3133/wri20004015.","productDescription":"vii, 65 p.","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true},{"id":35860,"text":"Ohio-Kentucky-Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":159077,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":394045,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_26214.htm"},{"id":11192,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/2000/wri004015/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"California","otherGeospatial":"Antelope Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.19503784179688,\n 35.16819542676796\n ],\n [\n -118.90228271484374,\n 34.84536693184099\n ],\n [\n -118.91189575195312,\n 34.78222760653013\n ],\n [\n -117.45620727539062,\n 34.30260622622907\n ],\n [\n -117.54959106445312,\n 35.163704834815874\n ],\n [\n -118.19503784179688,\n 35.16819542676796\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac5e4b07f02db679f12","contributors":{"authors":[{"text":"Sneed, Michelle 0000-0002-8180-382X micsneed@usgs.gov","orcid":"https://orcid.org/0000-0002-8180-382X","contributorId":155,"corporation":false,"usgs":true,"family":"Sneed","given":"Michelle","email":"micsneed@usgs.gov","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":202172,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Galloway, Devin L. 0000-0003-0904-5355 dlgallow@usgs.gov","orcid":"https://orcid.org/0000-0003-0904-5355","contributorId":679,"corporation":false,"usgs":true,"family":"Galloway","given":"Devin","email":"dlgallow@usgs.gov","middleInitial":"L.","affiliations":[{"id":5078,"text":"Southwest Regional Director's Office","active":true,"usgs":true},{"id":35860,"text":"Ohio-Kentucky-Indiana Water Science Center","active":true,"usgs":true},{"id":5058,"text":"Office of the Chief Scientist for Water","active":true,"usgs":true},{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true},{"id":509,"text":"Office of the Associate Director for Water","active":true,"usgs":true}],"preferred":true,"id":202173,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":23764,"text":"ofr2000185 - 2000 - Hydrogeology and simulation of ground-water flow at the Gettysburg Elevator Plant Superfund Site, Adams County, Pennsylvania","interactions":[],"lastModifiedDate":"2022-08-31T20:46:57.544871","indexId":"ofr2000185","displayToPublicDate":"2001-04-01T00:00:00","publicationYear":"2000","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":"2000-185","title":"Hydrogeology and simulation of ground-water flow at the Gettysburg Elevator Plant Superfund Site, Adams County, Pennsylvania","docAbstract":"Ground water in Triassic-age sedimentary fractured-rock aquifers in the area of Gettysburg, Pa., is used as drinking water and for industrial and commercial supply. In 1983, ground water at the Gettysburg Elevator Plant was found by the Pennsylvania Department of Environmental Resources to be contaminated with trichloroethene, 1,1,1-trichloroethane, and other synthetic organic compounds. As part of the U.S. Environmental Protection Agency?s Comprehensive Environmental Response, Compensation, and Liability Act, 1980 process, a Remedial Investigation was completed in July 1991, a method of site remediation was issued in the Record of Decision dated June 1992, and a Final Design Report was completed in May 1997. In cooperation with the U.S. Environmental Protection Agency in the hydrogeologic assessment of the site remediation, the U.S. Geological Survey began a study in 1997 to determine the effects of the onsite and offsite extraction wells on ground-water flow and contaminant migration from the Gettysburg Elevator Plant. This determination is based on hydrologic and geophysical data collected from 1991 to 1998 and on results of numerical model simulations of the local ground-water flow-system.\r\n\r\nThe Gettysburg Elevator Site is underlain by red, green, gray, and black shales of the Heidlersburg Member of the Gettysburg Formation. Correlation of natural-gamma logs indicates the sedimentary rock strike about N. 23 degrees E. and dip about 23 degrees NW. Depth to bedrock onsite commonly is about 6 feet but offsite may be as deep as 40 feet.\r\n\r\nThe ground-water system consists of two zones?a thin, shallow zone composed of soil, clay, and highly weathered bedrock and a thicker, nonweathered or fractured bedrock zone. The shallow zone overlies the bedrock zone and truncates the dipping beds parallel to land surface. Diabase dikes are barriers to ground-water flow in the bedrock zone. The ground-water system is generally confined or semi-confined, even at shallow depths.\r\n\r\nDepth to water can range from flowing at land surface to more than 71 feet below land surface. Potentiometric maps based on measured water levels at the Gettysburg Elevator Plant indicate ground water flows from west to east, towards Rock Creek. Multiple-well aquifer tests indicate the system is heterogeneous and flow is primarily in dipping beds that contain discrete secondary openings separated by less permeable beds. Water levels in wells open to the pumped bed, as projected along the dipping stratigraphy, are drawn down more than water levels in wells not open to the pumped bed.