This report, which was prepared in cooperation with the city of Houston and the Harris-Galveston Coastal Subsidence District, presents data on water-level changes in the Chicot and Evangeline aquifers.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr88168","usgsCitation":"Gabrysch, R., Ranzau, C., and Coplin, L., 1988, Approximate water-level changes in wells completed in the Chicot and Evangeline aquifers, 1977-88 and 1987-88, and measured compaction, 1973-88, in the Houston-Galveston region, Texas: U.S. Geological Survey Open-File Report 88-168, 7 p., https://doi.org/10.3133/ofr88168.","productDescription":"7 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":390286,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_17353.htm"},{"id":79480,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1988/0168/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":173084,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1988/0168/report-thumb.jpg"}],"country":"United States","city":"Galveston, Houston","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -96,\n 29\n ],\n [\n -94.75,\n 29\n ],\n [\n -94.75,\n 30.179\n ],\n [\n -96,\n 30.179\n ],\n [\n -96,\n 29\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4af3e4b07f02db691bb9","contributors":{"authors":[{"text":"Gabrysch, R.K.","contributorId":105691,"corporation":false,"usgs":true,"family":"Gabrysch","given":"R.K.","affiliations":[],"preferred":false,"id":225509,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ranzau, C.E. 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intermediate aquifer system, west-central Florida, May 1987","docAbstract":"The intermediate aquifer system within the Southwest Florida Water Management District underlies a 5,000 sq mi area of De Soto, Sarasota, Hardee, Manatee, and parts of Charlotte, Hillsborough, Highlands, and Polk Counties. The intermediate aquifer system occurs between the overlying surficial aquifer system and the underlying Floridan aquifer system, and consists of layers of sand, shell, clay, marl, limestone, and dolom of the Tamiami, Hawthorn, and Tampa Formations of late Tertiary age. The intermediate aquifer system contains one or more water-bearing units separated by discontinuous confining units. This aquifer system is the principal source of potable water in the southwestern part of the study area and is widely used as a source of water in other parts where wells are open to the intermediate aquifer system or to both the intermediate and Floridan aquifer systems. Yields of individual wells open to the intermediate aquifer system range from a few gallons to several hundred gallons per minute. The volume of water withdrawn from the intermediate aquifer system is considerably less than that withdrawn from the Floridan aquifer system in the study area. The surface was mapped by determining the altitude of water levels in a network of wells and is represented on maps by contours that connect points of equal altitude. The compos potentiometric surface of all water-bearing units within the intermediate aquifer system is shown. In areas where multiple aquifers exist, wells open to all aquifers were selected for water level measurements whenever possible. In the southwestern and lower coastal region of the study area, two aquifers and confining units are described for the intermediate aquifer system: the Tamiami-upper Hawthorn aquifer and the underlying lower Hawthorn-upper Tampa aquifer. The potentiometric surface of the Tamiami-upper Hawthorn aquifer is also shown. Water levels are from wells drilled and open exclusively to that aquifer. The exact boundary for the Tamiami-upper Hawthorn aquifer is undetermined because of limd geohydrologic data available from wells.
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The extent to which these plant communities are capable of adapting to and surviving fluctuations in the water table depends on physiological adaptations of the plants and on the water content, matric potential characteristics of the soils. Two methods were used to estimate soil matric potential in test sites in Owens Valley. The first was the filter-paper method, which uses water content of filter papers equilibrated to water content of soil samples taken with a hand auger. The other method of estimating soil matric potential was a modeling approach based on data from this and previous investigations. These data indicate that the base 10 logarithm of soil matric potential is a linear function of gravimetric soil water content for a particular soil. Estimates of soil water characteristic curves were made at two sites by averaging the gravimetric soil water content and soil matric potential values from multiple samples at 0.1 m depths derived by using the hand auger and filter paper method and entering these values in the soil water model. The characteristic curves then were used to estimate soil matric potential from estimates of volumetric soil water content derived from neutron-probe readings. Evaluation of the modeling technique at two study sites indicated that estimates of soil matric potential within 0.5 pF units of the soil matric potential value derived by using the filter paper method could be obtained 90 to 95% of the time in soils where water content was less than field capacity. The greatest errors occurred at depths where there was a distinct transition between soils of different textures. 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