\r\n\r\nGround-water flow was simulated for steady-state conditions prior to pumping and long-term average pumping conditions. The three-dimensional numerical flow model (MODFLOW) was calibrated by use of a parameter estimation program (MODFLOWP). Steady-state conditions were assumed for the calibration period of 1996. An effective areal recharge rate of 7 inches was used in model calibration. The calibrated flow model was used to evaluate the effectiveness of the current onsite and offsite extraction well system. The simulation results generally indicate that the extraction system effectively captures much of the ground-water recharge at the Gettysburg Elevator Plant and, hence, contaminated ground-water migrating from the site. Some of the extraction wells pump at low rates and have very small contributing areas. Results indicate some areal recharge onsite will move to offsite extraction wells.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr2000185","collaboration":"Prepared in cooperation with the U.S. Environmental Protection Agency","usgsCitation":"Low, D.J., Goode, D., and Risser, D.W., 2000, Hydrogeology and simulation of ground-water flow at the Gettysburg Elevator Plant Superfund Site, Adams County, Pennsylvania: U.S. Geological Survey Open-File Report 2000-185, vi, 34 p., https://doi.org/10.3133/ofr2000185.","productDescription":"vi, 34 p.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":203590,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":7640,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2000/185/","linkFileType":{"id":5,"text":"html"}},{"id":406040,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_30032.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Pennsylvania","county":"Adams County","otherGeospatial":"Gettysburg Elevator Plant Superfund Site","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.25,\n 39.833\n ],\n [\n -77.208,\n 39.833\n ],\n [\n -77.208,\n 39.883\n ],\n [\n -77.25,\n 39.883\n ],\n [\n -77.25,\n 39.833\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db625380","contributors":{"authors":[{"text":"Low, Dennis J. djlow@usgs.gov","contributorId":3450,"corporation":false,"usgs":true,"family":"Low","given":"Dennis","email":"djlow@usgs.gov","middleInitial":"J.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":true,"id":190678,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Goode, Daniel J. 0000-0002-8527-2456 djgoode@usgs.gov","orcid":"https://orcid.org/0000-0002-8527-2456","contributorId":2433,"corporation":false,"usgs":true,"family":"Goode","given":"Daniel J.","email":"djgoode@usgs.gov","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":false,"id":190677,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Risser, Dennis W. 0000-0001-9597-5406 dwrisser@usgs.gov","orcid":"https://orcid.org/0000-0001-9597-5406","contributorId":898,"corporation":false,"usgs":true,"family":"Risser","given":"Dennis","email":"dwrisser@usgs.gov","middleInitial":"W.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":true,"id":190676,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":38118,"text":"ofr00184 - 2000 - MODFLOW-2000, the U.S. Geological Survey modular ground-water model; user guide to the observation, sensitivity, and parameter-estimation processes and three post-processing programs","interactions":[],"lastModifiedDate":"2017-07-11T13:45:37","indexId":"ofr00184","displayToPublicDate":"2001-04-01T00:00:00","publicationYear":"2000","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":"2000-184","title":"MODFLOW-2000, the U.S. Geological Survey modular ground-water model; user guide to the observation, sensitivity, and parameter-estimation processes and three post-processing programs","docAbstract":"This report documents the Observation, Sensitivity, and Parameter-Estimation Processes of the ground-water modeling computer program MODFLOW-2000. The Observation Process generates model-calculated values for comparison with measured, or observed, quantities. A variety of statistics is calculated to quantify this comparison, including a weighted least-squares objective function. In addition, a number of files are produced that can be used to compare the values graphically. The Sensitivity Process calculates the sensitivity of hydraulic heads throughout the model with respect to specified parameters using the accurate sensitivity-equation method. These are called grid sensitivities. If the Observation Process is active, it uses the grid sensitivities to calculate sensitivities for the simulated values associated with the observations. These are called observation sensitivities. Observation sensitivities are used to calculate a number of statistics that can be used (1) to diagnose inadequate data, (2) to identify parameters that probably cannot be estimated by regression using the available observations, and (3) to evaluate the utility of proposed new data.
The Parameter-Estimation Process uses a modified Gauss-Newton method to adjust values of user-selected input parameters in an iterative procedure to minimize the value of the weighted least-squares objective function. Statistics produced by the Parameter-Estimation Process can be used to evaluate estimated parameter values; statistics produced by the Observation Process and post-processing program RESAN-2000 can be used to evaluate how accurately the model represents the actual processes; statistics produced by post-processing program YCINT-2000 can be used to quantify the uncertainty of model simulated values.
Parameters are defined in the Ground-Water Flow Process input files and can be used to calculate most model inputs, such as: for explicitly defined model layers, horizontal hydraulic conductivity, horizontal anisotropy, vertical hydraulic conductivity or vertical anisotropy, specific storage, and specific yield; and, for implicitly represented layers, vertical hydraulic conductivity. In addition, parameters can be defined to calculate the hydraulic conductance of the River, General-Head Boundary, and Drain Packages; areal recharge rates of the Recharge Package; maximum evapotranspiration of the Evapotranspiration Package; pumpage or the rate of flow at defined-flux boundaries of the Well Package; and the hydraulic head at constant-head boundaries. The spatial variation of model inputs produced using defined parameters is very flexible, including interpolated distributions that require the summation of contributions from different parameters.
Observations can include measured hydraulic heads or temporal changes in hydraulic heads, measured gains and losses along head-dependent boundaries (such as streams), flows through constant-head boundaries, and advective transport through the system, which generally would be inferred from measured concentrations.
MODFLOW-2000 is intended for use on any computer operating system. The program consists of algorithms programmed in Fortran 90, which efficiently performs numerical calculations and is fully compatible with the newer Fortran 95. The code is easily modified to be compatible with FORTRAN 77. Coordination for multiple processors is accommodated using Message Passing Interface (MPI) commands. The program is designed in a modular fashion that is intended to support inclusion of new capabilities.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Denver, CO","doi":"10.3133/ofr00184","issn":"0094-9140","collaboration":"Prepared in cooperation with the U.S. Department of Energy","usgsCitation":"Hill, M.C., Banta, E.R., Harbaugh, A., and Anderman, E., 2000, MODFLOW-2000, the U.S. Geological Survey modular ground-water model; user guide to the observation, sensitivity, and parameter-estimation processes and three post-processing programs: U.S. Geological Survey Open-File Report 2000-184, Report: ix, 209 p. , https://doi.org/10.3133/ofr00184.","productDescription":"Report: ix, 209 p. ","startPage":"1","endPage":"209","numberOfPages":"219","costCenters":[{"id":493,"text":"Office of Ground Water","active":true,"usgs":true}],"links":[{"id":165531,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2000/0184/report-thumb.jpg"},{"id":64368,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2000/0184/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":3454,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://water.usgs.gov/nrp/gwsoftware/modflow2000/ofr00-184.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db648cee","contributors":{"authors":[{"text":"Hill, Mary C. mchill@usgs.gov","contributorId":974,"corporation":false,"usgs":true,"family":"Hill","given":"Mary","email":"mchill@usgs.gov","middleInitial":"C.","affiliations":[{"id":5044,"text":"National Research Program - Central Branch","active":true,"usgs":true}],"preferred":true,"id":219055,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Banta, E. R.","contributorId":63038,"corporation":false,"usgs":true,"family":"Banta","given":"E.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":219057,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Harbaugh, A.W.","contributorId":15208,"corporation":false,"usgs":true,"family":"Harbaugh","given":"A.W.","email":"","affiliations":[],"preferred":false,"id":219054,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Anderman, E.R.","contributorId":62241,"corporation":false,"usgs":true,"family":"Anderman","given":"E.R.","affiliations":[],"preferred":false,"id":219056,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ]}